7 DAY

 
EARTH SCIENCE IN ‘
THE PUBLIC SERVICE

A symposium presented during dedication ceremonies,
U.S. Geological Survey National Center, Reston, Virginia, July 10—13, 1974

 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 921

Contributions from .'

Canada Department of Energy, Mines and Resources _
Council on Environmental Quality, Executive Oﬂice of the President

Dartmouth College, Department of Earth Sciences
Environmental Research Institute of [Michigan
Illinois State Geological Survey
johns Hopkins University, Department of Geography and
Environmental Engineering
Massachusetts Institute of Technology, Department of Earth and
Planetary Sciences
Oﬁice of Senator Paul]. Fannin
Pennsylvania State University, Department of Mineral Economics
Resources for the Future, Inc.
Syracuse University, Department of Geology
U.S. Department of Commerce, National Oceanic and Atmospheric
Administration
U.S. Department of the Interior
Assistant Secretary for Fish and Wildlife and Parks
Geological Survey
University of Oklahoma, Science and Public Policy Program
Virginia Division of Mineral Resources

 
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EARTH SCIENCE IN
THE PUBLIC SERVICE

A symposium presented during dedication ceremonies,
US. Geological Survey National Center, Reston, Virginia, July 10—13, 1974

 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 921

Contributions from:

Canada Department of Energy, [Mines and Resources

Council on Environmental Quality, Executive Oﬂice of the President

Dartmouth College, Department of Earth Sciences

Environmental Research Institute of Michigan

Illinois State Geological Survey

Johns Hopkins University, Department of Geography and
Environmental Engineering

Massachusetts Institute of Technology, Department of Earth and
Planetary Sciences

Oﬂice of Senator Paul]. Fannin

Pennsylvania State University, Department of Mineral Economics

Resources for the Future, Inc.

Syracuse University, Department of Geology

US. Department of Commerce, National Oceanic and Atmospheric
Administration

US Department of the Interior
Assistant Secretary for Fish and Wildlife and Parks

Geological Survey
University of Oklahoma, Science and Public Policy Program
Virginia Division of Mineral Resources

 
UNITED STATES GOVERNMENT PRINTING OFFICE, \VASHINGTON : 1974

tunes

UNITED STATES DEPARTMENT OF THE INTERIOR

ROGERS C. B. MORTON, Secretary

GEOLOGICAL SURVEY

V. E. McKelvey, Director

Library of Congress catalog-card No. 74-600198

 
For sale by the Superintendent of Documents, US. Government Printing Office
Washington, D.C. 20402 — Price $2.15 (paper cover)
Stock Number 2401—02594

CONTENTS

Welcoming remarks, by V. E. McKelvey, Director, US. Geological
Survey _________________________________________________
Geological surveys in the public service, by Charles H. Smith,
Assistant Deputy Minister, Canada Department of Energy,
Mines and Resources ______________________________________
New directions for energy policy and analysis, by Joseph L. Fisher,
Director, Resources for the Future, Inc. _____________________
Mineral-resource appraisal and analysis, by John Drew Ridge,
Head, Department of Mineral Economics, Pennsylvania State
University ______________________________________________
Crisis and catastrophe in water-resources policy, by M. Gordon
Wolman, Chairman, Department of Geography and Environ-
mental Engineering, Johns Hopkins University ______________
Environmental analysis and earth sciences in the public service, by
Beatrice E. Willard, Council on Environmental Quality, Execu-
tive Oﬂ‘ice of the President ________________________________
Lease management and resource conservation, by Don E. Kash,
Director, Science and Public Policy Program, University of
Oklahoma _______________________________________________
Resource and environmental data analysis, by Daniel F. Merriam,
Chairman, Department of Geology, Syracuse University ______
New directions in topographic mapping. by James L. Calver, State
Geologist, Virginia Division of Mineral Resources ___________
Geodynamics, by Charles L. Drake, Department of Earth Sciences,
Dartmouth College __________________~________-__. _________
Earth-resource surveys, by George J. Zissis, Chief Scientist, En-
vironmental Research Institute of Michigan _________________
Federal interagency coordination of natural-resources studies, by
Robert M. White, Administrator, National Oceanic and Atmos-
pheric Administration _____________________________________
Land resource—its use and analysis, by John C. Frye, Chief, Illinois
State Geological Survey ___________________________________
Technology information transfer, by Joseph S. J enckes, Administra-
tive Assistant to Senator Paul J. Fannin ____________________
Interdisciplinary approach to the solution of natural-resources prob-
lems, by Nathaniel P. Reed, Assistant Secretary of the Interior
for Fish and Wildlife and Parks ___________________________
Natural-hazards reduction, by Frank Press, Chairman, Department
of Earth and Planetary Sciences, Massachusetts Institute of
Technology _____________________________________________

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71

 
EARTH SCIENCE IN THE PUBLIC SERVICE

WELCOMING REMARKS

By V. E. MCKELVEY
Director, US. Geological Survey

Welcome to our symposium on “Earth Science in the Public Service”
and to the dedication of the John Wesley Powell Federal Building.

I appreciate your coming—especially our distinguished speakers who
have given so generously of their valuable time to come and share their
views on the important topics to be discussed here today and tomorrow.

The dedication of this building is a ﬁtting occasion for the symposium
We are now beginning, for earth science in the public service is, of course,
what the US. Geological Survey is all about. Had there been no such occa-
sion, however, it would have been desirable to create one, for we are at a
stage in this country’s, and indeed the world’s, development where we face
critical problems whose solution requires the application and further de-
velopment of earth science. Problems of energy, minerals, and water-
resource adequacy, of land use and preservation of environmental quality,
of the management of the resources of the public lands, and of the reduction
of natural hazards are examples of problems in the domain of the earth
sciences that are of critical importance to the Nation’s future.

It is not only appropriate, therefore, to focus on this topic of earth
science in the public service, but urgent that we do so with the greatest
perception and imagination at our command. We in the US. Geological
Survey are applying ourselves as vigorously as we can to the problems I
mentioned, but in planning this program, we expressed our need and desire
to have the beneﬁt of other ‘viewpoints. The response to our invitations to
speak on these topics has been heartwarming, for our speakers are dis-
tinguished leaders in their respective ﬁelds, and they have paid us a great
compliment in coming to share their views with us.

We plan to publish the papers that will be given here today, and I am
sure that the result will be a valuable guide not only to us in the US.
Geological Survey but to all who are concerned with public problems in the
earth-science domain.

Again, welcome, and thank you for coming.

EARTH SCIENCE IN THE PUBLIC SERVICE

GEOLOGICAL SURVEYS IN THE PUBLIC SERVICE

By CHARLES H. SMITH
Assistant Deputy Minister, Canada Department of Energy, Mines and Resources

I am honored to have been invited to join and
speak with you on the occasion of the dedication of
the John Wesley Powell Federal Building—this re-
markable building which is named after an outstand-
ing geologist and explorer, which represents your
National Center for earth studies, and which stands
for both the historical past and the future chal-
lenges facing the United States Geological Survey.
The reputation of the U.S.G.S. extends to all parts
of the world, and it is obvious that Major Powell and
the other scientists and politicians who were re-
sponsible for establishing the Survey in 1879
“planned better than they knew.”

The phrase “geological survey” means different
things to different people. To some it is the system-
atic recording of rock types along a picket line in
the bush or a steep mountainside, and it excludes
geophysical, geochemical, topographic, and other
related surveys of the Earth. To some, the phrase
refers to routine work and not to research, which
is called instead “geological science” or “earth
science.” Modern specialization has led to a multi-
plicity of professions, societies, and allegiances,
which feel more comfortable under such collective
phrases as “earth sciences,” “earth resources,” and
“earth surveys.” We increasingly use these latter
phrases to the point where people may rightly ask,
“What is this institution—the Geological Survey?
Either it is misnamed for the scope of its legitimate
activities, or, alternatively, it is doing things beyond
its mandate. By all the sacred principles of pro-
gram planning and budgeting the Geological Survey
should cease and desist, cut out these other activities
and use the money for geological work in the nar-
row sense, or, alternatively, why not rename the in-
stitution—perhaps the National Earth Surveys and
Research Institution?” It is unfortunately necessary

2

 
to remind the uninitiated continually that geology
means “the study of the Earth”; it is a respected
name with a long and honorable history and is not
a specialized subdivision of the term “earth sci-
ences.” Geology is an integrating science, created
directly from man’s observation of natural phenom—
ena and his effort to understand them and make
use of them, and it is based upon many basic sciences
and common sense.

I submit to you that the concept of a geological
survey in government today is the same as originally
conceived by your Powell, and by our Logan, the
founder of the Geological Survey of Canada. It
encompasses the full spectrum of scientiﬁc and
technical activities to provide data, information, and
advice on the national landmass and its resources,
thus ensuring proper husbandry of the land and
proper government of the nation. The original geo—
logical surveys included not only the full range of
earth resource, survey, and science activities of
their day, but, in addition, studies of the ﬂora,
fauna, and native peoples; the geologists of the day
were indeed broad in interests and practice. Today,
in many countries, these earth-oriented activities
have become increasingly dispersed through a num-
ber of organizations, federal, state, or provincial,
in universities and industry. Earth-science experi-
tise has developed in various parts of government
to serve such policy areas as defense, transport, agri-
culture, environment, and energy, to name a few.
The institution originally named the national geo-
logical survey is now a lesser component of the total
earth survey-science-resource function of govern-
ment than it was when originally formed. Neverthe-
less, the need of governments for accurate and timely
information on their landmass and its resource base
has not diminished, and one of the questions of the

GEOLOGICAL SURVEYS IN THE PUBLIC SERVICE 3

day is the role of responsibility of the national geo-
logical survey in providing that information and
advice. My thesis is that governments, and the public,
need, more than ever, to know in an integrated way
about the landmass and its contained resources, and
the conceptual model of the original geological sur-
veys offers the best means of acquiring such know-
ledge as against recent trends of institutionally dis-
persing the inventory task.

To appreciate a central government’s interests and
responsibilities in earth studies, it is beneﬁcial to
look back to the early evolution of earth surveys,
earth sciences, and interest in earth resources, which
resulted in positive action by both our governments
to formally establish geological surveys in the last
century. Then we might consider brieﬂy the chang—
ing policies and thrusts of these organizations over
the years, the scope of their involvement in human
affairs, and the changing needs of the future.

Earth surveys, earth sciences, and earth resources
have been inextricably entwined in the support of
mankind’s occupation and use .of our planet. One
can look far back to the ﬁrst use of earth resources
—ﬂint, chert and other hard stones—for weapons
by primitive man. Economic geology may have had
its inception with the desire for gem stones and
metals by the Egyptians and Greeks. This led to
mining activities by the Egyptians as early as 2000
B.C. The early history of earth. surveys, or maps,
is not easy to trace, but it is difﬁcult to imagine a
time when there were no maps. The ancient Baby-
lonians certainly practiced surveying, having made
a cadastral survey of their kingdom in 2800 B.C.
Earth sciences followed in historical sequence, as
mankind developed both the need and the capability
to study and understand the mysteries of the Earth,
for both intellectual and practical beneﬁt. The great
sea voyages of the 16th to 18th centuries sparked
research in mapmaking, geodesy, and magnetism.
This was the period of Mercator’s maps, Copernicus’
solar system, and Newton’s theory of gravitation. If
one were to draw a conclusion from the early histori-
cal record, it would be that the conduct of earth sur-
veys, interest in the earth sciences, and the develop-
ment and use of earth resources grew steadily in
response to man’s occupation of the Earth. In critical
periods, earth surveys and sciences were of signiﬁ-
cant importance.

In the last century, at the period of the Industrial
Revolution, man’s interest increased remarkably in
the search for greater quantities of earth resources.
The development of new lands in the Americas not
only depended upon the availability of mineral re—

 
sources but also on surveys of and information on
the land surface and its potential use. Geology was
turning more and more into an exact science based
upon a body of clear principles. Geologists ac-
cepted the concepts that rocks had formed by proces-
ses similar to those in action today; that in undis-
turbed strata the upper layers are younger; that
fossils change from older to younger beds and can
be used for regional or even worldwide correlation.
There were strong debates over the sedimentary
versus igneous origin of rocks, and considerable
progress was being made in establishing a uniform
system of stratigraphic nomenclature. It was this
fortunate conﬂuence of intellectual ferment, indus-
trialization, and settlement that formed the en—
vironment for the earth sciences, through geology,
to assume a major role in governmental endeavors.

Governments have traditionally funded earth
surveys in order to eifectively administer the affairs
of a land. Most of the earlier applications had cen-
tered around military activities and land settlement.
In the early years of the 19th century, many States
in your country sponsored geological surveys to
evaluate the mineral resources and to help with the
disposal of State lands. Some, such as the New York
Survey, were quite successful, but others were of
short duration. It is a mark of the wisdom and fore-
sight of a generation, or governments, when major
governmental structures are established and main-
tained well in advance of a need or crisis. Such events
occurred when national geological surveys such as
the US. Geological Survey and the Geological Survey
of Canada were formally established in the last cen—
tury. I do not suggest that these organizations were
not needed at the time of their formation—rather,
that the needs are greater, far greater, today than
when Powell and Logan attended to the creation
and development of our broadly conceived Geological
Surveys.

The directions given by governments to the ﬁrst
directors of these Surveys, many years ago, are
as meaningful today as when they were ﬁrst stated.
Clarence King, your ﬁrst Director, was required to
“examine the geological structure, mineral resources,
and products of the national domain, and to classify
public lands.” William Logan was called upon to
“make an accurate and complete geological survey
and furnish a full and scientiﬁc description of its
rocks, soils and minerals which shall be accom-
panied With proper maps, diagrams, and drawings,
together with a collection of specimens to illustrate
the same.” Of course, in neither case did the govern-
ments of the day adequately estimate the cost or

4 EARTH SCIENCE IN THE PUBLIC SERVICE

time span of such a task. Nevertheless, they pointed
in the right direction and laid the foundation for
the earth-resource knowledge base of our Nations
today. The Surveys they created have become major
instruments of economic and scientiﬁc development,
with far-reaching effects that have gone beyond
our national boundaries. The systematic examina-
tion of our national domains over the years has
had the dual characteristic of establishing an in-
ventory of mineral resources and the facts of nature,
through repeated observations.

Governments have grown in size and complexity
since the early founding years of their geological
surveys. They have passed through years of abund-
ance and shortages, wars, and depressions. In each
case the geological surveys have responded to the
challenges placed upon them—to provide the nation
with information and advice on its landmass and
resources. In their formative years, work evolved
around the exploration and settlement of the land.
The members of the survey became the foremost
authorities on the unsettled regions. Their reports,
maps, displays, and lectures drew the attention of
governments, industry, and the public to the re-
sources and opportunities of the land. Along with
their surveys came many scientiﬁc discoveries which
attracted the attention of the international scien—
tiﬁc community. The surveys established a close re-
lationship with the mining industry, providing in-
formation and ideas that guided prospectors to the
most promising areas, contributing to the opening of
major mining regions and to the development of
important mines. At times they were criticized for
being too closely involved in the search for, as op-
posed to research on, ore deposits. At other times
they were criticized for being too academic, or
working in geographic areas too remote and inac—
cessible for short-term economic development. How-
ever, through this complementary relationship,
industry and government have been successful in
reaching a high level of mineral development in
our lands. The geological surveys have also developed
their supporting role to governments through the
provision of sound information and advice for agri-
culture, for the military, for space programs, nu-
clear programs, foreign aid programs, earthquake
and hazards prediction, engineering work, energy
development, and many more. During both World
Wars, the survey staff's were engaged in major stra-
tegic mineral programs and resource appraisals.

Geological surveys today are being put under
increasingly severe pressure, probably greater than
have existed in any peacetime period since the time

 
of Powell and Logan. Human occupation over the
surface of the Earth has grown to such an extent
that man is recognized as a signiﬁcant geological
agent. He has touched all parts of the Earth’s sur—
face, penetrated the depths of the oceans, and ven-
tured into space. What he does not touch, he senses
remotely. His erosion of nature’s bounty is putting
into question the adequacy of resources to maintain,
for the future, established standards of life, and his
alteration of the environment has created concerns
about his ability to survive under conditions made
almost suddenly different from those under which he
has evolved. In the last 150 years, man’s develop-
ment has not been in the Wise light of integrated
knowledge but rather along compartmentalized
thrusts. A developing technology and population have
dictated at each moment or period of time the meas-
ure to which the Earth’s resources are used. A
systematic measure of the Earth’s capabilities has
not been the standard of man’s discipline towards
nature. Such a measure of the Earth’s capacity to
stand modiﬁcations in its materials and in the
regimen of processes should derive from the type
of concerted action for which our geological surveys
were created. Unfortunately, man’s use of the Earth
has outstripped the rate at which the knowledge
of our lands and their resource base has been gen-
erected, communicated, and understood by policy—
makers and the public. The aim of Powell to “edu-
cate the nation” has not yet been achieved in any
country.

The public is now becoming increasing interested
and concerned with the results of their geological
surveys—and let us remember again the direction to
Powell and Logan “to survey the mineral resources.”
Now the public and governments are concerned over
increased warnings of resource depletion. The Secre-
tary of your Department, Mr. Morton, stated
recently that “the United States, and the world as
a Whole, face a crisis of exhausted natural resources
within 25 years unless they act soon to develop the
long range planning to prevent it.” There have been
equally startling statements about man’s effect on
his environment. Who will provide the public with
the basic information respecting resource depletion
or degradation of the physical environment? I sub-
mit that this is the responsibility of the national
geological surveys.

It might be asked, “Could not this responsibility
be undertaken by industry?” The task of gathering
information on the mineral endowment and land-
mass has been pursued in the United States and Can-
ada, since Powell and Logan, by industry, State (or

GEOLOGICAL SURVEYS IN THE PUBLIC SERVICE 5

Provincial), and Federal institutions, supported to
a lesser extent by university groups. The success
of industry, in particular, has resulted from its
ability to develop and exploit resource data in a
competitive and conﬁdential manner. A great many
data have thus been collected by many groups, but
they are not well coordinated or synthesized in a
national sense. Although industry has synthesized
national data for fuels, there have been no com-
parable national estimates by industry for the other
mineral resources. The separate roles of industry
and governments in the process of resource inven—
tory over the past hundred years is reminiscent of
the situation in the 1870’s, when rivalry between
the military and civilian surveys brought disorder to
government science, reduced public conﬁdence in it,
and resulted in the formation of the U.S. Geological
Survey to reduce duplication and increase efﬁciency!
Without belittling the tremendous knowledge and
expertise developed by industry, I believe that the
public is now seeking its own independent source of
advice on the resources and environment of the
nations. In our universities and nonproﬁt research
organizations, there are admittedly experienced and
interested scientists with interests and viewpoints on
the resource base and its adequacy. Their role is
extremely important in developing new methodolo-
gies and new concepts and in assisting with the
major role of educating the public. They lack, how-
ever, access to a sizeable data base which permits
factual and timely statements on the national and
international resource situation today.

Can a geological survey produce the timely and
meaningful analyses required for the resource and
environmental policies of the next decade? For geo-
logical surveys to rise to this increasing responsi-
bility will require the focusing of talents and eiforts
in a manner not unlike that of wartime, but the
possibilities of disaster warrant such a reaction, even
if only to prove the predictions to be unfounded or
premature. However, this advisory activity is
fraught with many problems. The time is short. The
existing data base is inadequate. A pooling of in-
dustrial and government data will be required for
immediate effectiveness, along with new programs
to obtain data from as—yet—unexplored regions. It is
essential to an informed debate that the basic obser—
vations of industry and other groups become in-
creasingly accessible in the public realm, and new
legislation may be required to bear on this problem.

That is not all. We know that a single drill hole
can still turn a “barren region” into a “Prudhoe‘
Bay.” We must recognize that the methodology for

 
manipulating resource data and forecasting concen-
trations in unexplored areas is also inadequate. Much
depends upon intuition—or qualitative interpreta—
tions. We must look to those experiences in the
vagaries of geology to extrapolate, now with the aid
of the computer, the possible abundances of metals or
fuels in unexplored areas. But how will the quality
of their work be tested? It may not be subjected to
the test used by industry—drilling—for many years.
It may not be subjected to the normal tests of
science—the reproducibility of results. Under such
circumstances, the whims or judgments of a few
specialists can have a major inﬂuence on the policies
of a nation. In this area of judgment where the facts
are not crystal clear, the special interests of scien—
tists can easily inﬂuence their interpretations. Hence,
a new system of checks and balances will have to be
developed within the scientiﬁc community to test
the work and conclusions of their colleagues. It will
be a test of our geological surveys Whether they suc-
ceed in mobilizing our limited national expertise
from all sectors for this work, and thus show true
national leadership, or become merely one of a rising
babel on the world scene. What additional problems
will this create for the geological survey? There will
be problems of credibility, as the forecasts change
when new information is added. There will be prob-
lems of communication in explaining the meaning
and variations of resource estimates. There will be
problems in confronting professional experts from
other sectors, and in debating the technical termin-
ology, data, and interpretations in a public forum.
However, such debates will have to occur with in-
creasing frequency in the technical community, if
the people or their elected representatives are to
make their own decisions. There will be problems to
ensure that the pressures of this work do not cut
excessively into the scientiﬁc excellence and quality
of other essential survey programs. Vigilance will
be required to ensure a continuing buildup of the
basic geological data and derived information that
provide a survey with a springboard for any new
thrust, in any direction, arising from the events or
concerns of the day.

Before closing, I would like to add a word con-
cerning the importance of international activities.
Study and understanding of the earth is not limited
by national boundaries. It is essential that govern-
ments, through their survey organizations, work
closely together to set the standards and methods for
resource estimation. Although there is a trend to
consider such information as semiconﬁdential, it is
extremely important, in my view, that such know—

6 EARTH SCIENCE IN THE PUBLIC SERVICE

ledge be increasingly exchanged to provide a better
basis for discussions on the resource problems and
opportunities of the world.

The earth sciences and earth surveys are entering
a new era of public service. It is up to the earth
scientists and our earth-science institutions to rise
to this challenge and to show that the dreams and

aspirations of Powell and Logan were not in vain.
It is up to the national geological surveys to lead
the way by coordinating the many centers of infor-
mation now existing across the land and, by building
upon their established reputations for excellence and
objectivity, to ensure that the public receives the
information and sound policies required to meet the
new way of life that lies ahead.

EARTH SCIENCE IN THE PUBLIC SERVICE

NEW DIRECTIONS FOR ENERGY POLICY AND ANALYSIS

By JOSEPH L. FISHER
Director, Resources for the Future, Inc.

The dedication of the John Wesley Powell Federal
Building as the US. Geological Survey National
Center is an auspicious occasion for the Nation. The
U.S.G.S. has played a major role in the unfolding
history of our country: In the development of the
earth sciences; in the establishment of standards
of excellence in geologic, topographic, and hydro-
graphic data gathering, mapping, and analysis; in
the opening up of the West and Alaska and now
the offshore seas; and in the underpinning of eco-
nomic and social progress itself. In these times of
widespread disillusion with government and estab—
lished institutions of all kinds, Americans can take
heart that their Geological Survey holds ﬁrmly to
its mission of providing objective nonpolitical in-
formation of high quality about the land and water
resources on which we all depend for both life and
livelihood. This is what I mean when I say that this
is an auspicious national occasion.

I want to deal with some important problems
facing this country in energy and to suggest some
new directions for policy and analysis. Now that
last winter’s energy crisis, problem, or whatever, has
eased, we in this country must take care not to
revert to old attitudes and habits about energy. We
must take advantage of the respite to change our
consumption patterns, to try much harder to con-
serve energy, and to ﬁnd new reliable sources of
supply. None of this will be easy.

The energy future of the United States is vulner-
able. Renewed embargoes, higher costs of oil, difﬁ-
culties in preventing environmental problems, exces-
sive proﬁts for energy companies, and unrestrained
growth in demand can threaten that future. We
must do better through national policy and individ-
ual action to limit consumption and increase supply.
The objectives of low-cost energy, new and diversi-

 
ﬁed supply sources, environmental protection, com-
petition among companies, fair taxes, national see
curity, and good sustainable relations with other
countries must all be served.

The energy problems ahead are many and can be
a serious threat to the welfare of this and other na-
tions and to the peace of the world. If within the
next year the United States has not vastly improved
its energy policies for both the immediate future and
the longer range, an opportunity Will have been lost
and much trouble will lie ahead.

At this point a short quotation from Art Buchwald
is appropriate:

Three moving men walked into the ofﬁce of the
Energy Crisis and started taking down the pictures
and the graphs.

“What are you guys doing?” the Energy Crisis
asked. .

/ “We have orders to move all your stuff out. They’re
moving another crisis into this ofﬁce.”

“But I just got here,” the Energy Crisis pro-
tested.

“Don’t talk to us. We just do what they tell us.”

“Why am I being moved out of my ofﬁce?” the
Energy Crisis demanded.

“You want it straight? We don’t need you any-
more. You’re washed up. Get lost.”

Although the oil crisis in the immediate sense has
passed, the longer range outlook is full of “ifs,”
“ands,” and “buts.” If the embargo is not reinsti-
tuted, if the American people will intensify their
efforts to conserve, if research and development for
coal liquefaction or breeder reactors pays off, if
offshore drilling reveals lots of low-cost oil . . . and
environmental damages can be contained, and peace
can be maintained in the Middle East, and more re-
ﬁneries can be built . . . but will oil prices hold at

7

8 EARTH SCIENCE IN THE PUBLIC SERVICE

politically tolerable levels, but will companies accept
a reduction of their special tax advantages and still
proceed vigorously to expand supply, but will con-
sumers—industries, individuals, families—sustain
the discipline necessary to reduce their consumption
of energy, but will technology continue to provide
new practical means for converting energy raw
materials into usable heat and power? These are
only a few of the “ifs,” “ands,” and “buts” in the
American energy future.

Many observers believe that this country and the
world are passing over a major divide and entering
a new watershed in which energy will never again
be plentiful and low in cost. They believe that the
large boost in crude—oil price forced on the world in
late 1973, principally by the Arab contingent in the
Organization of Petroleum Exporting Countries
(OPEC), marked the end of the era of easy oil,
that from here on, 50- to 60-cent gasoline will be
the unpleasant fact of life, and that there will be a
continual scramble for new sources of oil and gas.
Others surveying the same scene are more optimistic.
They see higher prices weeding out unnecessary
consumption, stimulating new supply, and providing
the incentive for conservation.

Whatever one’s outlook may be, some fairly basic
decisions regarding the direction of future energy
policy and analysis seem to be at hand. Here are
some of them:

1. Market pricing—or controls. Should the US.
Government stand aside and let oil and other
other energy commodity prices rise to what-
ever level proves necessary to equate the forces
of demand and supply? Such a hands-off ap-
proach has advantages: Consumer and pro-
ducer choices would be allowed to work their
way without restriction, price and rationing
administration would be avoided, high prices
would stimulate the ﬂow of investment funds
to expand supply. Politically, however, this
approach would not be easy to live with, as
many members of Congress will testify, and it
would be hard on the low-income group. Also,
at least in the short run, higher prices would
exacerbate inﬂation.

2. Drastic alteration of the structure and function-
ing of the oil industry—pr business more or
less as usual. Large numbers of people are con-
vinced that industry, especially big oil, is
mainly responsible for the recent energy
crunch and has perpetrated a conspiracy to
raise prices by withholding supply. Others do

 
not agree with this but nevertheless think that
the oil-depletion allowance, foreign tax credit,
and other tax advantages should be eliminated
or at least reduced. Now is the time to do it,
they argue, because prices are very high and
the companies would not be hurt. In addition,
the case for breaking up the large vertically
integrated oil companies through tougher ap-
plication of antitrust laws is now being made
more vigorously than for some time. This is
urgent, so the case goes on, because oil com-
panies have been extending their activities far
into coal, uranium, and other parts of the
energy industry. Finally, support is mounting
for direct Government development and opera-
tion of commercial-scale yardstick plants to
produce shale oil, liquid or gaseous fuel from
coal, offshore oil, and nuclear power. The struc-
ture and functioning of the oil industry may
indeed be in for drastic change.

3. Extension or relaxation of environmental con-
trols. The direction of change regarding pro—
tection of the environment has been set in the
clean air and water legislation of the past few
years in response to the so-called environmental
revolution which amounted to a sudden percep-
tion of increasing pollution, congestion, and
landscape degradation. The energy-supply
crisis came in on the heels of the environmental
crisis, causing a reexamination of the air,
water, and other quality standards which had
been set, and especially the dates by which the
standards were to be reached. The National
Commission on Water Quality is a part of this
process of reexamination, as are other studies
of air-quality standards now progressing in
various places. The battle lines have been
drawn, and the outcome will hinge largely on
what happens in hundreds of speciﬁc cases for
locating powerplants, relaxing sulfur or other
discharge standards, leasing oil lands onshore
and offshore, raising electric rates, taxing in-
dustrial eﬂiuents, and enforcing regulations.

4. National self-sufﬁciency—or a world system. The
President has announced a goal of US. self—
sufﬁciency in energy by 1980. Prior to the Yom
Kippur War, this country was importing
nearly 30 percent of its crude oil, 10 percent or
so from the Middle East and North Africa.
Many regard the achievement of total self-
sufﬁciency by 1980 as impossible and undesir-
able as well. Large increases in domestic supply

NEW DIRECTIONS FOR. ENERGY POLICY AND ANALYSIS 9

of oil, they state, will take more time and will
be costly. The leadtimes for breeder reactors,
coal-conversion plants, oil-shale mining and
processing, and signiﬁcant offshore oil develop-
ment are quite long, ranging from 3 or 4 years
to 10 or 12 for single installations, let alone
whole new industries. Furthermore, national
self-suﬂ‘iciency, pursued rapidly and relent-
lessly, might upset entirely the applecart of
international relations and leave the United
States with troubles compounded in all direc—
tions. On the other hand, a countercase can be
made that Western European countries and
Japan would be better off to the degree that
the United States is self-suﬁicient in oil. There
would be less pressure on world oil prices, more
Arab oil for them, and larger U.S. domestic
production for them, as friends, to draw on
should the Persian Gulf source be shut off. The
principal opposition to US self-sufﬁciency,
however, comes from internally oriented per-
sons and agencies whose profound belief is that
problems like oil and energy are world prob-
lems and have to be met on that scale. Self—
suﬁiciency is a ﬂirtation with disaster, they
maintain, because it tears the fabric of inter-
national cooperation and peace.

5. Stability and manageableness in the international

balance of payments—or chaos. Oil selling in
the international market at $10, $12, or $15 a
barrel, when production costs range from 10
cents to $1 a barrel, when transportation costs
to almost any reﬁnery in the world are less
than $1 a barrel, and when reﬁning costs are
about the same, means huge monetary gains
for the exporting countries. Next year, the
Middle East and North African oil countries
could realize more than $50 billion—perhaps
as much as $80 billion—in proﬁts, taxes, rents,
or whatever these gains might be called. A]-
ready, very large sums in the hands of these
countries have piled up in volatile short-term
deposits and investments in US. and European
banks from which they have been loaned on a
longer term basis. The problem of sustaining
this kind of international monetary transfer
will be severe in the extreme and will call for
both national and international policies for
long—term investment of these oil funds in the
more developed oil-importing countries and in
less developed oil-poor countries. Also the situ-
ation will call for technical aid and industrial

 
capital to be furnished by the more developed
to the less developed countries. Recently I
have been advocating an ongoing World Con-
ference on Energy and Minerals Policy to cope
with these and related problems, perhaps under
United Nations’ auspices.

mation regarding energy—or privi-
secrecy. The energy situation is of
such cri ical importance for the national wel-
fare, an the state of public conﬁdence in the
energy 'ndustries is such that the proprietary
aspect f energy information should now be
largely liminated. Information from the en-
ergy in ustry on reserves, production, ship-
ments, processing, sales, prices, costs, and
proﬁts om now on should be reported to the
Govern ent and made public. The only excep-
tion sho Id be in instances clearly and directly
affectin military security. The major change
being s ggested is for revealing information
on rese ves; most of the other information is
already made public. This, of course, would
raise th hackles in the industry and would
constitu e a sharp change from past practice.
Howeve , because all major and substantial
compani s would be treated alike, no one of
them co- 1d easily claim that it would suffer any
serious isadvantage because the information
reporter is made public. The retention of some,
perhaps much, information in a conﬁdential
or secre status inevitably will lead to doubts
and app ehensions on the part of many people
and wou d mean that many companies will con-
tinue to be in the unenviable position in which
the tru hfulness of what they say will be
doubted.

Sever 1 reasons for this position are impor-
tant. Fi st, the country remains in a serious
energy ind which will take some years to
loosen. he hard job of increasing supplies,
especiall of oil and gas, will take a number
of years to complete, as will the job of estab-
lishing abits of greater conservation. In this
situatio and with this outlook, Government
leadersh p is imperative and cannot be exer-
cized eff ctively except on the basis of the most
, systematic, and prompt information
that can be obtained. Second, the information
should b kept open and available for public in-
spection. There is no other way of convincing
people t at games are not being played with the
vital public interest. Without full disclosure of

 
10

EARTH SCIENCE IN

information, the widely held belief that some
kind of rip-off is going on will not be dispelled.
Third, it is unrealistic to expect public support
for spending more than $2 billion a year on oil
exploration, development, and research gener-
ally, much of it for new sources and technolo—
gies, if knowledge of known sources and exist-
ing technologies is kept locked up in company
ﬁles.

7. Sustained, long-term, and large research and de-

velopment programs—or sporadic hit-or-miss
efforts. There can be only one answer to this
choice, of course. The problems are how to or-
ganize for it, at what scale to carry it on, and
how to deﬁne priorities and sequences. At pres-
ent, energy research and development in the
Federal Government is widely scattered among
many agencies—the Atomic Energy Commis—
sion, the Ofﬁce of Coal Research, and many
others. Each has its own mission, legislative
authority, funding, style, and constituency. N o—
where is the whole set of research and develop-
ment activities brought together, ordered, co-
ordinated, and made to serve deliberately chos-
en national objectives in an economically and
sustainable way. Two billion dollars or more a
year for energy research and development is
too much to spend in a relatively unorganized
way. The heavy emphasis of recent years on
conventional and breeder nuclear energy now
needs to be reexamined and placed in a larger
context of research and development on conver-
sion of coal to liquid and gaseous fuel, develop-
ment of oil shale and tar sand, offshore explora-
tion, solar energy, geothermal energy, and nu-
clear fusion. Technology for some of these
processes has already been proved; other
processes are nowhere near ready for commer—
cial use. All of them must be brought together
in a long-range program designed to meet an-
ticipated needs. Research on environmental
protection is equally urgent, as is research on
conservation of energy materials and improve-
ments in the efficiency of mining, conversion,
use, and reclamation. All logic points toward a
special, probably new, agency for energy re-
search and development.

8. Major changes in life styles—or not. Many im-

portant and sensitive groups in this country—
many young people, for example—argue and in
various ways demonstrate for a more simple
style of living and less consumption of energy

THE PUBLIC SERVICE

and energy-using vehicles and products.
Whether this devotion will be sustained into
middle age against the lure of creature com-
forts and the easy mobility of the auto remains
to be seen, but the challenge is serious and the
option may well be viable. High energy prices
make it attractive, as do its environmental ad-
vantages. The typical American uses 40 to 50
times as much energy as most Asians and Afri-
cans. People in Europe, Japan, and some other
countries enjoy quite good standards of living,
in many respects better standards than Ameri-
cans do, on half as much energy per capita.
Prudence points in the direction of a life style
requiring less energy, certainly in the direction
of conservation and more efficient use of ener-
gy; however, many still regard it as sensible
not to reduce consumption or to save on things
unless one absolutely has to.

9. New policy-making agencies and processes—or
muddle along with what we have. Debate on
how to instrument changes in energy policy and
programs is hot at this time, in Congress and
elsewhere. Most would agree that the Federal
Government, and the States and local govern-
ments also, need to pull their boots up, reorgan-
ize some, and do a better job in energy. At the
Federal level, a statutory energy administra-
tion has recently been established. A separate
agency for research and development, a new
Department of Energy and Natural Resources,
better coordinating arrangements, and, on the
Congressional side, a Joint Energy Committee
have been proposed and have merit. Doing
nothing, or not much, to improve policies and
programs would seem to be a failure of political
leadership, which in the face of new and severe
problems, the country should not tolerate. The
traditional dispersal of energy responsibilities
and the resulting poor performance has got to
go, as almost everyone would agree. The ques—
tion is exactly what changes should be made
and how the tasks and responsibilities should
be assigned so that decisions on new policy di-
rections can be translated promptly, smoothly,
and fairly into action.

These are some of the major issues in energy that
will have to be worked out if the needs of people in
this country are to be met in the coming years. The
answers are not easy because the problems are com-
plex. My own preferences for policy may have been
revealed somewhat in my presentation of the main

 
NEW DIRECTIONS FOR ENERGY POLICY AND ANALYSIS 11

issues. They are for a readiness to guide, and if
necessary to control selectively and temporarily, the
operation of the market in establishing energy prices
in these times of rapid inﬂation; for reduction in
certain tax advantages of oil companies; for stout
adherence to improving environmental conditions
with a minimum of compromises and delays; for a
decisive though limited movement in self-sufﬁciency
to lessen the insecurity of too great dependence on
uncertain overseas sources of oil; for retaining an
international trading and investing system in oil and
other energy commodities; for some fairly major
changes in life style; and for organizational changes
in government to promote an integration of energy
policies and programs.

My preferences for policy, or those of anyone, will
be no better than the facts, the research, and the
analysis that underlie them. The Geological Survey is
forever extending the facts and improving the re
search and analysis. Increasing attention in recent
years has been given to offshore geology, to environ-
mental aspects of mining and water development, and
to satellite and other remote-sensing devices. Eco—
nomic analysis has been strengthened; as an econo-
mist myself, I would hope that this could be enlarged
still more. The Survey might well aim to develop as
much expertise in appraising needs and requirements
for energy and other materials as it has long had in
appraising reserves. It could to advantage probe
deeply into the changing structure of demand for the
various energy sources as these are utilized in indus-
try, transportation, space heating and cooling, and
electric-power production. The role of prices should
also be considered, and various international factors
should be taken into account. A systematic and com-
prehensive framework of demand and supply esti-
mates, looking ahead to both the short range and the
long range, should be the goal. Such a framework,
reworked periodically, will reveal many clues as to
the priorities of research and analysis on new sources
of supply and new technology. Other agencies of gov-
ernment can help in this work, but I am urging the
US Geological Survey to take the lead. It would be

 
a new and exciting enterprise.

The other decisions about energy outlined earlier
also call for more study than has been given to them
thus far. Much more needs to be known about the
structure and behavior of the energy industries, the
response of both industries and people to environ-
mental controls, the world implications of greater
self-suﬂ’iciency in energy on the part of the United
States, the ramiﬁcations of the balance of payments
problems arising out of the much higher price of oil,
and the likely effects of higher prices on consump-
tion, new technology, and exploration for new sources
of supply. The agenda of future research on energy
is a long one, full of interest and excitement.

The Government’s role in energy, which involves
not only the Geological Survey but all agencies con-
cerned with energy, is likely to become more im-
portant and, I believe, should become so. It will have
to establish the broad objectives—low cost and de-
pendable supply, environmental protection, national
security, employment—and some degree of consensus
as to trade-offs among these objectives. It will have
to provide incentives for appropriate private initia-
tives and itself perform certain functions. It will
have to furnish much more basic information about
energy resources, likely future requirements, costs,
new technology, environmental impacts, and ways to
conserve supplies and increase efﬁciency in extrac-
tion, processing, and use. And here again is where
the Geological Survey comes in.

Even though an Energy Research and Develop-
ment Agency may soon be established to pull together
the more applied programs, the U.S.G.S. will still
have to be relied on for much of the basic informa-
tion and appraisals within which subsequent re-
search and development will take place. The higher
the structure, the more necessary that the founda-
tion be deep and ﬁrm. The American people have
come to expect excellence from the Geological Survey.
This new building, this National Center, especially
the people here who will do the work, can be trusted
to continue this tradition and to improve on it.

EARTH SCIENCE IN THE PUBLIC SERVICE

MINERAL-RESOURCE APPRAISAL AND ANALYSIS

By JOHN DREW RIDGE
Head, Department of Mineral Economics, Pennsylvania State University

“. . . There are only a limited number of places left
to search for most minerals. Geologists disagree
about the prospects for ﬁnding large, new rich ore
deposits. Reliance on such discoveries would seem
unwise in the long term” (The Limits to Growth, the
Club of Home Report, 1972, p. 55).

This less-than-optimistic attitude of the authors of
the Club of Rome report indicates, if nothing else,
that mineral raw materials are so important to the
continued industrial life of this Nation that we must
obtain the best possible understanding of the quanti-
ties of such materials in our subsoil. Although the
United States almost certainly can never again be-
come essentially self-sufﬁcient in metallic raw ma.-
terials, we would be foolhardy not to try to ﬁnd all
deposits of them that exist within our borders.

Most present exploration for mineral raw materi—
als is carried out by examining what the prospecting
organization considers to be the geologically most
favorable areas available to it. Such areas are either
(1) districts in which workable ore deposits have
been found previously, the most favorable sites being
those whose geology is decidedly similar to those in
which ore bodies have occurred; or (2) districts that
do not contain known ore bodies, but that have geolo~
gy much like that of areas that do. Examples of (2)
are provided by the recent ﬁnding of the zinc deposits
of central Tennessee or those of the new lead belt in
Missouri. Examples of (1) are furnished by the dis-
covery of the Kalamazoo ore body at San Manuel or
by the several deposits found around the rim of the
Sudbury basin since the end of World War II.

In an area in which ore deposits have previously
been found, some considerable information is known
on the surface geology. In addition, data are avail-
able on the subsurface geology because both drilling
and mining, as well as surface work, have been car-

12

 
ried out. This subsurface geology will not, of course,
be as well known to a company that does not own one
of the ore bodies already being exploited in the dis-
trict as to one that does. The ﬁrst company will, how-
ever, have acquired, in one way or another, more
knowledge of the character of the rocks in the sub-
surface than it would of any area that has not been
drilled and mined. Such an undrilled and unmined
area may, however, have been mapped and perhaps
examined by surface geochemical and geophysical
studies. To some extent, the surface mapping and
the geophysical work will have provided some in-
sights into the character of the subsurface geology,
but, at best, the inferences drawn from this work are
not applicable more than a few hundred feet beneath
the surface. What can be assumed from surface geo-
chemical work provides even less penetration be-
neath the surface.

In any area in which the information derived from
the surface is encouraging, the mining company ex-
amining the area will lay out a drilling program to
provide knowledge of the subsurface. The drilling
will be continued for as long as the results suggest
that ore has been found or may be found. As soon as
the balance of (usually subjective) probabilities
ceases to favor the discovery of ore, drilling will be
stopped, and exploration will be started in the next
(potentially) most favorable area. This method pro-
vides a continuously increasing amount of geologic
information, but if this information is not deposited
in a single repository, it is not readily available to
any but the company that acquired it. Thus, as a
means of providing a broad survey of what ore might
be available in the United States, exploration by indi-
vidual companies or groups of companies leaves
much to be desired.

If a broad survey is to be achieved, several things

MINERAL-RESOURCE APPRAISAL AND ANALYSIS 13

must be done. The ﬁrst of these is to continue, ac-
celerate, and reﬁne the surface mapping done by the
US. Geological Survey, so that much more of the
Nation is covered by geologically mapped quad—
rangles than is now the case. The second is for the
Survey to continue and expand surface geochemical
and geophysical work. The third is for the Federal
Government to require that the results of geological,
geochemical, and geophysical work done by private
ﬁrms on Federal lands must be deposited With the
Survey and that the Survey integrate this work with
their own results. The fourth, and most important
step, however, is that we obtain systematically a
much greater knowledge of What lies beneath the
surface than can be provided by the ﬁrst three meth-
ods of geological information gathering that have
just been mentioned. Such knowledge of the rocks at
depth can be produced best by drilling on a large
scale, the holes being taken down at least 3 miles
beneath the surface.

This drilling can be done in two ways. The ﬁrst is
to drill areas thought (again mainly subjectively) to
be geologically favorable, starting with what are con-
sidered to be the most promising, and working out-
ward into surrounding ones that show less favorable
surface indications of ore beneath. This approach has
the advantage of making maximum use of what is
known of surface geology, but it conﬁnes the pros-
pector to rocks and rock relations he already knows
to be associated with ore bodies. It provides no basis
for bold strides into the unknown. The second ap-
proach is based on the premise that much ore lies
below the 1,000-f00t outer skin of the crust that we
know something about by surface mapping, geo-
chemistry, and geophysics. To check the value of this
premise, it is necessary to prospect by drilling a
regularly spaced series of holes throughout the
United States. The only areas not to be drilled would
be those now used in such a way that they cannot
possibly be proﬁtably subjected to mining operations
even if they were to overlie large ore deposits.1 If a
second Rand were found beneath Manhattan Island,
it would not be good economics to convert that island
into a mining camp. Much of the area of the United
States, however, is so used at present that a large
mine would be more proﬁtable than whatever is being
done on that part of the surface today.

We will never know What underlies the entire sur-
face of the United States unless we look, and regu-
larly spaced drilling provides the only systematic
method today for such explorations. It can be con-
vincingly argued that so much. recoverable mineral

 
and fuel material would be found by such drilling
(Griﬂ‘iths, 1967) that the cost would be repaid many
times over. Griﬁiths (1967 ; Grifﬁths and Singer,
1970) has suggested that such drilling be carried out
on a grid pattern, the holes being spaced at 20-mile
intervals and each hole carried to a depth of 3 miles.
This program would require some 7,500 holes and
would cost about $3 billion.

Grifﬁths has pointed out that if ﬁve circular or el-
liptical targets, 28 miles across (the approximate
size of major oil ﬁelds in the United States), remain
undiscovered in this country, they would be found
with certainty by this drilling method. Smaller but
still large targets, such as major porphyry copper
deposits, would be less probably discovered directly,
but enough indications would appear in the holes to
justify further exploration by a more closely spaced
grid. Griffiths has assumed that the mineral raw ma-
terials found in this country to date constitute a ran-
dom sample of the outer 3 miles of the crust of the
contiguous 48 States. This justiﬁes the conclusion
that, if the entire 3 million square miles of the 48
States were tested, the area would be large enough
and mineral-rich enough for a commercial success to
be assured for the drilling program under a wide
variety of boundary conditions.

Using 1966 data, Griﬂiths estimated the average
value of mineral raw materials recovered from the
surface and subsurface mineral deposits in the con-
terminous United States. Allowing for the recovery
of mineral materials since that date, this average
value is now about $250,000 per square mile. The fre-
quency distribution of dollar value per square mile
for the 48 States is lognormal, having a mean value
of about $150,000. The variation from the average is
considerable; the value per square mile in Oregon is
less than $16,000 and that in Pennsylvania is more
than $1,800,000. These data do not mean, of course,
that each area of 400 square miles in which each drill
hole is centered will contain $100 million of recover-
able raw materials, but Grifﬁths’ calculations show
that each 400 square miles would, on the average,
contain that dollar value of raw materials. Thus, the
entire 3 million square miles of the United States, to
a depth of 3 miles, should hold $750 billion of recov-
erable raw materials. The best approach to making
sure that all such materials are found seems to be
grid drilling.

 
1It should be obvious that such a program of exploration cannot be
carried out for minerals alone. It must be designed to look for anything of
value within the crust of the Earth. Thus, to attempt to make separate
appraisals for oil and gas and for solid minerals is economically and
geologically unsound.

14 EARTH SCIENCE IN THE PUBLIC SERVICE

The usefulness of the drilling program would be
apparent long before it had been ﬁnished, because the
information available from any sizable drilled area
could be analyzed immediately and made the basis for
secondary exploration efforts.

It probably would be advisable to ﬁt the primary
20-mile grid to the area of the United States so that,
although the drilling would still be done on regularly
spaced centers, the holes would miss as many of the
known major areas of mineral raw material concen-
tration (solid, liquid, or gaseous) as possible. This
modiﬁcation of Grifﬁths’ concept may be somewhat
less than mathematically sound and must be thor-
oughly tested to make certain that it does not intro-
duce an unacceptable bias into the drilling scheme. In
favor of such a nonrandom ﬁtting of the grid is the
fact that probably less new data would come from a
hole through the rocks of the Butte copper district or
those of the East Texas oil ﬁeld than through those
of areas less well known geologically.

Probably only by some version of Grifﬁths’ scheme
will it be possible really to understand the ore geolo-
gy of the United States and to be certain that all
deposits of mineral and fuel materials in the outer
3 miles of the crust of this country would be found.
Such an approach would be a radical departure from
the system of exploration now practiced, but it
should discover the ore potential of the entire coun-
try much more rapidly than do present exploration
methods.

Another mathematically based approach has been
developed by Harris and his coworkers (1966, 1969,
1973; unpub. data). His methods, described brieﬂy
below, are designed to aid in the determination of
areas favorable to ore occurrence through quantify-
ing objective and subjective geologic and economic
variables and analyzing these mathematically. He
deals, however, with areas in which ore already has
been found or with areas whose geology is similar to
that in which major ore deposits have been
discovered.

In the ﬁrst study in this series, Harris (1966) has
suggested how to construct an objective model that
will associate probability of occurrence of some
measure of mineral wealth with the reconnaissance
geology of each subdivision (cell) of the area in ques-
tion. The model he developed has determined that
geologic variables can be related mathematically to
the probability of the occurrence of mineral wealth.
His quantiﬁcation of the geologic variables of a
geologically known ore-containing area in Arizona
and New Mexico in counts, percentages, and lengths
produced the values necessary to test his model. He

 
found that multiple discriminant analysis and classi-
ﬁcation analysis by Bayesian statistics and multi-
variate probability constitute a two-phase probabili-
ty model that associates probabilities with geologic
data and mineral wealth. On the basis of the success—
ful test of the model in the area studied, Harris con-
cluded that geologic data on a known ore-bearing
area can be used to guide exploration in an unknown
area of generally similar geologic characteristics.

In his paper with Euresty (1969), Harris reﬁned
his model to go beyond the assessing, through the
quantiﬁcation of geologic variables of expected gross
value of resources to the adjustment of gross value
through the consideration of economic factors. The
approach means that the geologically determined
gross value of a given cell is modiﬁed in terms of its
location relative to existing markets and transporta-
tion networks at a given time. This method, there-
fore, may indicate that a geologically less favorable
area may have advantages of place at a given time
that make it a better area for exploration than one
with more encouraging geologic characteristics.

Still further studies by Harris, in collaboration
with Brock, Donald, and Euresty (Harris, 1973; un-
pub. data), have advanced models that also include
subjectively determined variables. The subjective
material is obtained from estimates by geologists
knowledgeable in the area under study as to the
probabilities of the occurrence of ore in regularly or
randomly arranged cells.

These methods are designed to work from known
to less well known but geologically similar areas
and are conﬁned in their scope by this approach.
They provide, nevertheless, excellent supplements to
the study of areas in which only the surface geology
is known. Further, they can be adapted to the inte-
gration of the geology determined by Griﬂ‘iths’ grid
drilling with what surface geology is known in each
drill-hole area.

It is, of course, apparent that such a huge number
of holes to such considerable depths (as Grifﬁths’
method would require) would not be within the ﬁnan-
cial resources of any one mining or petroleum com-
pany or even of a consortium of them. Thus, it seems
obvious that, as the program here outlined must be
planned and executed as a unit, it must be carried out
by the Federal Government, through the agency of
the US Geological Survey. The results must be made
public property as soon as a sufﬁcient number of
holes to give signiﬁcant geologic results have been
drilled in any one major part of the continental area
of the United States. Once any major segment of the
drilling has been completed, the data from that and

MINERAL-RESOURCE APPRAISAL AND ANALYSIS 15

all other sources should be analyzed, probably by the
Survey’s Computer Resources Information Bank
(CRIB), supplemented by models of the Harris type.
Then, appropriate areas should be offered for lease to
mining companies for further and more detailed ex-
ploration in somewhat the same manner that areas
are offered for lease in the potentially oil- and gas-
bearing regions of the Continental Shelf. For such a
program to operate eﬂiciently, the areas offered for
lease would have to be large enough to contain possi-
ble worthwhile targets and yet not so large that they
would be too expensive for any one company to ex-
plore in the time allowed before all interest in the
leased area would have to be given up. Areas already
being actively prospected by companies or consortia
would not be offered for lease to other mining organi-
zations, but safeguards would have to be established
to make certain that areas claimed to be under an
active program of prospecting actually were being
so studied. For this program to function properly, it
probably would be necessary for the US. Govern-
ment to take over all mineral rights to all land in the
Nation (except areas being actively mined or pros-
pected) under its power of eminent domain. At the
same time, the Government would have to guarantee
to the owner of the surface rights, adequate com-
pensation for any damages done to the surface, and
to the owner of the mineral rights, royalties for any
material that might be removed from the ground in
any manner. Legal arrangements would have to be
made to insure that surface damage and environ-
mental impact were held to a minimum and that the
surface of the land ultimately would be restored to
usable conditions, whether or not the exact contours
of the original surface were actually duplicated.
Drilling would be a waste of time and money if it
were done in centers of considerable population or
industrial activity, but with such advances in tech-
nology as solution mining, much more of the sub-
surface could probably be mined than would at ﬁrst
seem possible. The amount of surface and environ-
mental damage caused by the recovery of oil is less
great than that caused by mining, but whatever the
exploiting process, all surface areas would have to be
restored.

For any tract leased, a time limit would have to be
placed on exploration, with provisos that part of each
tract be relinquished by the private exploration or-
ganization at regular time intervals so that, at the
end of a period of perhaps 6 to 8 years, the exploring
group would be left with one-quarter of the original
tract, which it must either exploit or drop after a
further period, perhaps 2 or 3 years. The prospector-

 
discoverer would have the right, against all other
persons, to obtain the mining rights to the ﬁnal re-
maining fraction of his exploratory lease, but he
would not be obligated in any way to establish a
mine in the area unless he wished to do so. If the
prospector-discoverer and the owner of the mineral
rights, whether a private person or the Federal or a
State Government, were unable to reach agreement
on the payments to be made for the mining rights,
either party could appeal to a speciﬁcally created
Government judicial or quasi-judicial body to decide
what recompense the owner of these rights should
receive.

Although the granting of rights to mine and to
prospect would limit the rights of the individual
property owner, the owner would not lose his proper-
ty permanently, as he does when the Federal Govern-
ment expropriates property for such uses as roads
and public buildings. Therefore, under the right of
eminent domain, the Government would probably
ﬁnd it constitutionally possible to enact such legisla-
tion as I have outlined to encourage exploration and
the exploitation of the Nation’s natural resources.

All geological, geophysical, and geochemical infor-
mation obtained in the course of exploration and min-
ing of leased tracts would have to be made available
to the appropriate agency of the Federal Government
(the US. Geological Survey). Further, the Federal
Government would be able, after a stipulated lapse of
time, to make public this information in connection
with other requests for bids for exploration rights to
parts of the original lease not retained by the original
leasee.

It should be emphasized that the information de-
rived from the grid drilling is to be integrated With
known surface geology and that the mapping and
geophysical and geochemical work of the Survey
should build on and expand the data provided by
drilling. Thus, the Survey’s surface programs proba-
bly would be concentrated around those holes that
gave the greatest indications of valuable mineral raw
materials at depth (solid, liquid, or gaseous), thereby
helping to add more rapidly to the workable mineral
reserves of the Nation.

It might be argued that the assignments of rights
to prospect would be on sounder legal grounds if they
were granted under the auspices of the several
States. The confusion that would result from 50
different controlling sets of laws and governing
bodies might be obviated by the preparation of a
model statute for such control and its adoption by
the 50 States. However, areas geologically suitable
for exploration may well overlap State boundaries,

16 EARTH SCIENCE IN THE PUBLIC SERVICE

and, even if the same laws were applicable in the two
or more States involved, the obtaining of a geo-
logically viable concession would be complicated by
the need to consult, negotiate with, and report to, at
least two administrative bodies and to comply with
the requirements of no less than two sets of inspec-
tors. Nor would the information obtained by work in
more than one State be as easily collated and dis-
tributed as it would be if a single Federal agency
(the US. Geological Survey) were to control the
granting and operation of prospecting concessions.

Tax laws would have to be altered to permit ex-
ploration costs to be deducted as current expenses by
the exploring organization. Further, these laws
should allow any actual exploitation, perhaps by a
reduced depletion allowance, to be carried out a
fraction more proﬁtably than if the sums spent in
exploration and exploitation had been invested in
any average type of economic activity within this
country. No company, consortium, or individual, is
going to invest money in petroleum or mineral ex-
traction for fun. Such work is done in the hope of
making a proﬁt. There are sound arguments for con—
sidering mining or petroleum recovery as a more
hazardous way of investing funds than in, say, the
making of shoes or the manufacture of ﬂour. There-
fore, a somewhat higher rate of return must be al-
lowed the exploiting organization either through tax
concessions or higher prices. This remains true
despite the current agitation against “windfall”
proﬁts. If the ﬁrst method is adopted, the cost of sup-
plying minerals or fuels from our subsoil would be
borne by the general public. In the second, the actual
consumers of the materials so produced would bear
the cost. Because of the widespread use of minerals
and fuels or of the products made from them, either
method would bear about equally on the average
consumer.

Much of the mineral-bearing rock found by, or
with the help of, grid drilling might not at present
be exploitable competitively with ore bodies now be-
ing mined, here or abroad. As world requirements
grow and technology advances, however, more and
more of the mineral material so discovered will come

 
to be proﬁtably mineable. Thus, returns will be
achieved from the information developed by the grid
drilling pro-gram far into the future.

The program here suggested is not designed to be
a gigantic boondoggle but to be an economically
sound method of achieving complete knowledge and
recovery of the mineral and fuel resources that are
available within the continental limits of the United
States. Such a system could also be applied to Alaska,
or to any major area of the world for that matter,
with equal opportunities for success.

It is readily apparent that the scheme just out-
lined to promote prospecting and exploitation of min-
eral resources in the United States would have to be
developed in much greater detail than I have pre
sented here. If this program is to be implemented
effectively, it must consider not only exploration and
exploitation but also the protection of society in gen-
eral against the ill effects of such activities. Careful
and sound planning of these discovery and recovery
operations, however, should reasonably balance the
good and ill effects of the ﬁnding and the removing
of mineral raw materials concentrated beneath the
surface.

REFERENCES CITED

Grifﬁths, J. C., 1967, Mathematical exploration strategy and
decisionmaking, in Origin of oil; geology and geophysics
—World Petroleum Cong, 7th, Mexico, 1967, Proc., V.
2: London, Elsevier Pub. Co., p. 599—604.

Grifﬁths, J. C., and Singer, D. A., 1971, Unit regional value
of non-renewable natural resources as a measure of po-
tential for development of large regions: Geol. Soc.
Australia Spec. Pub. 3, p. 227—238.

Harris, D. P., 1966, A probability model of mineral wealth:
Soc. Mining Engineers (A.I.M.E.) Trans, v. 235, no.
2, p. 199—216.

1973, A subjective probability appraisal of metal
endowment of northern Sonora, Mexico: Econ. Geology,
v. 68, p. 222—242; Discussion, p. 1345—1346.

Harris, D. P., and Euresty, D., 1969, A preliminary model
for the economic appraisal of regional resources and
exploration based upon geostatistical analysis and com-
puter simulation: Colorado School Mines Quart, v. 64,
no. 3, p. 71—98.

Ridge, J. D., 1968, Exploration for minerals on non-federal
lands: Earth and Mineral Sci., v. 39, no. 2, p. 19, no. 3,
p. 27-28.

 
EARTH SCIENCE IN THE PUBLIC SERVICE

CRISIS AND CATASTROPHE IN WATER—RESOURCES POLICY

By M. GORDON WOLMAN
Chairman, Department of Geography and Environmental Engineering,
Johns Hopkins University

“A good rain is the only quick solution to the prob-
lem of drought . . . Unfortunately a good rain washes
away more than the drought; it washes away much
of man’s interest in providing for the next one, and
it washes the supports from under those who know
that another dry cycle is coming and who urge their
fellows to make ready for it.” In these words, Walter
Prescott Webb (1954, p. V), the Texas historian,
enumerated one principle of the politics of water. So
stated, the principle relates to natural phenomena.
It is, in fact, a corollary of the political scientist’s
observation that issues in politics are accidental and
evanescent, not planned and long lived.

In contrast to these views, many a scientist and
engineer hopes for a more orderly approach to policy.
Thus, an engineer discussing Federal water policies
in the 1930’s expressed the hope “. . . that the poli-
ticians and planners eventually will be guided more
and more by fact-ﬁnding and hydrologic research
than by politics and social philosophy . . . national
water policy, in regard to both practice and planning,
should be based upon economic and engineering
facts . . .” (Guy, 1943, p. 312). Although perhaps few
today would publicly propound sentiments that as-
sume such a neutral, or value-free, role of science and
technology in society, Don K. Price (1954, p. v), in
his book on government and science, “. . . was struck
by the way in which a professional consensus, based
on the ﬁndings of research of a scientiﬁc or semi-
scientiﬁc nature, often brought about the adoption of
a new public policy and determined the methods of
its administration.”

At the dedication of a building bearing the name
of John Wesley Powell, a brief historical review of
some approaches to the problems of water resources
in the United States, which keeps these conﬂicting

 
models of chance and planned action in mind, may
be useful. These two models are not, of course, the
only ones that have been used to explain government
expenditures for public works or research. This re-
view emphasizes trends in water quality and quan—
tity and some broad social and economic trends; it
neglects an analysis of bureaucratic behavior, which
some analysts have suggested is the major determi-
nant of budgetary decisions (Wildavsky, 1964).
Such a bureaucracy hypothesis is drawn upon in
relating the historical ﬁndings to possible orienta—
tions of future programs in water quantity and
quality.

SOME GENERAL TRENDS

Since 1860, trends in population, gross national
product, expenditures for public works for water
supply, sewerage, and ﬂood control, and for water-
resources investigations and stream-gaging stations
have been roughly parallel in the United States. Even
the value of damages from ﬂoods has risen con-
sistently, along with expenditures for ﬂood control.
As the country has grown, so too has interest and
activity in water resources. Growth has generally
been continuous, although each activity shows m0-
mentary periods of acceleration or deceleration such
as the reduction in economic and population growth
in the 1930’s, a time when expenditures for water-
resources investigations increased threefold. Since
World War II, the rate of increase in expenditures
has followed the growth of the economy, except dur-
ing the decade 1955—65, the post-Sputnik era, when
total expenditures for water-resources investiga-
tions rose sharply from about $30 per million dollars
of gross national product to the current rate of
about $60 per million.

17

18 EARTH SCIENCE IN THE PUBLIC SERVICE

This graphical view of history suggests that con-
tinuity, if not planning, characterizes the develop-
ment of society and the concomitant development of
planning and execution of water-resources programs.
A broad brush and moving averages do demonstrate
continuity, but they also mask or belie other facets of
the record. Upon closer inspection, as many observers
have noted, one can discern distinctive eras and
cycles, as well as isolated moments when public inter-
est in water quantity and quality was stimulated by
natural events and political or social crises.

MAJOR INFLUENCES IN WATER-RESOURCES
HISTORY IN THE UNITED STATES

Only some highlights in a well-known history, in-
cluding legislation, engineering structures, inﬂuen-
tial literary works, and scientiﬁc studies, will be
touched upon here. Beginning with the Powell era,
a chronology of signiﬁcant events in water-resources
history would start with the passage of the Home-
stead Act in 1862. That act did not represent the
start of public interest in the development of the
West, but it did initiate a boom in westward migra-
tion and land settlement, one of several in the
period from the Civil War to the closure of the pub-
lic domain. This western orientation can be charac—
terized not only by the Homestead Act but by a
variety of familiar milestones such as the Timber
Culture Act (1873), the Desert Land Act (1877),
the establishment of the Reclamation Service (1902) ,
and the diversion of water from the Colorado River
to the Imperial Valley in 1901. Of special interest
here was the publication in 1878 of Powell’s “Report
on the Lands of the Arid Region of the United
States.”

A second period overlapping the ﬁrst and continu—
ing a strong western ﬂavor includes the conservation
era of Teddy Roosevelt, characterized by the 1908
Conservation Conference or the earlier White House
Conference. Although the act establishing Yellow-
stone Park in 1872 represented a milestone in the
concept of preservation, in general, the turn of the
century conservation movement spearheaded by civil
servants such as Pinchot, McGee, Leith, and Newell,
emphasized “wise use” or the “gospel of efﬁciency,”
as the historian Hays (1959) referred to it, and not
preservation.

Depression and the initiation of public works and
planning characterized the 1930’s, a period reviewed
by W. G. Hoyt (1943) , a principal engineer-hydrolo—
gist of the US Geological Survey. Hoyt noted that
during the 1930’s, natural catastrophies, ﬂoods and
droughts, occurred during a period of major eco—

 
nomic upheaval and changing political philosophy.
The combination produced the greatest surge in in-
terest in environment and in expenditures for water-
resources planning and development that the country
has experienced. Although the economy as a whole
dipped, water science and development, along with
land management, burgeoned.

The period of rapid economic and population
growth since the end of World War II has seen both
a resurgence of development after the wartime hi-
atus, and the recent environmental movement. Much
of this recent interest has emphasized, at least vocal-
ly, the “Spaceship Earth,” or the ﬁnite nature of the
world’s resources, and hence conservation with
greater emphasis upon preservation as opposed to
development. However, expenditures for major water
programs and for investigations have risen roughly
with the economy during the same period.

This simple sequential history is known by, or at
least taught to, every American schoolchild. Its re-
curring themes or near-cyclical character are cur-
rently played down by some, perhaps in the mis-
guided view that such a recounting will tend to con-
ﬁrm the notion that “history repeats itself,” or that
such a View of our history leads to cynicism. For bet-
ter or for worse, still closer inspection begins to
reveal singular episodes superimposed on these broad
eras and continuing growth.

WATER QUANTITY

In 1888, Powell was directed by the Congress to
establish the Irrigation Survey. This reﬂected a
growing recognition that development of the more
arid parts of the West would depend heavily upon
the availability of water. Powell, as his 1878 report
described, felt strongly that settlers should not be
encouraged to settle on lands that could not be pro
vided With adequate quantities of water. He believed
further that land should be parceled out in larger
units and in such a fashion that settlements could be
clustered and water made available to assure each
settler a sufficient share. Powell’s approach allied
science directly with public policy. The hydrographic
survey was to develop the facts for proper distribu-
tion of water and planning of land settlement, and to
do so rapidly and accurately to the satisfaction of
Congress and the engineers. Neither, in fact, was
satisﬁed.

Congress became increasingly disturbed that set-
tlement would have to be delayed or prohibited in
areas that the hydrographic studies showed were too
dry or for which information was not forthcoming.
Engineers considered the accompanying topographic

CRISIS AND CATASTROPHE IN WATER-RESOURCES POLICY 19

survey misdirected and too general. The Irrigation
Survey itself was abolished 2 years after its incep-
tion. The setback represented the demise of Powell’s
dominance in Federal science and in his relationship
with the Congress (Manning, 1967) . Although many
today disagree with some of his speciﬁc suggestions
for land settlement, virtually no one denies the pro-
phetic insights in his report on the arid lands. Vision
and public interest coincided for only a brief mo-
ment. Yet, although Powell’s policy views and the
speciﬁc agency program may have been eclipsed, the
Reclamation Service was established 12 years later,
and the work was continued by the same individuals
involved in the hydrographic measurements of the
earlier Irrigation Survey.

Subsequent history is replete with examples of
social action precipitated (no pun intended) by the
vagaries of nature. The Johnstown Flood (1889)
initiated the ﬁrst legislation on the safety of dams.
The ﬂood of 1913 on the Miami River in Ohio not
only sparked the creation of the Miami Conservancy
District in 1914 but initiated the classic technical
studies of hydrology and hydraulics embodied in its
reports. Creation of the Conservancy District and
advances in science and engineering represented a
rare instance when a man and a moment combined
to advance a prophetic future. Arthur E. Morgan
(1951), a man of vision, guiding genius behind the
Miami Conservancy District (and later a leader in
the development of the Tennessee Valley Authority),
capitalized on peaks of public interest stimulated by
natural and manmade calamity.

The ﬂood of 1927 on the Mississippi River stimu—
lated initiation of the “308 Reports” of the US.
Army Corps of Engineers. The Ohio and Mississippi
River ﬂoods of 1936 and 1937 and the ﬂoods of 1936
and 1938 on the Connecticut and other rivers in New
England led directly to the ﬂood control acts of 1936
and 1938 and to the initiation of construction of dams
and reservoirs. Floods and drought in the 1930’s pro—
vided the ideal stimulus for the maintenance of pub-
lic and political interest in land and water. As Hoyt
noted, expansion of the work of the Corps of Engi-
neers, creation of the TVA, the Soil Conservation
Service, the Fish and Wildlife Service, and the Na-
tional Resources Board (1934) (later the National
Resources Planning Board) and its Water Resources
Committee were derived from the combination of
depression, political upheaval, and natural catastro-
phe. This combination promoted huge expenditures,
not only for land and water management but also for
the science and technology needed to support these
efforts. Once again, however, as in Powell’s day,

 
Congress decided that too much planning might be a
bad thing, and in 1943, the National Resources Plan-
ning Board was abolished with the provision that no
other agency pursue the work.

The recent coming-of-age of ﬂood insurance and
alternatives other than structural measures to reduce
ﬂood damages suggests an interesting effect of catas-
trophe falling upon the “prepared mind.” In 1942,
Gilbert White observed that many alternatives to
structural measures might be useful in mitigating
ﬂood damage. In the intervening years, White and
others amassed information on the effects of ﬂooding
and on the experience in using these alternatives.
More than a decade later, a ﬂood insurance act was
passed, and this year, three decades later, congres-
sional appropriations speciﬁcally recognize addit-
ional alternatives.

To the best of our knowledge, no change has taken
place in the long-term mean runoﬂ" or rainfall in
various regions of the United States over the past
100 years. Although geologic evidence indicates that
the ﬂoods in 1936 on the Connecticut and Ohio Rivers
were the greatest in a geologic record representing
some thousands of years, there is no evidence that
ﬂoods today or during historical times are greater
than those of the past, or that droughts are deeper
and longer (Hoyt and Langbein, 1955). Further, we
have learned that wet year‘s follow wet, and dry fol-
low dry, and that climatic change is the rule, not the
exception. This unexplained paradox of both a con-
stant mean ﬂow and evidence of climatic change in
historic and geologic records may reﬂect both the
relatively short period of time over which measure-
ments have been made and the subtle nature of
changes in combinations of different climatic pa-
rameters which lead to signiﬁcant variations in ef-
fects. Even without major changes in climate, “ex-
tremes” of either drought or ﬂood beyond those we
have experienced are likely to occur in many areas.
This is so not only because we can readily envision
combinations of meteorologic events which have not
yet chanced to occur, but in addition because the
longer the record, the greater the likelihood that a
still larger ﬂood or longer drought will be
experienced.

The country has, of course, derived little comfort
from the evidence that the mean rainfall or climate is
much as it always was, or that the magnitudes of
oscillations about the mean are also much as they
always were. Generally we have responded to both
low and high ﬂow by building reservoirs. This is true
both East and West. Not only Los Angeles, but New
York and other eastern cities have gone long dis-

20 EARTH SCIENCE IN THE PUBLIC SERVICE

tances to provide water for growing cities. Reservoir
storage in some arid and semiarid regions has re-
duced streamﬂow to a point at which loss by evapora-
tion from additional reservoirs has exceeded gains
from increased storage (Langbein, 1959). For the
country as a whole, the added quantity of water made
available by storage equals roughly 15 percent of
total riverﬂow; only the Colorado, Pecos, and Upper
Missouri basins are near maximum levels of regula—
tion (Wollman and Bonem, 1971). Despite the fact
that large reductions in ﬂoodﬂows have been achieved
on many rivers, or perhaps because of the fact, the
public is probably unaware that a ﬁnite risk of ex-
ceeding the storage capacity continues to exist in
even the most heavily regulated basins.

If variability characterizes riverﬂow in the United
States, it is not surprising that catastrophic extremes
have captured public attention. At the same time, in
the Eastern United States, where variability is least,
economic growth has produced the earliest invest-
ments in reservoirs and aqueducts and has stimu-
lated the most intensive observations of streamﬂow.
The longest record and most intensive coverage are
needed where the variability is both temporally and
spatially the greatest. Because of the course of our
history, however, for some time, the availability of
money coincided with the availability of water to
provide a surfeit of information in the Northeast and
a deﬁcit in the drier parts of the country.

Attempts to grapple with the captions behavior of
natural streams have clearly inﬂuenced public policy.
Floods and droughts have stimulated investment in
observation, analysis, and control. At the same time,
the absence of catastrophe, although it may have
lulled the public consciousness, has not put it to sleep.
Thoughtful approaches to public policy, such as the
institutions propounded by Morgan for the Miami
River and the Tennessee Valley or the alternatives to
ﬂood control suggested by White, have achieved ac—
ceptance, sometimes riding a wave of catastrophe.
Perhaps even more important, the public has con-
tinued to support fact ﬁnding and analysis as the
population and the economy have grown. This is il-
lustrated perhaps by the coincidence of gaging sta~
tions and economic activity in the humid Eastern
United States. That a Federal agency believes this
relationship between economy and science is im-
portant is indicated by the following quotation from
the Geological Survey’s Long Range Plan (U.S. Geo].
Survey, 1964, p. 45).

The rate of development and use of water in the United

States, and consequently the need for water information,
has expanded faster than the water-resources program of

 
the Geological Survey. This discrepancy is shown in [a
comparison of] professional and technical scientiﬁc man-
power in the water-resources program [and] industrial
water use. During the period 1952—62, water intake by six
principal water-using industries increased more than 60
per cent, whereas the scientiﬁc manpower of the Survey
water-resources program increased only 40 per cent.

From 1960 to 1965, appropriations for water re-
sources rose from $48 to $59 per million dollars of
GNP. The Survey did not rest its case upon a ﬂood
or a drought.

WATER QUALITY

With regard to water quality, the record is differ-
ent. With rare exceptions, environmental degrada-
tion, or loss in water quality, has had few moments
comparable with the Mississippi River ﬂood of 1927,
the Susquehanna ﬂood of 1972, or the New York City
drought of 1965. For the most part, the chronology
is characterized by the undramatic increase in sew-
age generated by more people, or by the periodic in-
troduction and distribution of the products and
wastes of society, such as DDT, detergents, or radio-
nuclides. What is episodic, virtually random, and un-
predictable, is the introduction itself of innumerable
and wholly new materials, many of them foreign to
nature.

Thus it is more difﬁcult to isolate speciﬁc reasons
for the resurgence of an interest in environmental
quality in the 1960’s. Some relate the true awakening
of public consciousness to the reports of the astro-
nauts and to the magniﬁcent photographs of the lone-
ly Earth in space that appeared on television and on
the cover of “Life.” Others have suggested that the
barrage of studies of population growth and the
ubiquitous character of air and water pollution
struck the consciousness of an afﬂuent leisure popu-
lation able to enjoy the world of nature. True, there
have been ﬁsh kills, Torrey Canyon and Santa Bar-
bara oil spills, and the publication of “Silent Spring.”
Most of these incidents were not unique and repre-
sent some likely probability of error in a growing
society of immense complexity. The number of such
events in a given time period is increasing, but their
frequency with respect to the magnitudes of the
activities involved may well be decreasing. Acts of
nature have great impacts on water quality, but for
the most part they are ignored. The principal impact
acknowledged comes from the scale of human activi-
ty, and the effect is primarily cumulative, and not
episodic.

An equally important distinction between the place
of catastrophe in water-quality policy and that in

CRISIS AND C‘ATASTROPHE IN WATER-RESOURCES POLICY 21

water-quantity policy is that, with few exceptions,
degradation in water quality in this country has been
less immediately and directly related to massive hu-
man suffering. Although water—quality-related disas-
ters continue to occur, happily one must go back in
history for good examples such as typhoid fever epi-
demics in Lowell and Lawrence, Mass, in 1890.
These epidemics were river borne, and they were not
unique. Again, however, politics, science, and catas-
trophe were joined. In 1885, the Commonwealth of
Massachusetts had passed “an act to protect the
purity of inland waters of the state.” This act led to
the establishment of the Lawrence Laboratory and,
under the leadership of Sedgewick (1911) , to the cul-
mination of the movement for sanitation based upon
an emerging science and technology. The remarkable
results of this movement to improve the environ-
ment as a means of protecting human health are seen
in the striking decrease in typhoid fever in the
United States between 1900 and 1930, a decrease
which parallels the introduction of public water sup-
plies and treatment facilities and the growth of sys-
tems of sewerage and sewage treatment (Wolman
and Bosch, 1963).

Because the history and timing of response to
water-quality problems appear to differ markedly
from the response to problems of water quantity
(save in the penchant for building things), it is use-
ful to look more closely at the history of the quality
of the Nation’s waters. Unfortunately, as the Direc-
tor of the Geological Survey, the Environmental Pro-
tection Agency, the Council on Environmental Quali-
ty, and the authors of studies reconstructing this his-
tory have observed, the record available for the pur-
pose is exceedingly weak. Some examples must suﬂ‘ice
—and it is well to keep in mind in a review of water
quality that before Columbus, the Saline River was
saline, and the Missouri muddy.

Early history
Records indicate that dissolved solids in the Illi-

nois River have increased roughly 30 percent and-

chlorides on the Ohio about 50 percent since the turn
of the century. Apparently these constituents began
to increase in Lakes Erie and Ontario at about the
same time. In the same period, however, salinity on
the Colorado rose 100 percent (see Wolman, 1971, for
these and other general changes in river quality).
Most changes in dissolved solids resulting from in-
dustrialization or from agriculture, as well as
changes in sediment content, appear to have been
progressive rather than abrupt. Meade and Trimble
(1974) have shown, for example, that the sediment

 
content of rivers in the Southeastern United States
continues to reﬂect loads supplied from the water-
sheds during the height of cultivation in the last
century, despite the presence of reservoirs upstream
and recent changes in land use which have reduced
the supply of sediment. In contrast, on the Colorado
River, construction of major dams and reservoirs
abruptly reduced or eliminated the movement of sedi-
ment downstream.

Fish populations in lakes and rivers apparently
ﬂuctuated signiﬁcantly even before the 20th century.
On the Delaware River, ﬁsh catches declined as a
result of intensive ﬁshing and the use of weirs and
nets. Elimination of weirs and other obstacles about
1885 apparently permitted a resurgence of the shad
population. The shad catch rose to a peak in 1900 and
declined sharply by 1910 (Kiry, 1974). In the Great
Lakes, marked changes have occurred in the composi-
tion of species of ﬁsh. Perch, for example, have com-
pletely replaced pike and herring in the Lake Erie
harvest; total production continues to be about 50
million pounds of ﬁsh per year (Beeton, 1969, p.
175).

Dissolved-oxygen levels in the Hudson River in the
vicinity of New York fell rapidly from about 1900 to
1915 as the result of the large quantities of un-
treated sewage delivered to the river. On the Po—
tomac, as early as 1804, merchants in Georgetown
(now part of the District of Columbia) were peti-
tioning Congress to dredge sediment from the river.
By 1883, Major Hains reported a stench from sew-
age sludge and sediment which he thought “inap—
propriate to the official residence of the ﬁrst magis-
trate of the land” (Geyer and others, 1965J p. 30). In
general, fear of typhoid fever, foul smells, and the
unsightly condition of the rivers in the Eastern
United States stimulated the initiation of measures
to control pollution. Recent surveys of citizen’s deﬁ-
nitions of pollution continue to emphasize sights and
smells and not the esoteric surrogates experts meas-
ure. Efforts at control of sewage efﬂuents in many
eastern rivers from the early part of this century
until the 1930’s were at best able to maintain rela-
tively low levels of dissolved oxygen because of the
growth of population and industry. By 1930 or 1940,
anaerobic conditions prevailed in many rivers ad-
jacent to metropolitan centers.

The last forty years

Large investments in sewage-treatment works, be-
ginning in the 1930’s, began to raise dissolved-
oxygen levels and river quality, for example, on
the Potomac at Washington, DC, and on the Missis-

22 EARTH SCIENCE IN THE PUBLIC SERVICE

sippi at St. Paul, Minn. In seeking models for public
response to water problems, it must be noted that
although the conservation ethic of the day con-
tributed, investments made during the New Deal for
sewage-treatment plants were viewed primarily as a
vehicle to improve the economy and to provide em-
ployment. Ironically, in all likelihood they did little
to improve the economy, but they did improve the
rivers.

Some rivers, including the Delaware and the Ohio,
may have reached their lowest quality by the mid-
1940’s during World War II. A section of the Dela-
ware 12 miles long in the vicinity of Philadelphia
was Without oxygen, and sulﬁdes blackened ships in
the harbor (Kiry, 1974). Expenditures for sewage—
treatment plants rose after the war. By about 1952,
minimum levels of several parts per million dissolved
oxygen prevailed in the Delaware as they do today.
The Ohio River Water Sanitation Commission, cre-
ated by Compact in 1948, had generated more than
$1 billion of State and local funds for pollution con-
trol by 1965 (Cleary, 1967, p. 126). The river and
many of its tributaries began gradually to improve
in quality. These expenditures for pollution control
after World War II seem to have been inspired by
prosperity, not depression, and they moved forward
Without beneﬁt of either natural catastrophe, politi-
cal fanfare, or popular slogans; however, they were
not Without local popular support and competent
technicians, who occasionally had the brilliant per-
suasiveness of an Ed Cleary (1967) of ORSANCO
armed with a toothless compact.

A succession of Federal water pollution control
acts marked the late 1950’s and 1960’s. The most
recent peak of interest in the environment sparked
the passage of “clean water” legislation in the 1970’s.
The most recent act, the Water Pollution Control Act
Amendments of 1972, was predicated on the assump-
tion: that waterways should not be used for the
dumping of wastes; that efﬂuents, not ambient water
quality, would be a better basis for regulation; that
technology could be depended upon to treat or control
the wastes that a technological society had gener-
ated; and that point sources should be given priority
for control.

Currently, New York City, in the middle of a $4
billion program, is spending at the rate about $1
million per day in the construction of sewers and
treatment plants. According to “Engineering News-
Record” (May 30, 1974, p. 14), this amounts to $143
per person annually, nearly ﬁve times more than
Seattle, the second largest spender. As a result, dis—

 
solved-oxygen levels in the harbor have risen to 50
percent of saturation, the highest level since the
early 1900’s. Although New York had expended large
sums on treatment plants from 1950 to 1965, the
city’s present heroic effort began in 1966 after the
passage of State and Federal pollution control
legislation.

The past 5 years has also seen a rapid rise in pri-
vate expenditures for pollution control. Curiously,
however, the interest that peaked in 1970 has not
been accompanied by a comparable commitment of
public money since that time. Expenditures for pub-
lic sewerage facilities for the country as a whole have
risen continuously since 1856, but in the past year
these have begun to level off. This year’s expendi-
tures for public treatment works are likely to be less
than those of last year (US. Environmental Protec-
tion Agency, 1973b). A variety of reasons have been
given for this recent decline, including insufﬁcient
funds for public works, bureaucratic wrangling, and
the state of the economy. Whatever the reasons, total
discharge of pollutants from both point and nonpoint
sources may well be continuing to rise.

Studies of the recent past have suggested, as yet,
no clear patterns of response in the water environ—
ment to the new pollution control efforts. A US.
Council on Environmental Quality (1972, p. 14)
study suggests that from 1957 to 1970 dissolved oxy-
gen may have risen at 50 percent of the sites sam-
pled in the study and declined at 23 percent. The US.
Environmental Protection Agency (1973a) reported
roughly similar ﬁgures, comparing the 5-year period
1963—68 With the following 5 years to 1972. From the
council study, improvement seems greatest where
point sources of pollutants dominate, and no trend is
evident in agricultural basins. Levels of phosphates
and nitrates in streams continue to increase in many
reaches, apparently as a result of inﬂow of deter-
gents and industrial eﬁluents in some places and of
fertilizers in others.

Water quality has declined, or on occasion, im-
proved, as a result of the activities of man. Until re
cently, the greatest changes may be described as co-
incidental and not directly related to a concern for
the quality of the water resource itself. Thus, deb
velopment of farming in the forested East produced
vast quantities of sediment which drastically altered
the waterways. Abandonment of farming in turn re-
duced this yield, and lake and river quality improved.
Similarly, in the drive to eliminate typhoid fever, the
rivers beneﬁted. Only in the 1930’s did the effort turn
principally to the waterways themselves, and, even

CRISIS AND CATASTROPHE IN WATER-RESOURCES POLICY 23

then, a primary stimulus to action was the concern
for unemployment and the state of the economy. In-
terest in water quality accelerated after World War
II and may have peaked in 1970 or 1971.

Sequential changes in water quality and attention
to them are not a response to natural catastrophe and
are only occasionally a response to dramatic political
or economic events. Indeed, political enthusiasm and
expenditures for engineering works have run well
ahead of the rate of acquisition of adequate knowl-
edge about the quality of the water. Proposed ex-
penditures for water pollution control currently run
as high as $4 billion to $6 billion per year. This may
or may not be an appropriate amount. Unfortunately,
although major efforts are clearly needed, informa-
tion about the quality of the water itself is too poor
to permit sound evaluation of the efﬁciency of these
large expenditures, or of alternative strategies for
efﬁcient use of increasingly scarce monies. Similarly
unfortunate is the absence of measures of the social
costs of polluted water. Lack of knowledge about
water quality and about social costs clouds public de-
bate over the appropriate level of effort to be ex-
pended in water pollution control.

LESSONS FROM THE HISTORICAL RECORD
STIMULANTS To INTEREST IN WATER: THE MonELs

Historically, catastrophe, whether natural ﬂood or
manmade depression, episodically stimulated invest-
ment in water management. However, changes in
water quantity, and particularly changes in water
quality, although they may have inﬂuenced public
policy (a policy about ﬂoods without ﬂoods is unlike-
ly) have not been the dominant inﬂuence on expendi-
tures for public works or for scientiﬁc investigations
of water resources. As the Geological Survey has
recognized, the budget is most closely tied to the
broad social and economic march of the country.

Dominant social concerns have broadly determined
historical behavior, and more often than not, legisla-
tion and action have preceded or even contravened
scientiﬁc understanding; the Desert Land Act based
on the hope that trees would induce rainfall to aid
settlement, and the expectation that forests would
control major ﬂoods are cases in point. Yet the results
of these actions, often inefﬁcient and sometimes in-
effective, can be salutary and are not all bad. Then
too, the very passions, sometimes spurred by catas-
trophe, that provoked action stimulate scientiﬁc ef-
fort, which may serve to redirect public policy at a
later time. Progress in sanitation suggests that even
between the peaks of political passion, gains can be
made. One cannot, and apparently need not, wait for

 
that rare combination of remarkable man, prepared
science, and natural or manmade catastrophe. At the
same time, one can be prepared to strike when the
iron of public interest is hot.

The record suggests that a combination of continu-
ous investment in science, the ponderous momentum
of society, and preparedness to make quantum steps
when opportunity affords may not be a poor strategy
for a scientiﬁc agency. Some may lament that such a.
strategy too closely parallels the political scientists’
model of a typical bureaucracy protecting its ﬂanks
While inching slowly forward (Tullock, 1965), an
image of caution not boldness, of dullness not cre-
ativity. The image is not warranted. Continuity is
desirable in scientiﬁc inquiry and particularly so in
the observation of hydrologic phenomena. The rela-
tively smooth growth curve that characterizes the
history of water-resources investigations may be
rational both in terms of the agency’s needs and
those of the society. At the same time that the coun-
try seeks guidance over the long term, it demands
creative response to the problems of the day as it per-
ceives them.

TRENDS TOWARD NATIONAL RESPONSIBILITY

In addition to a modest test of some hypotheses
about the causes and stimuli of interest in water re-
sources, even this brief historical review provides
evidence of the continuing trend toward national and
away from State and local responsibility for water
management. Approaches to both water quantity and
quality reﬂect this trend. The visitation of catastro—
phe in the form of ﬂoods and droughts on any one.
section of the country has, since the 1930’s, for ex-
ample, led to the increasing assumption of responsi-
bility at the national level. The Flood Control Act of
1938 liberalized cost-sharing provisions for the Fed-
eral ﬂood control projects and relieved the direct
beneﬁciaries of major responsibility for reimburse-
ment. More recently, the devastating ﬂoods associ-
ated with Tropical Storm Agnes in 1972 produced
modiﬁcations of the ﬂood insurance act of 1968. Re
quirements for land-use planning in ﬂood-prone lands
were strengthened, and the level of premium pay-
ments required of the beneﬁciaries was signiﬁcantly
reduced.

In the field of water quality, the tendency toward
the assumption of national responsibility is also
apparent in the passage of the Central Arizona Proj-
ect by the Congress in 1970. Recognizing that the
water available in the Colorado River was already
overcommitted in this country, and further, that the:
United States had recently accepted a commitment to

24 EARTH SCIENCE IN THE PUBLIC SERVICE

supply Mexico with a speciﬁed quantity of “unsalty”
water each year, Congress provided that the Nation,
not the region, bear the costs of meeting the added
burdens of the recent agreement with Mexico on
water quality.

Similarly, it may be ironic, but perhaps under-
standable, that Arthur Morgan’s pioneering effort to
“internalize the externalities,” that is, to approach
water management on a regional basis under local
authority, is currently in danger of being dismantled
as Federal and State powers over pollution abate-
ment grow. Such conﬂict between local, State, and
Federal government is, of course, a logical conse
quence of further expansion of the Federal and State
interest reﬂected in the Water Pollution Control Act
Amendments of 1972.

MODEST PROPOSALS

The fundamental work of an agency such as the
Geological Survey consists of programs of observa-
tion and analysis which customarily grow incre—
mentally as the needs of society expand. Over time,
responsibility is assumed for a long list of activities.
Many of these cannot be summarily abandoned. As
custodian of the knowledge of long-term trends in the
hydrologic cycle, for example, the Geological Survey
cannot simply halt all observational programs di-
rected toward this objective. Similarly, society would
be ill served by wholesale abandonment of interest in
speciﬁc facets of the hydrologic cycle. This does not
mean that nothing is ever abandoned, or that pro-
grams never change, or that the emphases do not
change. Rather, it means that additions and new
emphases must be selected from a current array of
public interests and demands. Some of these may
require radical departures in attitude or approach,
even if not in apparent content. The present scene
abounds in issues, concerns, and catastrophes. These
issues and the demand for continuity provide some
basis for selection of priorities.

The issues are familiar. First, the evidence is good
that although the fervor may have died in the breasts
of some environmentalists, much of the American
public is convinced that they want a better environ-
ment. Second, population will continue to grow, even
at a reduced rate, for several decades, and continu-
ing numbers of people will want to share in the fruits
of growth. Third, energy has recently become a part
of American consciousness. Fourth, in the world as a
whole, drought, hunger, and starvation are daily
realities. From the standpoint of an interest in water,
these issues all involve two points of view, ﬁrst the

 
long view of what may be happening to the resource
as a whole, and second, a detailed knowledge of how
water is used and affected by speciﬁc hum-an
activities.

WATER-QUALITY APPRAISAL: A UNIFIED APPROACH

The ecological truism that “one man’s garbage is
another man’s mea ” or that things are connected,
provides a starting point for the ﬁrst approach. Legal
ﬁat cannot disconnect the parts of the hydrologic
cycle or the cycles of materials between land, air, and
water. Given the major interest in environment and
the large sums to be expended in behalf of its im~
provement, a major effort to structure a comprehen—
sive program of evaluation of water quality covering
the continental and coastal waters is needed. Like
the Survey’s emerging studies of regulated water
systems (Benson and Carter, 1973), such a program
must involve a knowledge of sources, transport, stor-
age, and sinks of residuals to the water environment.
Acid rain in New England and the linkage of ground
water and land disposal illustrate the interactions of
land, air, and water.

Today’s map of areas of major pollution potential
is virtually identical with one made in 1936; the areas
of urbanization have simply grown larger, and more
pristine areas have been invaded. Unfortunately, for
most areas, we know neither the sources nor thevsinks
of materials entering the lakes, rivers, and estuaries.
The relative contributions of point and nonpoint
sources vary from 10 to 90 percent. Trace metals and
other minor constituents are sometimes found in
high concentrations in the water and bottom sedi-
ments. Not only is their distribution poorly known,
but we cannot compute with satisfactory accuracy
the rate of removal of such materials should new
sources be completely controlled. The prospects for
permanent burial or for mobilization of both nutri-
ents and toxic materials are poorly known (Symons,
1969). In the long run, the estuaries and continental
shelves are the probable sinks for pollutants if river
regulation is not too extensive. Only very recently,
however, has a true compilation of the transport of
dissolved and suspended materials to the continental
margins been published (Curtis and others, 1978;
Leifeste, 1974) . This is based on limited information,
and data on other materials are even more meager.

The purpose of a comprehensive program of ap-
praisal is to assist in the prediction of the impact of
policy decisions. Because this requires a knowledge of
process, observation must be accompanied by con-
tinuing analysis. Parameters chosen for study will
include meaningful biological characteristics as well

CRISIS AND CATASTROPHE IN WATER-RESOURCES POLICY 25

as signiﬁcant physical features and inorganic sub-
stances. In depth an-d scope, the inquiry may comple-
ment the needs of law enforcement, but the two pur-
poses are not synonymous. For example, a pollution
index may be a useful monitoring tool, but such an
index may mask the interrelationships needed to de—
ﬁne effective policy instruments. Similarly, although
regulators need access to facts and competent scien-
tiﬁc assistance, the historic record has shown that
mission-oriented agencies may become addicted to
demonstration rather than evaluation (Schif'f, 1962).

The pieces of such a program have, of course, re
ceived attention. Current efforts, however, appear
both too limited and too fragmented relative to our
presumed commitment to environmental quality. Per-
haps the Water Resources Council can be made re-
sponsible for spelling out a truly broad mission for
the agencies involved, not as a treaty but as a com-
prehensive plan. As the observer of water and the
possessor of the sense of time, the Survey has a
major role to play.

WATER AND CLIMATIC CHANGE

Famine in Africa and elsewhere calls attention to
another facet of water resources that requires a long
View but that has consequences directly related to
problems of current public policy. What are the char-
acteristics of climatic and hydrologic variations, and
what is the level of uncertainty appropriate to the
planning of human activities? As the history of
Colorado River development illustrates, human ex-
perience, and particularly local experience, can only
include patches of the record. Even the best of plan-
ning using stochastic concepts is unlikely to encom-
pass some unexpected long-term trends; hence, short-
age and surfeit may be mitigated but are not likely
to be eliminated. The consequences of certain as-
sumptions about hydrologic variability are becoming
even more painfully evident today, as shown by the
relation of the destruction of grassland and the re-
cent dependence on wells in sub-Saharan Africa.

The problem of climatic variability is perhaps of
even more signiﬁcance in a broader context. Much
current thinking is based upon too simple a concept
of equilibrium or balance in nature. The record re-
veals that the entire landscape and the natural biota
associated with it may undergo signiﬁcant alterations
from what we presume today to be a condition of
equilibrium or stability, when such alterations are
triggered by a succession of years of climatic and
hydrologic change. Such changes in the past, for ex-
ample, may have produced rates of erosion in the
Midwest which exceeded those produced by farming,

 
and they have resulted in the ﬁlling and excavation of
the valleys of the Southwest a number of times. Pub-
lic policies based on the assumption that men are re-
sponsible, as some policies were in the 1930’s, may be
both costly and doomed to failure.

WATER USE: DEMAND, PRODUCTION FUNCTIONS,
AND MASS BALANCES

The Geological Survey has long had responsibility
for measuring or estimating the withdrawal and
“use” of water in the United States. These estimates
are classically viewed as measures to be matched
against estimates of supply, as part of the process of
developing public policies for resource allocation. As
so—called needs, or requirements, on the use side have
risen, however, it has become increasingly evident
that evaluation of policy alternatives requires a deep-
er knowledge of the demand and supply relationship.
Not only must the use of differing quantities. of
water of a given quality be measured, but inquiry is
needed into the economic and social factors that lead
to particular choices. We need to know not only how
much water of what kind is used, but also why.

Obviously the study of water use in every kind of
industrial, commercial, or household activity is un-
warranted. Clearly, however, production functions
providing explicit information on the role of water in
major economic activities and on the way in which it
is used and transformed are essential to future
policy choices. The widespread interest in energy
makes analyses of the amounts of water used and the
changes in water quantity and quality in the energy
industry imperative. Considering their importance,
current estimates of quantities of water needed for
various energy conversion processes seem unneces-
sarily conjectural. Work has been started by the
Survey and by others (Delson and Frankel, in press)
in some of these ﬁelds. Additional effort in the energy
industry, in agriculture, and perhaps in several other
major sectors of the economy may be warranted. The
use of production functions (Minhas and others,
1974; Lof and Kneese, 1968) and mass balance frame—
works for studies of speciﬁc activities (Bower and
others, 1972) will provide additional tools for meas-
uring the effects of various activities on the water
resource, for estimating needs for speciﬁc data or re-
search, and for evaluating the probable response of
different activities to different policies affecting
water resources.

The Government Accounting Ofﬁce noted that the
budget for true research in the understanding and
techniques of improving water quality is quite small
—a Montana rancher recently referred to a disease

26 EARTH SCIENCE IN THE PUBLIC SERVICE

she called “lackadata.” Cries for research and for
data can, of course, be excuses for inaction. As com-
plete knowledge is unattainable, action cannot wait.
Because this is so, scientiﬁc inquiry and appraisal of
the kind described above—in current environmental
jargon, “evaluation”—must accompany action. The
argument is sometimes sound that we must do
something to ﬁnd out what happens. Unfortunately,
we usually do something but rarely ﬁnd out what
happens. There will be no excuse 20 years from now
for “lackadata” disease where reclamation following
mining for coal or for shale oil in the West is con-
cerned. A proper study of the impact on water re-
sources of such activities as energy conversion or
mining, however, demands elaboration of a plan of
study before activities begin and a scheme of ﬁnanc-
ing to assure the necessary longevity.

OBJECTIVES AND HOPES

Studies of long-term trends and variability in
water quality and water quantity, as noted earlier, do
not consist simply of data collection. Similarly,
evaluation of demands and uses of water by man are
more than hydrologic budgets. Adequate understand-
ing of each requires an inquiry into the dynamics of
processes. Hopefully, the results of such inquiry will
lead to better understanding of the way in which
human and environmental systems work and an im-
proved basis for prediction of probable interactions,
if not of probable futures. New concerns for energy
and for conservation in the United States may stimu-
late research in water resources in directions promis-
ing greater utility abroad, particularly in the less
developed world. While we seek solutions to our own
legal, social, and technological problems, a search for
efﬁciency in water and energy uSe coupled with at-
tempts to minimize env1ronmental impacts may aid
this process.

Most of the major issues of the day—environment,
growth, food and famine, cities, and energy—involve
water. All are crises in that people today are poor
and starving. None of the questions that confront us
in the ﬁeld of water quantity and quality can be
properly called a crisis, however, if that word implies
a short time scale. As they have always been, the
problems of water quantity and quality are perpetual.
The ability to take advantage of the political mo—
ment, or the awakened public consciousness, by Vir-
tue of a disaster or an election may determine the
extent to which these ﬂeeting moments of interest
are well used in the slow business of improving the
ability of the public and its representatives to make
wise decisions about the future.

 
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of the Great Lakes, in Eutrophication—causes, conse-
quences, correctives~symposium [1067] Proc.: Wash-
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Benson, M. A., and Carter, R. W., 1973, A. national study
of the streamﬂow data-collection program: U.S. Geol.
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Bower, B. T., Lof, G. 0. G., and Hearen, W. M., 1972,
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Cleary, E. J., 1967, The ORSANCO story—Water quality
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EARTH SCIENCE IN THE PUBLIC SERVICE

ENVIRONMENTAL ANALYSIS AND EARTH SCIENCES
IN THE PUBLIC SERVICE

By BEATRICE E. WILLARD
Council on Environmental Quality, Executive Ofﬁce of the President

It is a special honor to be with you for the dedi-
cation of the John Wesley Powell Building of the
U.S. Geological Survey. It is most ﬁtting that this
symposium be held to commemorate that great
geologist-explorer whose vision led to the estab—
lishment of the U.S. Geological Survey, and to di-
rect our thoughts ahead to the contributions earth
sciences can make to the problems ahead.

As a Westerner, familiar from childhood with
the landscape Powell brought to the attention of
the Nation and the world by his courageous sci-
entiﬁc explorations, I have long been an admirer
of Powell’s work. The understanding of the geologic
processes that produced this landscape contributes
essential insight to the work of the Council on En-
vironmental Quality, just as it has long made a
major contribution to my professional competence
and has been a source of continuing personal fas-
cination.

Our two sciences have much in common. They
both look at landscape from the process systems
Viewpoint—mentally seeing hundreds, thousands,
even millions of years into the past, and, using
this perspective, determining what the future
might hold. They both, as sciences, have discovered
basic principles about the operation of Earth’s
landscapes that can assist man in adapting to—
harmonizing with—Earth’s processes, if the prin-
ciples are accepted and used.

If John Wesley Powell were alive today, he ob-
viously would be proud of the many laudable sci-
entiﬁc accomplishments of the U.S. Geological Sur-
vey, and he would be pleased at the expansion of
its work into the oceans and Arctic regions. How-
ever, he would be astounded at the huge desert lake
that bears his name and mortiﬁed that man could

28

 
allow the submergence of land of such rare beauty
and scientiﬁc value so that an engineering tech-
nique might be used to solve a political problem. I
mention this distasteful fact only because it sounded
an alert to citizens and, together with many other
signs of environmental deterioration in the 1950’s
and 1960’s, led to awakening the Congress to the
great need for a National Environmental Policy
Act.

In preparing for this auspicious occasion, I kept
asking myself, “How would Dr. Powell want the
Nation to use earth sciences were he alive today?”
As a great student of nature and in tune with the
natural processes operating in our landscape, he
would urge our acceptance of the basic principles
of landscape into the ﬁber of our thinking and ac-
tion. He would insist that we choose these prin-
ciples as our guidelines for decisionmaking, rather
than political expendiency, economics, and develop-
ment for growth’s sake alone. He would utilize
these basic landscape principles, as most scientists
today do, as the framework for all action. He would
communicate them in meaningful ways to the Na-
tion’s citizenry, the Congress, agency personnel,
and administrators, so that these principles might
permeate thought and action as our Constitution
and Bill of Rights do.

I ﬁnd it continuingly beneﬁcial to reexamine the
basic principles of the earth sciences and how they
can guide thinking and action about landscape.

The ﬁrst principle is by far the most important,
yet hardest to accept: Everything affects every-
thing else. This principle demands that we ques-
tion the many ramiﬁcations of human action and
choose the path that has the most overall positive
effects, after taking into account long-range values

ENVIRONMENTAL ANALYSIS AND EARTH SCIENCES IN THE PUBLIC SERVICE 29

and short-term beneﬁts. This demand became law
as part of the National Environmental Policy Act
of 1969, in the requirement to prepare environ-
mental-impact statements—analyses of the ramiﬁ-
cations of human actions.

The second principle is that landscape is a mosaic
of dynamic systems (earth systems, ecosystems)
comprising physical components (rocks, landscape
features, soil, climate, water), biological compo-
nents (plants, animals, humans), and the intricate
dynamic processes that operate among these two
types of components (erosion, deposition, tectonic
movements, cycling, competition, symbiosis, evolu-
tion, succession, politics, and economics, to name a
few). In these systems, all components have a role
integrated with the whole and are inseparable from
the whole.

This second principle ampliﬁes the ﬁrst and
makes the systems approach to research and de-
cisionmaking mandatory. The systems-analysis ap-
proach requires a truly interdisciplinary team ap-
proach, where each member is interacting with
each other member of the team in the design, plan-
ning, and conduct of research and data analysis.
This approach precludes the possibility of omitting
from analysis those lesser known or more diﬂ‘icult
parts of the systems, because, to research, those
gaps in knowledge of the system show up as blanks
in the diagrammatic models of the system that
block further analysis. The Western coal-mining
study of a set of interacting local, regional, na-
tional, and global systems, rather than “rock in the
box,” encompasses the systems approach to a de-
gree. It is encouraging to see systems analysis be-
ing applied to solid-waste management, and the
resulting much more eﬂ‘icient use of time, minerals,
energy, and land.

The third principle is that components of land-
scape systems have limits to their functioning
such as melting points, freezing points, denaturing
points, dehydration limits, nutrient limits, stress
and tension limits, and absorption limits. These
various parameters, interacting, describe the op-
erational perimeters of the biological and physical
systems and therefore dictate the characteristics
of ecosystems. Learning what these parameters are
and how they operate enables man to make more
precise analyses and to draw up wiser plans for re-
source management. Projects designed with the op-
erational framework of the system in constant View
can avoid or mitigate problems that arise from
ignorance or oversight of these limits. For example,
a long-range View of national materials policy from

 
the perspective of this principle could recognize
these points and limit use of materials now, so as
to prolong the supply of resources for the beneﬁt
of future generations. -

The fourth principle is that components of eco-
systems, operating through complex interlocking
biological and physical processes, deﬁne a feature
of all systems, 'which ecologists call “carrying ca-
pacity.” Physicists call it a “breaking point,” “fa-
tigue point,” “stress point.” Whatever the term, it
is a highly useful concept in wise management of
systems. Environmental analyses that include de-
termination of this feature for various human ac-
tivities will show the way to avoid many of the
overload characteristics that we see in air, streams,
lakes, forests, and ranges. Standards set with an
understanding of carrying capacity, which encom-
passes the concept of tolerance limits of organisms
and physical factors, will work to bring man’s ac-
tivities into balance with ecosystems. Carrying-
capacity determination, although difﬁcult and com-
plex to calculate, has been successfully done in
engineering, agriculture, and wildlife management
for decades. It is beginning to be applied in recrea-
tion resource management and in regional planning,
as in the Paciﬁc Northwest.

The recent investigations on “limits to growth”
are an effort to determine a global carrying capacity
for basic resources essential to life. It stands to rea-
son that as all material resources are ﬁnite, the
sooner we tailor human use of these resources to
carrying capacity worldwide, the sooner we can
bring human activities into balance with the Earth’s
resource base. Not a simple goal, but a highly de-
sirable one, and the US. Geological Survey work
of resource assessment is fundamental to it.

Furthermore, the carrying-capacity principle is
dynamic, adjusting with the advent of new tech-
nologies and new discoveries of resources, while
maintaining a balance between users and resources.
I envision great potential for the US. Geological
Survey in its second century, putting the carrying-
capacity principle to work for the beneﬁt of man.

The ﬁfth principle is that landscape systems are
dynamic. They progress through various phases of
development to a point of dynamic equilibrium,
in which state they remain until a major change
of conditions takes them back to an earlier stage
of development—precipitiously, as by earthquake
landslide, ﬂood, volcanic eruption, or insect infesta-
tions, or gradually, as by erosion, climate change,
or evolution. Use of this principle in environmental
analyses frees us from believing that the land-use

30 EARTH SCIENCE IN THE PUBLIC SERVICE

and resource planning and management must be
static. Environmental analyses that include calcula—
tion of the rate of change provide a measure of
ecosystem cost and beneﬁts to compare with eco—
nomic costs and beneﬁts. It is even possible to
analyze ecosystem costs and beneﬁts in dollar
terms, as Eugene Odum has done with the salt
marshes of Georgia. He has found that salt
marshes sold for landﬁll and urban construction go
at $1,000 to $3,000 an acre; if the land is main-
tained as marsh, however, the composite value of
the work of the ecosystem for man—in air and
Water cleansing, nutrient production, nursery
grounds for shell and ﬁn ﬁsh, hurricane buffering,
and recreational and scenic values—is $85,000 an
acre—a free contribution.

As Powell well knew, these principles must be-
come integral to the thinking, decisions, and ac-
tions of all of us. Practicing this fact an engineer
in Denver designed a tool for integrating ecology,
including the earth sciences, into design, planning,
construction, and operation of projects. He calls
this tool the “3 E’s Tripod.” One leg stands for
engineering, one for economics, and one for ecology,
including earth sciences. As you well know, tripods,
to be functional, must have the three legs united to
a ﬁrm central core, and each leg must be in action
and bearing its proportionate weight.

If the principles of landscape are applied, to—
gether with those of engineering and economics,
from the outset, a synergism is set up in the ensuing
analyses that take place in the conceptualization, re-
connaissance, feasibility, and decision phases. Just
as in engineering and economics, the types and
amounts of data and complexities of environmental
analysis increase as you move from phase to phase.

What do these natural guidelines suggest for the
second century of the U.S. Geological Survey:

First, in NEPA (PL. 91-190), carrying capacity
and recycling have been codiﬁed in Section 101 (b) :
In order to carry out the policy set forth in this Act, it is
the continuing responsibility of the Federal Government to
use all practicable means, consistent with other essential
considerations of national policy, to improve and coordinate

Federal plans, functions, programs, and resources to the
end that the Nation may——

* * * * *

(5) achieve a balance between population and resource use
which will permit high standards of living and a wide
sharing of life’s amenities; and

(6) enhance the quality of renewable resources and ap-
proach the maximum attainable recycling of depletable
resources.

 
A double-edged challenge is provided in implement-
ing these two provisions: to maintain the quality
of life and environment While bringing human ac-
tivity into balance—harmony—with the function-
ing of landscape systems.

Second, as the knowledge of Earth increases, the
interrelatedness of geologic, biologic, and climatic
forces becomes more and more evident. This knowl-
edge can enable humans to predict future pheno-
mena with ever-increasing accuracy. This capability
can make it possible to bring human activities into
greater and greater harmony with Earth’s land-
scape systems. For example, the ability to map
earthquake zones and to predict the frequency and
occurrence of earthquakes with increasing accuracy
will make it possible to plan uses compatible with
high-risk areas that complement uses on adjacent
low-risk areas.

Third, geologic and ecologic knowledge can en-
courage precise speciﬁc adaptation of human ac-
tivities to the landscape processes. Some of this is
now evident; more interaction with the public can
lead to more rapid application of the knowledge to
solving human problems. For example, the public
is learning that ﬂood plains are river rights-of-
Way that can be shared by rivers and humans for
activities compatible with periodic ﬂooding; that
earthquake zones can have human uses compatible
with their instability; that erosion and deposition
processes can be understood and human activities
can be located in ways compatible with the con-
tinued operation of the processes, rather than al-
tering the processes locally and regionally, only to
wonder afterward why erosion is removing beaches
and cliffs below cherished resort hotels and homes.

In conclusion, I have drawn some broad-brush
implications of how earth sciences might contribute
to environmental analyses in the future, on the
basis of natural principles so that we can stand
back a moment from the work at hand and ask our-
selves, “Where are we going and do we have the
right quadrangle map to get there ?”—as scientists,
as administrators, as policymakers, as engineers.
The quality of life in the future depends in part
on how well we apply these principles of earth sci-
ence in our daily activities. I rest assured that the
U.S. Geological Survey will continue to expand on
its meritorious tradition initiated by the man we
honor today, by providing the Nation and the
world essential components of better and better en-
vironmental analyses.

EARTH SCIENCE IN THE PUBLIC SERVICE

LEASE MANAGEMENT AND RESOURCE CONSERVATION

By DON E. KASH
Director, Science and Public Policy Program, University of Oklahoma

In practice, public policy and management in the
American experience reﬂect a consistent pattern.
That pattern is to deﬁne decisions wherever pos-
sible as involving questions that can best be an-
swered with information. If one only listens to the
rhetoric, policy debates in this country regularly
sound as if there are no differences among the
values being promoted. In truth, the gut political
choices are among preferences and tastes and who
gains the beneﬁts or suffers the costs. Value
preferences have nonrational and nonempirical
roots and generally cannot be changed by facts or
more information.

This appears to be the case in spades with re-
gard to lease management and resource conserva-
tion. In the resource sector, three fundamental
value issues appear and reappear. They are: First,
the question of “fair value” for resources; second,
the question of who gets to develop the resources
or resource allocation; and, third, the question of
what values are to be maximized in postlease regu-
lation.

One pattern of disguising value questions is to
paper them over by establishing mechanical choice-
making procedures. An example of this is the pro—
cedure for allocating leases on the basis of bonus
bids. In a complex situation, we elevate a single
variable—in this case dollars—to a dominant posi-
tion and let it make the choice. That camouﬂages
the fact that the elevation of the variable involved
a major value choice.

A second pattern is to submerge the value
choices in a mass of information. The debate is
then over who has the best information and what
the information says. In both cases, the parties-at-
interest never have to lay out their selﬁsh purposes.
The value choices in the resource area are especial-

 
ly clouded by the information quagmire. This tend-
ency to seek answers in information usually allows
decisionmaking to be transferred to the profes-
sionals and experts.

The central problem in our period of change is
that the mechanisms we have traditionally used to
convert value choices into choices among facts are
not working well because the substantive conditions
in our society have been undergoing massive
changes as a result of modern technology. These
changes have spotlighted some of the inherent con-
tradictions in our traditional assumptions and rules
of operation. Three of these traditions appear rele-
vant to the topic of this paper.

The ﬁrst and most hallowed tradition is the con-
stitutionally established principle that there should
be “walls of separation” established between the
various sectors, functions, and institutions of our
society. The fundamental purpose of this tradition
has been to protect against the abuse of power
thought to be the result of decisionmakers who
have conﬂicts of interest. This particular term
“wall of separation” was used by the Supreme
Court in a 1947 decision declaring that the Con-
stitution requires a “wall of separation” between
church and state.

For our purposes, the most important reﬂection
of this tradition has been the conception that an
adversary relationship is to be desired in the re-
lationsbetween Government and business, or more
generally, the public sector and the private sector.
That conception has been particularly important
in guiding relations between the Department of
the Interior and the resource industry. The fact
that the wall has been breached with regularity in
the resource sector and, in fact, that conﬂicts of
interest are endemic in a complex society has been

31

32 EARTH SCIENCE IN THE PUBLIC SERVICE

consistently overlooked until recently. In practice,
the wall has nearly crumbled in the natural-re-
sources sector.

The second tradition is that the private sector
best serves the public interest when it is governed
by the competitive rules of the marketplace. Stated
succinctly, this tradition says that the private sec-
tor, in this case the resource industry, operates
best with minimal encumbrance by government. In-
creased Government involvement leads to increased
inefﬁciency. That conceptual construct of what the
economists called “the market” is supposed to be
relied upon to govern business behavior. This faith
in the marketplace provides much of the conceptual
underpinning for the desired adversary relationship
between Government and business because Govern-
ment interference is supposed to foul up the op-
eration of the market.

The third tradition is that down at the .nitty-
gritty level, on a day-to-day basis, Government-
industry relations will be carried out in both Sec-
tors by professionals who share a common expertise
and whose real world activities are organized
around common problems. In the resource sector,
whether these professionals be geologists, engineers,
economists, or lawyers, they share the common bond
of a community that views resource management as
an activity best carried out by full-time experts. No
matter where they may be employed—in a Govern-
ment agency or a corporation—they see that ad—
versary process of “politics,” which is central to
the ﬁrst tradition, as a cross they must bear.

CONTRADICTIONS IN THE MANAGEMENT
SYSTEM

Clearly, there has been a fundamental contradic—
tion between tradition one, the wall of separation,
and tradition three, professional management. That
contradiction, however, could be dealt with on an
ad hoc basis so long as leasing and management
took place in a condition of abundance. The philo-
sophical debate over the role of the public sector
versus the private sector might exercise the glands
of liberals and conservatives, but except in the rare
cases, such as Teapot Dome scandal, it had little
impact on what actually happened. Even in cases
of scandal, the corrective action was aimed at con-
straining the abuse of power by corrupt and
avaricious men in a condition of abundance. The
objective was to ﬁnd sanitary procedures that would
protect the public from such men. In practice, this
meant letting a system of clean procedures make
the value choices.

 
Guided by these conﬂicting traditions, the Con-
gress and the executive branch responded in ex-
pected fashion. Within the Department of the In-
terior, a formal “wall of separation” was con-
structed between the organization responsible for
allocating resources and determining revenue
(Bureau of Land Management) and that respon-
sible for conservation and follow-on management
(US. Geological Survey). This was the case even
though the effective exercise of these responsibili-
ties required the agencies to be intimately inter-
twined.

For those resource allocation and revenue de-
cisions assigned to the Bureau of Land Manage-
ment, the traditions have further required the
establishment of procedures that allow minimum
discretion. Where competing companies were de-
sirous of obtaining the right to develop resources,
that right was given either by bonus bids or lottery,
and where there were no competitors, it was given
on a ﬁrst-come basis.

Where procedures are used to disguise and there
fore make value decisions, the only information
necessary is that Which is associated with the single
decisionmaking variable, in this case, time of re-
quest, lottery number, or size of bonus bid. On the
other hand, where facts are used to disguise and
therefore to make the value choices, as in the case
of follow-on regulation, responsibility is assigned
to the professional, scientiﬁcally oriented US.
Geological Survey. In general, the information
disguise was possible because a maturing resource
industry and the Government shared common goals
with regard to conservation. Those goals were the
orderly and timely resource development and maxi-
mum ultimate recovery of the resource. Although
conservation management required sharing infor-
mation and analysis between industry and Govern-
ment, that did not pose a serious threat, given the
shared goals of the postlease or heavily profession-
al management phase.

CHANGING VALUES

As society’s values have changed and as scarcity
has replaced abundance, the elements of the pub-
lic interested in resource management have ex-
panded, and many of the new elements manifest
different values. This has resulted in resource policies
being subjected to a different kind of scrutiny and
has led to widespread criticism. The criticism re-
ﬂects a belief that existing resource management
arrangements are not responsive to the threats of
existing or potential scarcity, new kinds of mul-

LEASE MANAGEMENT AND RESOURCE CONSERVATION 33

tiple—use concerns, and heightened environmental
sensitivities. These pressures have blurred the
boundaries between the responsibilities of the pro-
fessionals and the lay public. Similarly, the divid-
ing line between the resource allocation and-revenue
questions and the follow-on management activities
is no longer clear.

Stated differently, leasing and resource manage-
ment must now be responsive to a much broader
set of goals and criteria. Both leasing and resource
conservation decisions must now reﬂect tradeoffs
among revenue returns, accelerated resource avail-
ability, and environmental-multiple-use concerns.
The dilemma is well illustrated by the proposal to
lease 10 million acres of Outer Continental Shelf
(OCS) lands a year.

It seems unlikely that leasing at that rate will
generate a per-acre bonus-bid return equal to that
produced under a program that leases 1 million
acres a year, thus raising fair-value questions.
Similarly, the need to lease according to some
scheme of areas ranked for their environmental
sensitivity, as proposed by the Council on Environ-
mental Quality, will likely affect both revenue re-
turn and rate of development.

An equally complex condition is developing in
the area of postlease management of resources, as
environmentally responsive management appears
to require substantial prelease planning. This re-
quires early acquisition of a broad range of in-
formation and a substantial increase in the range
and amount of management expertise.

These changing goals and the public attitudes
they reﬂect spotlight two operational demands.
First, there is a demand that at all times, Gov-
ernment must have information and interpreta-
tions on resources equal to those held by industry.
The underlying assumption is that the complex and
highly discriminating judgments Government must
now make among conﬂicting values requires the
best available information. If you cannot use a
single variable and mechanical procedures, you try
to substitute information and expertise.

Second, there is the demand for public participa-
tion in all resource decisions from prelease plan-
ning through postlease regulation. Laymen want a
role. The professionals ﬁnd this diﬂ‘icult because
without professional competence, even with com-
plete information, the layman does not understand
the critical nuances of resource management.

Few things are more offensive to a professional
than a layman questioning his professional deci—
sions. The professional and lay perspectives differ

 
as follows: Experts focus on cause-and-effect re-
lationships. They are oriented toward understand-
ing what causes events to take place, and they un-
derstand the complex and frequently difﬁcult prob-
lems associated with modifying causal relation-
ships. Laymen are oriented toward what the effects
mean to their value preferences. They manifest
little concern for professional values. Laymen may
not be able to explain why, but they can tell What
they like and do not like. When dissatisfaction is
high, the lay public demands the right to participate
so that they can register their likes and dislikes.
The changes I see in resource management are all
linked to this demand for expanded public involve
ment. When nonprofessionals assert the right to
participate in resource management and when they
further assert that nonprofessional values must
carry equal weight, the system is politicized. That
has happened to the resource management system.
Succeszul political systems are those that ﬁnd ac-
commodations among conﬂicting values and con-
ﬂicting facts. Resource management in the future
must ﬁnd such accommodations.

THE CHALLENGE

This is a major challenge for resource managers
generally, but especially so for a professional or-
ganization such as the US. Geological Survey. The
essence of the present demand for management
change is that the contradictions be eliminated by
assuring an adversary relationship between the
Government’s professionals and those in industry.
This is a major reason behind the demand for bet-
ter Government information and more public in-
volvement.

The objective is to insure that Government pro-
fessionals can and will perform as competent ad-
versaries of the industry professionals. In this, as
in every area of our technological society, the
growing pressure is to create a system of “our
professionals” and “their professionals.” This seems
to reﬂect a belief that the public has been snookered
by communities of experts who deny access to the
uninformed. The critical public wants its own ex-
perts—it wants the Government experts to demon-
strate their loyalties by ﬁghting with those in in-
dustry.

These demands are particularly threatening to
the resource industry. From my vantage point, the
resource industry reﬂects a distinctively conserva-
tive posture. By this, I mean that it inherently
fears change. The reasons appear to be at least
threefold: (1) The industry has a history of liv-

34 EARTH SCIENCE IN THE PUBLIC SERVICE

ing with wide ﬂuctuations—going from surpluses
and low prices to scarcity and high prices—and
its response has been to make stability a highly
sought goal; (2) it has been an industry popu-
lated by no-nonsense professionals; (3) it has made
a conservative free-enterprise ideology its rhetorical
touchstone.

From the industry’s point of View, the changes
that are being demanded are seen as a threat to
its proﬁts, a threat of Government meddling in its
day—to-day operations, and as a result, a threat to
the American way. Change in the way the leasing
and resource management system operates is there-
fore, to be resisted, as even small changes are viewed
as having the potential for opening the ﬂoodgates.

In my View, the industry’s approach to change
must, in the end, fail. Existing or potential scarcity
will probably not be effectively managed by institu-
tions and arrangements set up to manage surplus.
Nor will multiple use and environmental values be
effectively responded to by a system established
when they were of no concern.

INFORMATION

Central to the whole issue of industry-Govern-
ment cooperation at present is the question of in—
formation—how much there is, how adequate it is,
who has access to it, and how adequate various or—
ganizations are in an interpretive capacity. The
great danger is that, given our traditions, the ad-
versary process will involve a conﬂict over facts,
when in reality the differences are over values.

The importance of information is therefore more
symbolic than real, but it is no less important for
that reason. Only when both industry and Govern-
ment approach resource information as a public
commodity, in fact only when vigorous and posi-
tive efforts are made to communicate it and make
it understandable, will stable resource management
be possible. The symbolic issue that must be ad-
dressed is the belief that actions are being taken
that are not in the public interest and that such
actions are possible because of selective use of in—
formation and expertise.

Having said that information is central to the
whole debate, let me repeat that I believe it is
something of a red herring. Perhaps it is best char-
acterized as having a distorting effect. It leads to
industry exaggerating what it does not know and
its critics exaggerating what it does know. In sub—
stance, the availability of all of industry’s infor—
mation will provide few answers. My point is that
any effort at addressing the more basic issues re-

 
quires taking actions aimed at getting the informa-
tion issue into perspective. I believe that that re-
quires Government having access to all resource
information, and that as far as is possible, resource
information should be made public.

MAJOR ISSUES

What would the major issues look like if infor-
mation were eliminated as an issue. The “fair
value” question would have to be faced for What
it is. That is, how much of the proﬁt should ﬂow
to Government? In practice, this is a question con-
cerning what the Government gets after the com-
pany has made a reasonable proﬁt. I do not know
what a reasonable proﬁt is, but that is the basic
value question. Given a decision on fair value,
there are many straightforward ways of collect-
ing the money. Either proﬁt sharing or straight
taxation arrangements could handle the mechanics,
but to assume that a bonus bid-ﬁxed royalty will
result in “fair value” is to dodge the basic question.

The question of who gets to develop the re-
sources would require deﬁning criteria sensitive to
a broad set of public interests. Presumably, the
criteria would focus on who could bring the re-
sources on line rapidly and provide adequate pro-
tection for multiple use and environmental con-
cerns. The major concern revolves around big com-
panies versus small operators. In the case of 008
oil and gas, my personal View is that we do not
want small operators incapable of paying the costs
of responding to a “Santa Barbara.” Should the
value choice be to insure access for small operators,
however, the Government would need to make ad-
justments, such as developing the capability for
responding to accidents.

The question of postlease regulation and con-
servation, like the other two, requires value choices.
In this case, the issue is which of the conﬂicting
values you bias the system toward. The Department
of the Interior outlines its management objectives,
in part, as follows: orderly and timely resource de-
velopment, encouragement of development compati—
ble with other land uses, maximum ultimate re-
covery, protection of the environment, rehabilitation
of lands, protection of public safety, compliance with
NEPA, and insuring fair market value return on
the disposition of its resources. That list contains
some fundamental conﬂicts if one gets enthusiastic
about any one of those objectives. Regulation in-
volves ﬁnding the “golden mean” among these ob—
jectives. It cannot be found with more information.
Further, different interests have a different con-

LEASE MANAGEMENT AND RESOURCE CONSERVATION 35

ception of what the “golden mean” is.

The central regulatory question is where you
rest what the lawyers would call the burden of
proof. Regulation varies, depending upon whether
you require the developer to prove that there will
be “minimal environmental damage” or the critic
to prove “major environmental damage,” or
whether you require the use of “best available tech-
nology” as opposed to “best practicable control
technology.” In summary, regulation involves mak-
ing continuous judgments in gray areas; vesting
those judgments in a professional organization
equipped with the best available information does
not change that reality.

A PROPOSAL FOR COOPERATION

Basic to the needs of successful resource manage-
ment in a complex society is the development of con-
sensus among parties reﬂecting different values.
This is the challenge to Government at present.
Such an approach is juxtaposed to the call of many
critics who want a more Vigorous adversary process
which comes to a head at major decision points.

Implicit in the preceding interpretation is the
view that planning, resource allocation, and follow-
on regulation are inseparable elements. They there-
fore require close cooperation at every stage among
industry, other interests and Government, and be-
tween the Bureau of Land Management and the
U.S. Geological Survey. Only such cooperation will
provide the stability necessary to balance the mul-
tiple values. On this point, I would note that we
may have lessons to learn from other industrialized
countries which seem to do better at working in
such a cooperative mode.

Achievement of cooperation requires a resource
allocation-management system that makes coopera-
tion beneﬁcial to all parties-at-interest. Designing
a system that would accomplish that goal requires
craftsmanship of mind-boggling proportions. Un-
der no circumstances would I claim to have accom-
plished the task. Nonetheless, let me suggest the
outlines of a system to which I have given some
thought.

Central to this scheme is the substitution of a
system of licensing resources based on work pro—
grams for the present leasing arrangements.

Step 1 involves Government collection of early
and expanded resource information. Such informa-
tion would include all that collected by companies
or individuals under exploration or prospecting per-
mits, plus a substantially expanded Government ex-
ploration program.

 
Step 2 would call for long-term licensing sched-
ules for each major resource. This would provide
the necessarily long leadtime for planning resource
development.

Step 3 would require preparation of regional
programmatic impact statements, as areas in new
region-s are added to the long-term license sched-
ule. These statements should be planning documents
and should go considerably beyond present environ-
mental impact statements. They should be prepared
by interagency task forces and should be general
development plans including resource, land-use, and
environmental concerns. Their purpose should be to
deﬁne the role and relationship of the resource de-
velopment to the overall use of the region. The pro-
grammatic statements should also include an as-
sessment of the Government management struc-
ture’s capacity to meet its obligations as deﬁned in
the statement. A major purpose of the programmatic
statements should be to provide early access to in-
formation and policymaking for all interested par-
ties; the statements would therefore be the ﬁrst
step in the process of political accommodation and
consensus-making necessary to resource develop-
ment.

Step 4 would involve preparation of a shorter,
perhaps 5-year, license schedule consisting of areas
deﬁned by coordinates. More speciﬁc designation of
the areas to be licensed is necessary to guide the
resource and environmental data collection neces-
sary for the preparation of the license impact state-
ment.

Step 5 would involve preparation of a license im-
pact statement. It should be subsidiary to the pro-
grammatic statement and concentrate on local con-
cerns. The license statement should not repeat
material covered in the programmatic statement
except where it is necessary to amend the plan de-
scribed in the programmatic statement. It should,
however, include an assessment of the agency capa-
bilities for managing the involved resource develop-
ment.

Step 6 would involve allocating licenses based on
work programs that meet the requirements laid
down in the impact statements. Where there are
competing bidders, licenses should be allocated by
choosing among the competitive work programs.
The decisive variables should be (1) speed and
completeness of exploration activity, (2) time
schedule for initiation of production, and (3) re-
sponsiveness of exploration and production activities
to land-use and environmental concerns. All proposed

36 EARTH SCIENCE IN THE PUBLIC SERVICE

work plans should be made public when licenses are a redesign of much of the existing management
awarded. system. It would require both new legislation and

Step 7 should involve regulation that requires ap— major changes in the existing administrative ar-
plication of “best available technology and proce- rangements. It is my view that nothing less is re—
dures” for the protection of health and safety and quired to develop the cooperative system required

the environment. to meet the new resource management circum-
The scheme I have just sketched would involve stances we face.

EARTH SCIENCE IN THE PUBLIC SERVICE

RESOURCE AND ENVIRONMENTAL DATA ANALYSIS

By DANIEL F. MERRIAM
Chairman, Department of Geology, Syracuse University

INTRODUCTION

All the predictions on the depletion of our na
tional resources are pessimistic. We are exhausting
our raw materials, and now it is only a question
of when. It is of top importance, therefore, that
optimum use be made of these resources as they
are exploited, and it will be necessary to achieve a
balance between use, conservation, and environment-
al considerations. As difﬁcult as this may be, how-
ever, the real problem will be in ﬁnding new reserves
to replace the depleted ones. Geologists will play a
key role in the exploration for these new mineral
resources.

I was impressed several years ago by the comments
Bob Weimer (1970, p. 154) made in regard to fu-
ture exploration for petroleum in the Rocky Moun-
tains. Bob, among other things, advocated a team
approach in the evaluation of scientiﬁc data, or, in
his words a “. . . turn to sophisticated geology in
the search for . . . [mineral resources] . . . .” In this
day and age, when large volumes of data are auto-
matically acquired, and techniques are readily avail-
able by which to massage them, this approach de-
mands use of the computer.

Because signiﬁcantly fewer prospects are being
found by traditional methods and because the easy-
to-ﬁnd prospects are gone, the success ratio will
obviously decline. This means an ever-increasing
effort to ﬁnd less and less. Thus, signiﬁcant changes
in philosophy, applied methods, and education are
in the offing if explorationists are to meet the chal-
lenge of the future. In the words of Andre Hubaux
(1973, p. 160), former research secretary of
COGEODATA, “The very future of the geological
profession may well depend on its capability to set
a policy for the presentation to proper authorities
of the basic geological data to estimate the reserves

 
of commodities.”

The new philosophy will reﬂect team inquiry. The
geologist now will integrate his thinking with com-
puter scientists, statisticians, engineers, hydrolog-
ists, geochemi‘sts, and geophysicists in outlining
areas of interest and in monitoring their develop-
ment. Methods will reﬂect the latest available tech-
niques and perhaps simulated real-world models
based on millions or even billions of items of data.
New ideas wil be put forth by the younger better
disciplined geologists who will have been trained
to interpret and judge the interdisciplinary multi-
based data that have been treated in a complex
manner. Therefore, it is extremely important to
train young professional geologists to think in a
multidisciplinary approach to problem solving, to
introduce them to all the latest developments, and
to give them a thorough background and under-
standing of computers and their use.

In the past when new concepts were introduced, it
was not long until methods and technology were de-
veloped to implement the associated ideas. For ex-
ample, the application of geophysics in mineral—re-
sources exploration resulted in an entire new area
of theory and an industry to provide the equip-
ment. As each new exploration technique is intro-
duced, the success ratio increases for a time and
then declines slowly. This results in a series of
surges followed by intervening low periods. Advent
of the computer and application of it to exploration
and exploitation problems will be no exception. Just
now we are in the application phase of this con—
cept and as the team approach is used and as oom-
puters are fully utilized, we should witness a surge,
although short lived, in successful exploration for
mineral resources. It should be emphasized here
that even though the locations of resources are

37

 
38 EARTH SCIENCE IN THE PUBLIC SERVICE

known, the resources may not be recoverable be-
cause of economic or technological reasons—a point
well made by Pratt and Brobst (1974) in their re-
cent U.S.G.S. Circular “Mineral Resources: Poten-
tials and Problems.” The computer also can help in
problems of exploitation as well as in bookkeeping,
as, for example, in the resource appraisal program
of the US Geological Survey, and in projecting
short— and long-term supply and demand.

I would like to take, in turn, each of the areas—
philosophy, applied methods, and education—and
examine them in more detail. First, however, the
data should be examined.

THE DATA

Data are accumulating at an almost alarming
rate. If the geologist is to digest even part of them,
he needs help, and that help must come from the
computer.

There are many advantages in computer-process-
able data. These data are usualy collected under
controlled or semicontrolled conditions, and thus
they are, or should be: (1) objective (usually), (2)
systematic (or in a form that easily can be made
so), and (3) organized (thus ready for analysis
by mathematical and statistical techniques). In
the long run, computer-processable form is the most
economical in which to store large masses of data.

Most data ﬁles are accumulated for special proj-
ects. In fact, objectives should be outlined clearly
before initiation of such a ﬁle (Gilliland and Grove,
1973). In contrast, an archival ﬁle is one of basic
data, diverse, but having widely accepted stand—
ards (Hubaux, 1969).

Several countries are working towards develop-
ment of archival ﬁles, notably Canada, through the
Canadian Centre for Geoscience Data (Burk, 1972).
Romania also is making an effort on a national
basis (Dimitriu and Dumitriu, 1973), as is
Czechoslovakia (Hruska, 1971). I suggest that it
would be proper for the US. Geological Survey to
take the lead in this country and establish a na-
tional center based on the one in Canada. One of
the charges of the US Center for Geoscience Data
would be the development and maintenance of data
ﬁles for use by the geological community. Along
with this function would be the responsibility of
setting standards and exercising quality control of
the ﬁles. Inasmuch as the Survey is deeply involved
in data storage and retrieval already, this seems to
be a logical next step.

One notable example of the Survey’s ever-increas-
ing commitment in this area is the recently estab-

 
lished mineral-resources data bank, CRIB, a Com-
puterized Resources Information Bank (Calkins and
others, 1973). CRIB will provide a quick means for
summarizing and displaying data on mineral re-
sources. In just 5 months after the bank was im-
plemented it contained about 10,000 records. An-
other important ﬁle is RASS, a Rock Analysis and
Storage System. The main ﬁle has been in opera
tion a little more than 5 years and contains about
250,000 records.

It is interesting to note that the national, state
and provincial surveys have been in the forefront
in developing data systems. This is undoubtedly
because historically they have been repositories for
these data. Museums also have been involved with
data systems because of their special curatorial
problems. Recently, two comprehensive summaries
have been published on the status-of—the-art:
“Computer-based Storage, Retrieval and Processing
of Geological Information,” which appeared as Sec-
tion 16 of the 24th International Geological Con-
gress in Montreal (Bergeron and others, 1972), and
“Data Processing in Biology and Geology,” which
was edited by John Cutbill (1971) for Academic
Press. The status of data processing in the earth
sciences in Canada was reviewed by obinson (1970).

Robinson (1974) of the Canadian Survey has
noted that data must be the origin-a1 observations
free from conclusions of the observer. Many geologic
terms however have genetic implications and thus
in fact have conclusions inherent in their use. This
practice, of course, allows disagreements to arise
because of the terminology. Semantic symbols as
proposed by Colin Dixon (1970, 1971) and Pierre
Lafﬁtte (1968) are one possible solution to this
dilemma.

Data are important, and their half-life has been
estimated as nearly inﬁnite in contrast to con-
clusions which have a half-life of only about 3.7
years. The preservation of data is of international
concern, and COGEODATA, a committee sponsored
by the International Union of Geological Sciences,
presently is making plans for the future. “The aims
of the committee are to facilitate access to avail-
able geological data and to promote compatibility
between these data on an international scale”
(Hubaux, 1973, p. 163). A common data base would
allow easy communication on a worldwide basis, en—
hancing geological interpretations; effective use
could be made of mathematical and statistical tech-
niques where standard and comparable data were
available; and many misunderstandings could be
avoided.

In addition to public ﬁles, several commercial sys-
tems are in operation at present. The one best known
to geologists is the Well History Control System
(WHCS), which even 2 years ago had data from

File

GEODAT _________

SIIRS ____________

GEOMAP

EDP System Agto _

GRENVILLE _____

RESOURCE AND ENVIRONMENTAL DATA ANALYSIS

TABLE 1.—Tabulation of select special data ﬁles

Organization

Geological Survey
of Canada.

Smithsonian In-
stitution .

Department of
Geology, Univer-
sity of Reading,
England.

Geological Survey of
(Sjweden and Boliden
0.

Geological Survey of
Greenland.

Quebec Department of
Natural Resources.

Geological Survey of

Canada.

US. Geological
Survey.

Content

General

Chemical analyses, C”
dates, sediment
analyses, rock
properties.

Specimen records for
rocks, marine crus—

taceans, and sea
birds.

Many data sets, project
oriented.

Geologic mapping

Geological ﬁeld data;
mainly for mapping
igneous and meta-
morphic terranes

Field and laboratory
data for a high-
grade metamorphic
area.

Geological ﬁeld map-
ping in the Grenville
province.

Mineral resources

Detailed geological and
mining data.

Mineral resources in-
formation bank.

Size

80,000 items as of
1972.

About 25,000 speci-
mens processed in
the ﬁrst 18 months
at a rate of about
430 records/Week.

100,000 cards ________

To handle about 75,000
observation points,
with 150,000 sys-
temic registrations
and approximately
15,000 samples.

Descriptions of about
10,000 outcrops.

Data on about 4,000
deposits.

10,000 records in the
ﬁrst 5 months.

39

about 700,000 wells in computer-processable ﬁles
(Forgotson and Stark, 1972). A list of representa—
tive special ﬁles is given in table 1. Hubaux (1972)
has compiled a more exhaustive list.

Remarks and references

Started in 1964; di-
rected by K. R. Daw-
son (Burk, 1972).

Started in 1967; re-
trieval programs
written in COBOL
(Squires, 1970).

Contains data back to
1964; utilizes
ROKDOC (London,
1969) .

Introduced in 1970;
retrieval programs
in FORTRAN; also
contains data-anal—
ysis programs such
as DA (Discrim-
inant analysis),
PCA (Principal
components anal-
ysis) and FA (Fac-
tor analysis)
(Berner and others,
1972).

Initiated in 1966; sys-
tem programmed in
Gier ALGOL 4
(Platou, 1971).

Started in 1968; di-
rected by A.-F.
Laurin (Laurin and
others, 1972).

Contains information
on Canadian de-
posits (Burk, 1972;
Robinson, 1970).

Contains information
on US. mineral
resources; retrieval
program, GIPSY
(Calkins and others,
1973).

 
RASS ____________

US. Geological
Survey.

Geochemistry

Data on rock, soil,
vegetation, or water
samples.

About 88,000 records
with as many as
300 items for each
record in analytical
laboratory ﬁle; as
many as 620 items
for each sample of
162,000 records in
airploration research

e.

Started in 1969; pre-
1968 data stored in
a card ﬁle. Utilizes
STATPAC (Miesch,
written commun.,
1974).

40 EARTH SCIENCE IN THE PUBLIC SERVICE

TABLE 1.——Tabulatiovn. of select special data ﬁles—continued

 
File Organization

Content

Size

Remarks and references

 
Paleontology

 
University of Cali-
fornia, Museum of
Paleontology.

Western Interior
Foraminiferal
Data Project.

Colorado School of
Mines.

Vertebrate, inverte-
brate, plant, and
micropaleontological
collections.

Cretaceous foramini-
fers from the West-
ern interior.

About 84,000 localities
and 100,000 speci-
mens.

704 references; 6,000
species citations in-
volving 3,000 differ-
ent species from
4,000 localities.

Started in 1965
(Berry, 1972).

Retrieval uses
SAFRAS (Kent,
19 72) .

 
Well information

 
Borehole data
' from central
Scotland.

Institute of Geological
Sciences.

Well data from Oasis Oil Co _________

Libya.

Lithologic data from
cores of Carboni-
ferous age.

Company records of
boreholes; lithologic,
stratigraphic, struc-
tural, and paleonto-
logic data.

Four borehole records
into the detailed ﬁle
and 15 into the gen-
eral ﬁle as of 1971;
60 more records
ready.

Retrieval programs in
Atlas machine code—-
utilizes ROKDOC‘
(Gover and others,
1971)

Data retrieved in raw
or summary form
(Conley and Hea,
1972)

Lithologic well U.S. Geological Survey Water-well records in _____________________ Started in 1965‘(Mor-
data. and Kansas Geologi- Kansas; lithologic gen and McNellis,
cal Survey. data. 1971)
Saskatchewan Saskatchewan Subsurface geological 18,000 wells _________ Started in 1964; re-
Government Government. and engineering trieval by TELLUS
well-data data. (COBOL based)
system. (Buller, 19172)

 
RETRIEVING THE DATA

Putting data in machine-processable form for
inclusion in data system is all well and good but
of little value if such data cannot be retrieved. Many
retrieval programs, some rather sophisticated,
are being used at present include GEOMAP,
TELLUS, GIPSY, and SAFRAS. Many of the re
trieval programs are constructed for use with a
particular ﬁle system, for example, GEOMAP pro-
grams with GEOMAP ﬁles, and the TELLUS pro-
gram system with the Saskatchewan well-data ﬁle.
GIPSY and SAFRAS, on the other hand, are de-
signed for general use. GIPSY, for example, is be-
ing used to process the data in CRIB.

SAFRAS, an acronym for self-adaptive ﬂexible
retrieval and storage, was developed by Pete Sutter—
lin and associates at the University of Western On—
tario with a grant from the Geological Survey of
Canada. Here, I would like to encourage Federal sup-
port of research. The U.S. Geological Survey, through
a system of direct grants, could commission special
computer—oriented research at universities having
special expertise. This system has been highly suc-
cessful in Canada and could be equally successful in
the United States. The SAFRAS system was de-
signed for general application so that no prestruc-
turing of the data is required; it is easy to use—ﬁles
can be merged, sorted, and reorganized—and the re

trieval is in plain language. A directory precedes

 
the data, giving a complete description of the ﬁle;
this feature allows the ﬂexibility (Sutterlin and
DePlancke, 1969).

G-EXEC, an acronym for the Geologist EXEC-
utive, is a super system designed not only for stor-
age and retrieval, but for analysis and display of

' data as well. The system was developed mainly by

Keith Jeffery and Elizabeth Gill 1 in response to
needs of the Institute of Geological Sciences in Lon-
don. It consists of two parts: (1) the data ﬁles and
(2) the process programs. The system is data inde-
pendent because each data set is self—describing. The
system is modular so that it can be implemented on
small computers and can be modiﬁed or improved
easily. The user commands are in near—English,
facilitating use of the system.

Other systems undoubtedly will be developed in
the future. There are pros and cons to big systems
for archival data versus small speciﬁc systems for
project-oriented data ﬁles. Small systems are cheap
to develop and use, and search is quick because the
data are limited. Large systems are expensive to
develop, maintain, and use, and a search may be time
consuming and thus expensive. However, the ulti-
mate use is greater as the data base is larger.

In the future, big data storage and retrieval sys-
tems will be put into use and small specialized sys-

1Jeffrey, K. G., Gill, E. M., and Henley, S., 1974, G-EXEC system,

user’s manual: Inst. Geo]. Sci, unpub. rept,, prelim. draft of issue
no. 2, 136 p.

 
RESOURCE AND ENVIRONMENTAL DATA ANALYSIS 41

tems will proliferate. Standards and quality control
will gradually be installed at all levels, and geologists
will eventually record all their data on standard
forms utilized worldwide. The US. Geological Sur-
vey, as already pointed out, can continue to be an
effective leader in this area of electronic data proc-
essing where so much expertise is available from
years of experience.

PHILOSOPHY OF SEARCH

Now, I would like to turn to the philosophy of
search, or if you prefer, exploration. In the words of
John Griﬁ‘iths (Grifﬁths and Singer, 1973, p. 9),
The search for non-renewable natural resources is usually
conducted on the 19-century “cause and effect” philosophy.
It is generally believed that if we could explain the origin
of an ore body or petroleum deposit we could predict where
to ﬁnd additional resources. This philosophy is the main
basis for much research devoted to the description and
analysis of natural resources.

Unfortunately, this philosophy, as outlined by Grif-
ﬁths, was good enough in the past but may not stand
us in good stead much longer, at least without modi-
ﬁcation.

Recently, a new approach to the search problem is
emerging; that is, combining statistical techniques
and geology with the expectation of increasing the
exploration success ratio. This approach is through
simulation, in which a stochastic model can simul-
taneously consider many variables to determine the
“best” solution to the problem. Since the work of
Allais in 1957, in which the Algerian Sahara was
used as a case study, the purely statistical approach
has been modiﬁed to take into account geology and
other factors.

One note of caution here, and that too sounded by
John Grifﬁths (1968, p. 6): “. . . the importance of
the philosophy of the scientiﬁc method is that it
encourages an investigator to take a new look at his
problem and not, as is quite commonly done, to at-
tempt to use new tools—more or less as fads—as
additions to old practices.” The one big advantage of
a new approach is that it allows the problem to‘be
reexamined with a new outlook and to be appraised
from a different point of View.

The ﬁrst step in any search is to outline the areas
of interest, that is, to determine the favorable areas
for exploration. The selection of favorable areas
will be based on many factors, including geology.
Once the areas are deﬁned, then the exploration and
development of the deposits require additional data.
These data may be collected according to a prede
ﬁned plan, taking into account the size and shape of
the suspected targets. Much has been written on the

 
“best” methods to use, sampling schemes, and tech-
niques to evaluate the data. Once a deposit is found
and delineated, it needs to be evaluated. For each of
these steps, computer techniques are available to
assist the geologist.

Dee Harris (Harris and Euresty, 1969) of the Uni—
versity of Arizona has approached the problem by
appraising the effect of economic factors which are
evaluated prior to the allocation of exploration effort
and concurrently with mineral occurrence. The tech-
niques used to analyze simultaneously the probabilis-
tic events between economic and geologic conditions
are multivariate geostati-stics and simulation. This
regional, multiple-mineral evaluation approach has
been applied in several areas including Alaska (Har-
ris, 1969) and northwestern Canada (Harris and
others, 1971).

Frits Agterberg and his associates at the Geologi-
cal Survey of Canada also use a regional approach.
Geological and geophysical parameters are assessed
for cells of a predetermined size, and probabilities
of mineral occurrence are extrapolated from known
cells to unknown ones. The potential of any cell is the
difference between the projected and the proven re—
serves for each cell. The Abitibi area on the Canadian
Shield is the object of an ongoing study (Agterberg
and others, 1972). .

John Harbaugh (Harbaugh and Prelat, 1973) and
geologists of the Kansas Survey are developing an
historical model for parts of Kansas. Outcome proba-
bilities for exploratory wells are estimated for each
step through time, on the basis of the geology as
perceived at that particular time increment. The
probabilities are revised with each increment of time
for each cell, as information becomes available.

Larry Drew (1974) of the U.S.G.S. developed a
random-walk simulation model for exploration of
petroleum deposits in the Powder River basin of
Wyoming. The hindsight model was used to demon-
strate the relationship between the intensity of
drilling and the exploration outcome, as summarized
by the quantity of petroleum and the number of de-
posits discovered, and the probability of gambler’s
ruin and different levels of success.

These are just a few of the possible models that
offer insight into exploration philosophy; reﬁne-
ments of these models, or new ones, certainly will be
used in the future. The US. Geological Survey can
continue its work in determining strategies for
exploration for natural resources. These models
would be helpful in evaluating Federal lands avail-
able for lease and perhaps could be applied directly
in areas where the private sector has no interest.

 
42 EARTH SCIENCE IN THE PUBLIC SERVICE

APPLIED METHODS

Techniques are available for analyzing three types
of data: (1) sequential data, (2) map data, and (3)
multivariate data. Most techniques have been adapted
from other disciplines, including medicine, engineer—
ing, biology, statistics, and psychology. Individual
programs are usually put together into systems to
facilitate the analysis procedures, for example,
G-EXEC, ROKDOC, and NTSYS. NTSYS is a large
system of classiﬁcation programs developed by the
biometricians at the State University of New York
(SUNY), Stony Brook. ROKDOC was developed by
geologists at Reading University in England, and
G-EXEC has already been described.

Few techniques have been speciﬁcally developed
for solving geological problems. However, one such
set of techniques, regionalized variables, was de-
veloped by the French school of geostatistics headed
by George Matheron.

Many examples could be cited of the successful
application of statistical techniques to exploration
and exploitation problems. For the most part, these
techniques are applied to problems within the 19th-
century context of “cause and effect.” That is, the
techniques could have been applied years ago, if
it had been practical to do the calculations by hand.
Even so, their application now has not been without
positive effect, and here are a few examples.

The ﬁrst used and probably the most successful
technique has been trend analysis. Trend surfaces
are used to separate map data into two components
—regional and local. In structural geology, trend
surfaces can be used to simulate regional dip of beds;
the resulting residuals correspond to local structural
highs and lows. The anomalous areas thus are em-
phasized by removing the regional dip. The tech—
nique has been used especially in petroleum explora-
tion in areas of low dip, where local highs, masked
by regional effects, may serve as petroleum traps.

Harmonic analysis was used by Agterberg and
Fabbri (1973) to determine that the pattern of clus-
ters of copper and gold occurrences on the Canadian
Shield are more or less equally spaced. The copper
deposits were shown to coincide with geological
structures of one age, and the gold mineralization
was associated with features of another age. This
technique was used also to demonstrate that algal
limestone buildups were formed at approximately
equal intervals in the Pennsylvanian seas of Kansas.
These buildups occur in the subsurface and are of
interest because they may serve as possible petro-
leum reservoirs (Merriam and Doria-Medina, 1968).

 
Effective use of cluster analysis of geological data
of tungsten deposits of North America has been
made (Collyer and Merriam, 1973). This particular
study was traditional in the sense that the tech-
nique was used to evaluate a “cause and effect” re—
lationship; that is, which deposits formed in a simi-
lar environment. Analysis of the clusters of deposits
with similar attributes emphasized subtle or unrec-
ognized relationships in the original data. Once these
attributes were determined, they could be used in
exploring for similar deposits. Because nonnumeric
data can be used in this type of study, the technique
offers promise in utilizing historic records. A similar
analysis was made for 30 base—metal mining districts
in the United States by Joe Botbol (1971) of the
U.S.G.S.

Factor analysis is a technique which displays data
in a simpliﬁed and condensed form. It is used to
determine structure within a complex interrelation-
ship of variables. Factor analysis has been used ex-
tensively with geochemical data (Miesch, 1969), and
a factor-analysis exploration model was proposed by
Ed Klovan (1968), a model in which factor scores
would be mapped and favorable areas projected from
the coincident patterns of known occurrences.

Discriminant analysis has been used by John Grif-
ﬁths (1964) to identify petroleum—producing from
nonproducing sandstones. The technique can be used
to assign unknown samples to previously deﬁned
groups.

Many techniques are presently being tested to de-
termine their range of applications and limits with
geological data. The Geological Survey can do much
to foster development of new techniques for analyz-
ing geological data. Work along this line is proceed-
ing, and the Survey is publishing results. These
publications should be increased and made more
readily available, as they constitute the only series
of this type in the United States. I would like to sug-
gest that the Survey take the responsibility in serv—
ing as a clearing house for computer programs, in
the framework of GEOCOMP as proposed by John
Harbaugh (1964), and as the Kansas Survey did so
admirably during the mid- and late 19608. This func-
tion could well come under the aegis of the US.
Center for Geoscience Data. I would encourage
the Survey to consider making their network of
computers available to the geological public. Just
imagine some of the results in teaching and research
if such access could be arranged! This possibly could
be the forerunner of a national hookup having many
remote terminals distributed around the country and
operated on a basis similar to the Dartmouth system.

 
RESOURCE AND ENVIRONMENTAL DATA ANALYSIS 43

EDUCATION

Universities are responding—albeit slowly‘——to the
needs of the modern computer world. Computers are
introduced at an early stage in education, sometimes
in high school, and certainly in university—usually
in the ﬁrst year. Mathematics and statistics are
taught and used in geology courses. Many textbooks
on geomathematics and computer applications now
are available. Most universities have at least one
numerically oriented faculty member. Computers are
readily accessible and economical (at least they are
for users in the university where generally they are
free), and of course they are easy to use! However,
despite all the activity, only about 10 percent of the
geology students in this country are exposed to
computer-oriented courses in university. More and
more the interdisciplinary approach to problem solv-
ing is being stressed.

Professional geologists can take advantage of the
published literature, take night classes and short
courses, or attend any of the many workshops,
seminars, conferences, and chautauquas that are held
throughout the country each year.

Communication and the handling of the published
literature is an increasingly difﬁcult problem. Some
2 million items have been published in geology, and
that number is increasing at a rate of about 100,000
items per year. This means that the geological liter-
ature is doubling every 6 to 7 years (Lea, 1972).
No geologist, no matter how fast he can read, can
possibly keep up with more than a fraction of the
total publications. In fact, it may be difﬁcult to keep
up in his own ﬁeld. Greater dependence then is
placed on the bibliographies, current-awareness j our-
nals, and such services as GEO - REF. GEOCOM
Bulletin and GEOCOM programs for the computer-
oriented geologists are available through Geosys-
tems in London. The International Association for
Mathematical Geology is an active organization, and
membership is open to anyone interested in mathe-
matical geology or computer applications. The As-
sociation publishes a quarterly journal (which in
1975 becomes a bimonthly) and a newsletter. In
addition to all the other sources of information, a
new journal, “Computers and Geology,” starts in
1975.

The US Geological Survey is making a contribu-
tion to the national reference scheme in supporting
GEO - REF. In addition to support for indexing pub-
lished material, I suggest that it would be in the
national interest to establish a US. Index to Geo-
science Data. The index, patterned after the Cana-
dian index, would include all sources of geoscience

 
data, including computer-based ﬁles, published liter-
ature, unpublished open-ﬁle reports held by govern-
ment agencies, and relevant public documents. The
index would identify original observations and
measurements, but it would not abstract literature.
The production of the index would be part of the
US. Center for Geoscience Data.

SUMMARY

This summary of “Resource and Environmental
Data Analysis” has been, of necessity, short and
much abbreviated. Emphasis has been placed on the
“resource,” but many of the generalities and sum-
maries could serve the “environmental” aspect of
data analysis equally well. Although many problems
lie ahead, I look for geologists to meet their respon-
sibilities and commitments with foresight and in-
genuity. The future looks bright for the Geological
Survey as it continues to fulﬁll its role as the or-
ganizational leader in American geology.

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Agterberg, F. P., Chung, C. F., Fabbri, A. G., Kelly, A. M.,
and Springer, J. S., 1972, Geomathematical evaluation
of copper and zinc potential of the Abitibi area, Ontario
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Agterberg, F. P., and Fabbri, A. G., 1973, Harmonic anal-
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Montreal, Sec. 16, 222 p.

Berner, H., Ekstrom, T., Lilljequist, R., Stephansson, 0.,
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Berry, W. B. N., 1972, An automated system for paleon-
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Botbol, J. M., 1971, An application of characteristic anal-
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Spec. Vol .12, p. 92-99.

Buller, J. V., 1972, Development of the Saskatchewan com-
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44 EARTH SCIENCE IN THE PUBLIC SERVICE

Burk, C. F., Jr., 1972, Storage and retrieval of geological
data in Canada: Earth-Sci. Rev., v. 8, no. 1, p. 153—
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Calkins, J. A., Kays, 0., and Keefer, E. K., 1973, CRIB—
The mineral resources data bank of the U.S. Geologi-
cal Survey: U.S. Geol. Survey Circ. 681, 39 p.

Collyer, P. L., and Merriam, D. F., 1973, An application of
cluster analysis in mineral exploration: Internat. As-
soc. Math. Geology Jour., v. 5, no. 3, p. 213-223.

Conley, C. D., and Hea, J. P., 1972, A lithologic data-re—
cording form for a computer-based well-data system:
Internat. Assoc. Math. Geology Jour., v. 4, no. 1, p.
61—72.

Cutbill, J. L., ed., 1971, Data processing in biology and
geology: London-New York, Academic Press, 346 p.
Dimitriu, Alexandru, and Dumitriu, C., 1973, Geologic data
processing in Romania: Internat. Assoc. Math. Geology

Jour., v. 5, no. 3, p. 313—318.

Dixon, C. J ., 1970, Semantic symbols: Internat. Assoc. Math.
Geology Jour. v. 2, no. 1, p. 81—87.

1971, Machine language for representation of geologi-
cal information, in Data processing in biology and
geology: London-New York, Academic Press, p. 123—134.

Drew, L. J., 1974, Estimation of petroleum exploration suc-
cess and the effects of resource base exhaustion via a
simulation model: U.S. Geol. Survey Bull. 1328, 25 p.

Forgotson, J. M., Jr., and Stark, P. H., 1972, Well-data ﬁles
and the computer, a case history from northern Rocky
Mountains: Am. Assoc. Petroleum Geologists Bull., v.
56, no. 6, p. 1114—1127.

Gilliland, J. A., and Grove, G., 1973, Some principles of
data storage and information retrieval and their im-
plications for information exchange: Internat. Assoc.
Math. Geology Jour., v. 5, no. 1, p. 1—10.

Gover, T. N., Read, W. A., and Rowson, A. G., 1971, A
pilot project on the storage and retrieval by computer
of geological information from clored boreholes in
central Scotland: Inst. ‘Geol. Sci. Rept. 71/13, 30 p.

Grifﬁths, J. C‘., 1964, Statistical approach to the study of
potential oil reservoir sandstones: Stanford Univ. Pubs.
Geol. Soc., v. 9, no. 2, p. 637—668.

1968, Operations research in the mineral industries,
in Proceedings of a symposium in decision-making in
mineral exploration: Vancouver, Univ. British Columbia,
p. 5—9. _

Griﬂiths, J. C., and Singer, D. A., 1973, The Engel simulator
and the search for uranium, in Application of computer
methods in the mineral industry: South Africa Inst.
Mining and Metallurgy, p. 9—16.

Harbaugh, J. W., 1964, Computer pool may help geologists:
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Harris, D. P., 1969, Alaska’s base and precious metals re-
sources; a probabilistic regional appraisal: Colorado
Sch. Mines Quart, v. 64, no. 3, p. 295—328.

Harris, D. P., and Euresty, D., 1969‘, A preliminary model
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Harris, D. P., Freyman, A. J., and Barry, G. S., 1971, A
mineral resource appraisal of the Canadian Northwest
using subjective probabilities and geological opinion,
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Hubaux, Andre, 1969, Archival ﬁles of geological data: In-
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Kent, H. C., 1972‘, Computer-based information bank for
foraminiferal data, Western Interior Region, North
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Laurin, A. F., Sharma, K. N. M., Wynne-Edwards, H. R.,
and Franconi, A., 1972, Application of data processing
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Lea, G., 1972, GEO-ARCHIVE; an information retrieval
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die tendencias pollinomias y de Fourier aplicados a la
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Bol., v. 8, no. 1, p. 59—74.

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lithologic—log data to numbers for use in the digital
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EARTH SCIENCE IN THE PUBLIC SERVICE

NEW DIRECTIONS IN TOPOGRAPHIC MAPPING

By JAMES L. CALVER
State Geologist, Virginia Division of Mineral Resources

We are asked to consider a product of engineering,
the topographic map, that has become a funda-
mental, indeed an essential, tool in our society. It
has won this important use in local, regional, state,
and national levels from its unique ability to serve
basic-planning and decisionmaking problems that
confront all levels of society, from the individual to
the most complex group within industry and gov—
ernment. This accurate and up-to-date graphic rep-
resentation of natural and manmade features por-
trays location, shape, and elevation of plains, hills,
mountains, valleys, rivers, and lakes, as well as
roads, buildings, dams, mines, quarries, towns, and
cities.

The primary goal of the National Topographic
Mapping Program has been to complete the 1 224,000
quadrangle map series of the 48 conterminous States
and Hawaii. This objective was accomplished for
Virginia in 1972 through a 10-year cooperative ef-
fort between the US. Geological Survey and the
Commonwealth of Virginia. Virginia now has an ac-
curate and consistent base to which a variety of cri-
tical information can be related and combined for
decisionmaking. Although the national goal is to
have such coverage for all States, individual States
may shorten the time period for such coverage by
entering into a cooperative ﬁnancial agreement with
the US. Geological Survey.

The primary reason for a State geological survey
to become interested in topographic maps is to ob—
tain an accurate base on which to depict geological
formations and mineral resources and to show physi-
cal features. Through expanded technology and a
signiﬁcant shift toward increased involvement by
individuals in such activities as energy and resource
exploration and development, land-use planning, en-

46

 
vironmental protection, urban development, reclama—
tion projects, and outdoor recreation, new and some—
what specialized products have been derived from
the topographic mapping process. The US. Geologi-
cal Survey has recognized the importance of these
new approaches and has developed new products
that can complement topographic maps and that ﬁll
some of the needs of urban planners and other spe-
cialists. Urgent and demanding needs have brought
about a product known as the orthophotoquad as a
complement for line maps; used in combination with
a standard quadrangle map, it will provide the detail
of a photograph. These rectiﬁed photographs make
possible direct measurements at the scale of 1:24,-
000, and provide information in photographic detail
that is not portrayed on conventional quadrangle
maps. Land use and the differentiation of coniferous
from deciduous trees can be interpreted from them.
Orthophotoquads are of such importance that the
US. Geological Survey has proposed a 3-year plan
to have all the country’s unmapped areas, except
Alaska, photographed and have orthophotoquads
available for sale. In Virginia, 11 orthophotoquads
of growth areas have been received recently, and 15
others are awaiting printing.

Demand for orthophotoquads has been accelerat-
ing, and Robert Lyddan, Chief of the Topographic
Division of the US. Geological Survey, has informed
me that cooperative programs for their preparation
are underway with Connecticut, Nevada, New York,
North Carolina, and Virginia, that orthophotoquads
are in preparation for the entire State of Arizona,
and that the Bureau of Indian Affairs and the Soil
Conservation Service are cost sharing with the US.
Geological Survey for orthophotoquad preparation.

Orthophotomaps, another product, combine the
features of orthophotoquads and topographic maps

NEW DIRECTIONS IN TOPOGRAP‘HIC MAPPING 47

and show, by using color tones, wetlands and vege-
tation differences. The Dismal Swamp and Wacha-
preague areas in Virginia are being prepared in this
form.

Of speciﬁc interest are two relatively new prod-
ucts, the slope map and the land-use classiﬁcation
map. The ﬁrst of these is a valuable tool for land—
use planning and portrays various slope zones of the
terrain. Such maps are prepared by mechanical
techniques from the contour plate of standard topo-
graphic maps. Classiﬁcation of land into zones of
slope may be elementary to users of topographic
maps, but to individuals who have little or no train-
ing in engineering or geology, a slope-classiﬁcation
map is more readily understood and is a usable item.
These maps may ﬁnd great use by legislators as a
quantitative aid in making land-use decisions.

Land-use classiﬁcation maps have become a de—
sirable product. Interpretation and delineation of
land—use information in conjunction with the pro-
duction and revision of standard topographic maps
in Virginia has met with the acceptance of indi-
viduals interested in current use of the land and
planning for future uses. Land-use inventory has
been overprinted in four 71/2-minute orthophoto—
quads in the Fredericksburg, Va., area. Certainly
more such information will be required in the future.
It is our opinion that such maps should be made
for each 71/2-minute quadrangle. In urban areas in
Virginia where there is an update schedule for re-
vision every 5 years, such maps would be of great
value to local and regional planning groups.

Eight states have land-use-mapping programs
utilizing ERTS data and high—altitude photography
(Alabama, Colorado, Maryland, Mississippi, Ne-
braska, Rhode Island, South Carolina, and Ten-
nessee).

To implement an efﬁcient revision program to
keep the topographic maps up to date, Virginia has
been divided into ﬁve sectors of approximately equal
size; one sector is ﬂown each year to produce quad-
centered mapping photographs. These are enlarged
three times and compared with the existing printed
quadrangle. This comparison is an eﬁ‘icient way to
determine cultural changes and to schedule priori-
ties for updating the topographic maps. A quad-
centered photograph replaces a mosaic of perhaps
nine or more mapping photographs formerly needed
to depict the area of a 71/é-minute quadrangle. These
photographs are available for more than half the
805 Virginia quadrangles, and the remaining are
scheduled within the updating program. Those maps
selected to be photorevised depict growth features

 
in purple; to date about 25 percent of the Virginia
quadrangles has been revised. This aerial photo-
graphy as a sales item from the US. Geological
Survey is an important byproduct of the mapping
program.

Intermediate-scale maps are in demand and Vir-
ginia is giving consideration to a county series at
1:50,000 scale. This scale is easily convertible to the
metric system and will ﬁll the present needs as well
as lessen the future impact caused by this country’s
adoption of the metric system. Careful consideration
should be given to converting all the present 71/2-
minute quadrangle series from 124,000 to 125,000
scale. Consideration should likewise be given to
1:50,000- and 1:100,000-scale intermediate or
county— or regional-format maps. Such intermediate-
scale maps need to be designed so that they would
be suitable for enlarging or reducing for use by
planners and engineers.

I would like to spend a few minutes considering
several items that would make a good product even
better. It is necessary to keep up-to-date State cov-
erage at several scales, the graphics of which could
take one—half reduction. A program should be ex-
panded to make mapping expertise available perhaps
on a consulting basis to public bodies for large-
scale mapping and to assist public agencies in the
selection of a common scale for mapping. Other
improvements would be to locate all routes of access
such as trails and former roadways; to annotate all
benchmarks; to correctly identify all public-use
boundaries, especially those of the United States
forests; to differentiate pipeline commodities; to
identify river miles for the plotting of hydrologic
data; to keep information at the same date that is
used for county maps or maps that have scales of
1:50,000 or 1:100,000; to better annotate restric-
tive land-use areas, such as hospitals, churches,
cemeteries, military areas, actual forest boundaries,
and airports; to identify all public recreation areas
such as parks, forests, game management tracts,
parkways, and so forth; and to develop physical and
cultural map information in digital form.

If such improved maps were available, there
would be more meaning in the present topographic
mapping goals. Brieﬂy speaking, these goals are:
to keep up to date the 1224,000- 1:250,000- and
1:500,000—scale map series; to have orthophoto—
quads, slope maps, orthophotomaps, and county
maps made for areas of demand; to inform the pub-
lic of map availability and uses by means of press
releases, mail-outs, displays, and conferences, and to
provide a communications link between the map-

48 EARTH SCIENCE IN THE PUBLIC SERVICE

maker and the user; to identify map needs; and to
advertise byproducts such as aerial photographs,
stable base copies, stable base copies of color separa-
tion plates, and geodetic control.

Who are the users of topographic maps? The early
development of topographic mapping had a close link
with the need for an adequate base on which the
geology of an area could be depicted. New groups
have found uses for the topographic map that ex-
ceed those of the geologist, even though his require
ments have expanded to include detailed magnetic,
gravity, and seismic data as well as stratigraphic,
rock-type, mineral-resource, and surface- and
ground-water data. Every individual is a potential
user; at present his greatest use of the map is for
recreation, including hunting, ﬁshing, hiking, camp-
ing, and vacationing. State agency uses throughout
the country have increased. In Virginia, the Divi-
sion of Mineral Resources utilizes topographic maps
as bases for geologic maps and mineral-resource
maps, and for benchmark data. The Division of
Mined Land Reclamation uses the maps in delineat-
ing areas to be strip mined and to be reclaimed,
and the Division of Forestry uses them in ﬁre-con-
trol access and in the control and determination of
insect infestation. The Division of Industrial De-
velopment uses the maps as graphic aids for depict—
ing potential industrial build-ing sites, the Depart-
ment of Taxation utilizes enlargements as an aid
for delineating properties, and the Game and Inland
Fisheries Commission uses the maps to prepare
sportsman guide maps on which campsites, picnic
areas, and boat ramps are annotated. The Depart—
ment of Highways utilizes the maps in planning
new roadways. The Ofﬁce of Emergency Prepared-
ness maintains a ﬁle of 71/2-minute quadrangle maps
to aid victims of natural hazards. The Outdoor Rec-
reation Commission maintains up-to-date map ﬁles
to locate and keep an inventory of recreational fa-
cilities, and the Historical Landmarks Commission
makes an annotation of buildings that are on the
National Register. Regional planning districts util-
ize the 71/2-minute series for an inventory of natural
and cultural features and for land-use plans. City
and county planners and engineering departments
use the maps as an aid in the development and ex—
pansion of public utilities as well as to portray vari-
ous factors of environmental interest. Policemen,
county sheriffs, ﬁremen, and rescue squads utilize-

 
the maps to shorten the response time in answering
emergencies. Public schools ﬁnd the maps invaluable
in courses on geography and land-use planning.
Land surveyors, realtors, and transmission com-
panies have asked our organization for assistance,
including questions on the availability of aerial
photographs and topographic maps.

One hesitates to mention quality control in such
an overall excellent product, but inadequate depic-
tion of public ownership of land has become a vexing
and frustrating problem. In Virginia, our National
Forests are not recorded properly, and the bound-
aries as shown are erroneous and misleading. Con-
sider a standard 71/2-minute quadrangle, half of
which is designated as National Forest; however,
within that 30-square—mile area, all the land is in
private ownership. Not even 1 acre is owned by the
National Forest. Further, consider the confusion of
the poor hunter who is confronted with no-trespas-
sing signs on land indicated on the map as National
Forest. Also consider the frustration of the property
owner who pleads with us to have correct boundary
information on the map. The answer that the land
lies within a proclamation boundary or a land ac-
quisition boundary of the National Forest is of no
help. These individuals become distrustful of an
otherwise excellent product. If speciﬁcations do not
allow accurate boundaries of forest lands and other
public-use lands, the question will be raised over and
over again—for Whom are the maps being prepared?

Within the past few years a new and imaginative
system has been developed to use various types of
imagery in small-scale mapping. Such images have
attracted serious investigators by offering the op-
portunity to monitor temporal changes through re-
petitive observations. Certainly users who are con-
cerned with land-use analysis have welcomed the
color composites derived from the spectral band of
ERTS—l imagery. The images now available have a
ﬁtted Universal Transverse Mercator grid and a
1:500,000 scale. The map of tomorrow may be a re
ﬁnement of such images. Technical advances that
would make possible even greater resolution than
exists today will become tomorrow’s commonplace
method for making large—scale maps. Aerial photo-
graphs will be replaced by satellite and airborne
imagery, just as alidades and plane tables were re-
placed by photographs and electronic measuring de-
Vices.

EARTH SCIENCE IN THE PUBLIC SERVICE

 
GEODYNAMICS

By CHARLES L. DRAKE
Department of Earth Sciences, Dartmouth College

INTRODUCTION

Almost 200 years ago, Benjamin Franklin (1782),
after some geological observations, wrote to Abbé
Soulavie in France
Such changes in the superﬁcial parts of the globe seemed
to me unlikely to happen if the earth were solid to the
centre. I therefore imagined that the internal parts might
be a ﬂuid more dense, and of greater speciﬁc gravity than
any of the solids we are acquainted with; which therefore
might swim in or upon that ﬂuid. Thus the surface of the
globe would be a shell, capable of being broken and dis-
ordered by the violent movements of the ﬂuid on which it
rested.

Franklin thus anticipated the Geodynamics Proj-
ect and the plate-tectonics model that has caused a
revolution in geological thought during the last dec-
ade.

Franklin continued, ,

If (these thoughts) occasion any new inquiries and pro-
duce a better hypothesis, they will not be quite useless. You
see I have given a loose to imagination; but I approve
much more your method of philosophizing, which proceeds
upon actual observation, makes a collectiOn of facts, and
concludes no farther than those facts will warrant.

Here I believe that Franklin is anticipating the
existence of the US. Geological Survey and is put-
ting his stamp of approval on the methodology that
has been in its tradition since the days of John
Wesley Powell. This tradition has served the coun-
try well, as have the many distinguished geologists
of the Survey, past and present. Of special import-
ance has been the interplay of ideas, the interchange
of people, and the coordination of efforts between
the Survey and the academic community, a part of
this tradition that has been of mutual beneﬁt to all
parties and that should be continued and strength-
ened in the future.

 
THE GEODYNAMICS PROJECT

The roots of the Geodynamics Project are of some
age, pregeological phylloxera, so to speak, and drew
nourishment from the rich organic topsoil of geo-
logical speculation. Speculation on the origin of the
surface features of the Earth, the causes of natural
disasters, and the reasons behind economic emplace-
ment of mineral deposits and hydrocarbons has a
long and varied history. The ideas were many, but
the data necessary to substantiate or repudiate these
ideas were few.

Early ideas about the origin of the surface fea-
tures of the Earth were many and often bizarre,
but no more so than the model that we ﬁnd most
acceptable today. This model aSsumes that the
Earth’s outer shell consists of a small number of
large lithospheric plates that, as suggested by Frank-
lin, are decoupled from the underlying substratum
and move relative to one another, colliding along
the young mountain systems, separating along the
midocean ridge system, and sliding relative to other
plates in regions such as that of the San Andreas
fault system in California. Development of this
model was less a question of establishment of new
ideas as it was one of collecting and analyzing data
that would allow selection from among many ideas.

The basic data were in three areas. The ﬁrst re-
lated to the concept of a rigid lithosphere overlying
a more plastic asthenosphere. This concept had
many adherents, Barrell (1914—15) and Daly (1914)
especially, who concluded on the basis of geodetic
and petrologic grounds that the asthenosphere was
either liquid or glass. Beno Gutenburg (1926) in the
1920’s, took full advantage of inadequate data from
the propagation of body waves through the Earth
and concluded that a low-velocity layer existed at

49

50 EARTH SCIENCE IN THE PUBLIC SERVICE

depth, a conclusion that was subsequently substan-
tiated by studies of surface-wave dispersion when
modern electronic computers became available. Hugo
Benioff (1949) added to the concept through his
studies of the energy release from South American
earthquakes during the ﬁrst half of this century. He
found a large change in the rate of energy release
of intermediate— and deep-focus earthquakes during
the 1920’s that was not reﬂected by the shallow-
focus earthquakes. This led to the conclusion that
the outer shell of the Earth was decoupled from the
interior. More recently, Joe Boyd of the Geophysical
Laboratory, Carnegie Institution, and Peter Nixon
of the Department of Mines, Lesotho (Boyd and
Nixon, 1973), have come up with what they suggest
is the ﬁrst direct evidence of a less competent as-
thenosphere through studies of rocks blasted out of
kimberlite pipes in southern Africa. From experi-
mental petrology, geological thermometers and bar-
ometers have been devised that allow equilibrium
samples of certain rock types to be related to depth
and temperature. From studies of the rocks from the
kimberlite pipes, Boyd and Nixon (1973) were able
to sort out the deep stratigraphy of the lithosphere
and the upper asthenosphere. Their results indicate
a jump in the thermal gradient at depths of about
150 km beneath South Africa, a jump that may be
related to mechanical heat sources. Further, the
rocks from depths greater than this jump are
sheared, whereas those from above are crystalline.
It should be noted that objections to this relatively
simple picture have been raised both by geochemists
and geophysicists. Nevertheless, the body of data
that exists to date supports the ﬁrst idea espoused
by Franklin that beneath a rigid outer shell is a layer
that is dense and ﬂuidlike on which the outer shell
swims.

Franklin’s second thought, that this outer shell
was capable of being broken and disordered by the
motions of the underlying liquid, was followed by
the concept of continental drift. This has had a long
and checkered history, beginning with Snider in
1858, and had an early culmination in Wegener’s
classic presentation in 1915. This culmination was
premature, however, because many objections were
raised to the concept, particularly with regard to the
driving mechanism and the mechanics of the sys—
tem, but also on emotional grounds because the con-
cept was so fantastic. When paleomagnetic data in
the 1940’s and 1950’s revealed consistent polar-
wandering tracks for the individual continents and
diverging tracks among the continents, the contro-
versy was renewed. It remained a controversy until

 
further magnetic work coupled with marine investi-
gations and Deep Sea Drilling Project results led to
the seaﬂoor-spreading idea. This idea was based
ﬁrst on the time sequence of reversals of the mag-
netic ﬁeld established by Cox, Dalrymple, and Doell
(1967) of the US. Geological Survey in Menlo Park,
and second on the correlation, by several investiga—
tors, of this reversal sequence with the linear mag-
netic anomalies that parallel the midocean ridges.
This correlation suggested that new crust was being
formed at the axes of the midocean ridges and was
moving laterally away from the axes at rates of a
few centimetres per year, a conclusion borne out by
basement ages determined by the Deep Sea Drilling
Project. These ﬁndings did not solve the mechanism
problems; they bypassed it by demonstrating that
movements similar to continental drift had taken
place. Marshall Kay likes to cite Ayer’s Law in cases
like this, which states “Things that have happened,
can happen.”

Now Franklin did not, apparently, conceive of the
Earth as expanding, but if we create new crust at
the ridge axes, we either have to expand the Earth to
ﬁt it in, or we must somehow get rid of old crust.
This problem was resolved by the seismologists.
Most of the earthquakes of the world occur at shal-
low depths—less than 70 km. The exceptions are
found in the areas where young mountain systems
and island arcs are found—around the Paciﬁc and
in a belt extending from the East Indies to the Medi-
terranean. Deep-focus earthquakes were ﬁrst noted
by Turner in 1922,'and Wadati in 1935 showed that
in the Japanese region they dipped on a plane from
the Nippon trench to beneath the continent in China.
Benioﬁ‘ in 1954 demonstrated that this was the case
in the entire circum-Paciﬁc region. Isacks, Oliver, and
Sykes (1968) studied the Tonga region in detail and
found evidence that the outer shell of the Earth, the
lithosphere, was being underthrust to depths of at
least 700 km. Thus, old lithosphere—old oceanic
crust—was being returned to the deep mantle and
reassimilated and at rates comparable with the rates
of generation of new crust at the oceanic ridges.
This was true in most areas around the Paciﬁc, a
prime exception being California, where the two
plates slide along each other, producing shallow
earthquakes of often devastating character.

Thus Franklin’s concept has grown into the plate—
tectonics model, a model that evolved during the
Upper Mantle Project, an international project de-
signed to study the outer 1,000 km of the Earth’s
crust and upper mantle. The signiﬁcance of the
model was not lost on the scientiﬁc community, and

 
GEODYNAMIC‘S 51

it resulted in the establishment of the Geodynamics
Project, sponsored by the International Council of
Scientiﬁc Unions at the urging of the International
Union of Geodesy and Geophysics and the Interna-
tional Union of Geological Sciences, to which more
than 50 countries have subscribedX'lThe program is
strongly based upon the plate-tectonics model, be-
cause it is the most promising model to date, and
its purpose is to study the dynamics and the dynamic
history of the Earth. A program for United States
' participation by Government agencies, academic in-
stitutions, and industry was designed by a commit-
tee of the National Academy of Sciences (Natl.
Acad. Sci., Geodynamics Comm, 1973), with the aid
of some 200 correspondents and advisors; a com-
mittee, which includes the US. Geological Survey as
a principal participant, has been established by the
Federal Council on Science and Technology to co-
ordinate the Federal program.

THE FUTURE

If we look to the future, we can see opportunities
both in terms of basic science and in terms of prac-
tical consequences of a better understanding of the
dynamics of the Earth. Let me give a few examples.
We have managed to bypass temporarily the ques-
tion of the driving mechanism for plate tectonics by
demonstrating indirectly that large horizontal move-
ments of the lithosphere have taken place. Many
models have been proposed, but we are hampered
by the lack of boundary conditions—good physical
and chemical parameters for the materials deep
within the Earth. This is an area in which there are
many opportunities for pioneering work.

Our present model for the movement of the plates
is essentially that proposed by Wegener in 1915. It
is excellent on a large scale, but inconsistencies on
smaller scales must be resolved if the model is to be
useful geologically. For example, if the Atlantic is
closed completely, we are faced with serious over-
laps of ancient rocks in Central and South America
that must somehow be accounted for. Resolution of
this and similar problems will require careful analy-
sis of the onshore and offshore data into a coherent
picture.

The model also assumes that the plates are rigid;
yet there is both geodetic and geological evidence for
vertical movements at rates comparable with the
horizontal movements, that is, centimetres/year,
within the plates. The apparent rates decrease by
orders of magnitude as the length of time over
which they are measured increases, which suggests
that the vertical movements are oscillatory. Both the

 
Geological Survey and NOAA are involved in the
study of these vertical movements, through geologi-
cal and geodetic investigations, and I can think of
no efforts that are likely to be more fruitful than
efforts in this area. Not only is it important scientiﬁ-
cally to see whether or how these vertical move
ments are related to the major horizontal move-
ments, but most of the hydrocarbons of the world
have accumulated in areas that have been affected
by these vertical motions. The petroleum industry
has taken a very strong interest in the model. The
search for hydrocarbons is focused upon structures
that might trap them rather than upon oil and gas
directly; thus, the best knowledge of the dynamic
history of the Earth, the rates of motion and the
accelerations and decelerations of these motions, will
yield the most accurate structural interpretation.

Recent studies of earthquakes by investigators
from academic institutions and from the Geological
Survey have led to plausible models for the initia-
tion of major tremors. These models suggest that
forerunners of such tremors may allow more ac—
curate prediction of major events than has been the
case in the past. As long as the lithospheric plates
move relative to one another, earthquakes will take
place, but it is not inconceivable to imagine that the
stored energy might be released gradually rather
than suddenly, thus mitigating the damage. A criti-
cal unknown is the cause of major earthquakes in
plate interiors, such as the ones in New Madrid,
Mo., Boston, Mass, and Charleston, SC. These were
very large earthquakes, but unlike those in the
circum-Paciﬁc region, they have no obvious relation-
ship to the interplate reactions and perhaps are
related to the recent vertical movements within the
plates mentioned earlier.

In recent years, identiﬁable relationships have
been indicated between the plate-tectonics model
and the occurrence of major ore deposits. In the Red
Sea and Salton Sea areas—regions of diverging
plate boundaries—metal-rich brines and sediments
have been found. High metal contents have also been
found in other parts of the ocean ridge system.
Again, it is not inconceivable that metal concentra-
tions may accompany the formation of new crust at
the ridge axes, that these move laterally with time,
and that a distillation process in the underthrusting
areas concentrates these metals into exhalative, vein,
or porphyry deposits. As most of the metal deposits
with readily identiﬁable surface manifestations
have already been identiﬁed, it is not unreasonable-
to conclude that the future lies with those who have
the best understanding of the dynamic history of

52 EARTH SCIENCE IN THE PUBLIC SERVICE

the Earth. Dan Merriam pointed out at the dedica—
tion that new approaches are also needed, but these
must be combined with the best genetic models.

New tools and approaches will play an important
role in this project. The Deep Sea Drilling Project
has been an exciting and scientiﬁcally productive
program that has enormously increased our knowl-
edge of the geology of the ocean basins. Much more
remains to be learned from further detailed study of
the cores in the archives. Similarly, deep drilling for
scientiﬁc purposes on the continents, combined with
very deep penetration reﬂection studies, promises to
be equally revealing. A panel established at the insti-
gation of the US. Geodynamics Committee and sup-
ported by the Carnegie Institute of Washington has
studied this problem and has made far-reaching
recommendations. Several sources have shown en-
thusiasm for a continental drilling program, and it is
inconceivable that such a program could be imple-
mented without major participation from the US.
Geological Survey.

Of equal signiﬁcance is the opportunity that ex-
ists for reevaluation and synthesis of existing geo-
logical data on the continents in light of the new
model. Most of these data were collected and inter-
preted prior to the development of the new model,
and the reevaluation will not only have beneﬁcial
scientiﬁc and practical consequences, but it will also
identify critical areas that deserve additional study.
This observation provides an opportunity to offer
strong encouragement to basic ﬁeld mapping. This
mapping provides the basic elements of all our geo—
logical knowledge. Without it we have no boundary
conditions. It is easy to lose sight of this When we
have black boxes, computers, aircraft, spacecraft,
ships, or other exciting things to work with.

The Geodynamics Project is not designed to ﬁnd
minerals or energy sources or to prevent natural
disasters. It is a project whose aim is to learn about
the dynamics and dynamic history of the Earth and
to provide basic knowledge that will contribute to
better utilization of the Earth’s natural resources
and to the mitigation of the effects of natural dis-

 
asters. As such, it clearly falls into the area of
responsibility of the Geological Survey. Many Sur-
vey scientists assisted in the design of the US. Pro—
gram (Natl. Acad. Sci., Geodynamics Comm., 1973),
and I look forward to continued Survey participation
in its implementation.

REFERENCES CITED

Barrell, Joseph, 1914—15, The strength of the earth’s crust:
Jour. Geology, v. 22, p. 28—48, 145—165, 209—236, 289—
314, 441—468, 537—555, 655—683, 729—741; v. 23, p.
27—44, 425—443, 499—515.

Benioﬂ’, V. H., 1949, Seismic evidence for the fault origin
of oceanic deeps: Geol. Soc. America Bull., v. 60, no.
12, pt. 1, p. 1837—1856.

1954, Orogenesis and deep crustal structure—ad-
ditional evidence from seismology: Geol. Soc. America
Bull., v. 65, no. 5‘, p. 385—400.

Boyd, F. R., and Nixon, P. H., 1973, Structure of the upper
mantle beneath Lesotho: Carnegie Inst. Washington,
Geophys. Lab. Ann. Rept, p. 431—445.

Cox, Allan, Dalrymple, G. B., and Doell, R. R., 1967, Re—
versals of the earth’s magnetic ﬁeld: Sci. Am., v. 216,
p. 44-45.

Daly, R. A., 1914, Igneous rocks and their origin: New
York, McGraw-Hill, 563 p.

Franklin, Benjamin, 1782, [Letter to Abbé Soulavie; read
at a meeting of Am. Philos. Soc., 21 Nov. 1788.]

Gutenberg, Beno, 1926, Untersuchungen zur Frage, bis zu
Welche‘r Tiefe die Erde Kristallin ist: Zeitschr.
Geophys, v. 2, p. 24—29.

Isacks, Bryan, Oliver, Jack, and Sykes, L. R., 1968, Seis-
mology and the new global tectonics: Jour. Geophys.
Research, v. 73, no. 18, p. 5855—5899.

National Academy of Sciences, Geodynamics Committee,
1973, US. Program for the Geodynamics Project—
scope and objectives: Washington, D.C., Natl. Acad.
Sci., 235 p.

Snider, A., 1858, La création et ses mysteres devoiles: Paris,
A. Franck et E. Dentu, 487 p.

Turner, H. H., 1922, On the arrival of earthquake waves at
the Antipodes and on the measurement of the focal
depth of an earthquake: Royal Astron. Soc., Monthly
Notices, Geophys. Supp, v. 1, p. 1—13.

Wadati, K., 1935, On the activity of deep-focus earthquakes
in the Japanese Islands and neighborhood: Geophys.
Mag. (Tokyo), v. 8, p. 30>5~325.

Wegener, A. L., 1915, Die Entstehung der Kontinente und
Ozeane: Braunschweig, F. Vieweg & Sohn, 94 p.

 
EARTH SCIENCE IN THE PUBLIC SERVICE

EARTH-RESOURCE SURVEYS

By GEORGE J. ZISSIS
Chief Scientist, Environmental Research Institute of Michigan

INTRODUCTION

In the summer of 1974 the world stands on the
threshold of a new, greatly increased ability to in-
ventory and monitor the Earth’s resources. It seems
especially appropriate to examine a few of the im-
plications of that ability on the occasion of this
dedication symposium, for the US. Geological Survey
has played a central role in bringing earth sciences
to bear upon our need for earth—resource surveys.

The aspects which I Wish to review brieﬂy involve
the development and application of remote-sensing
technology to the attainment of the vitally needed
resource data base. It is in this development and
application that the U.S.G.S. has pioneered. Together
with the National Aeronautics and Space Adminis-
tration (NASA), and many other Federal agencies,
the U.S.G.S. has created the knowledge needed to
exploit the capabilities of space-based and aerial
remote-sensing systems. Leading this activity
within the Department of the Interior has been the
Earth Resources Observation Systems Program.
Many persons come to mind as we think back over
the growth of this effort. Leading them all, I am cer-
tain, would be Dr. William T. Pecora, whose vigorous
support and wise guidance of the program was an
inspiration to all of us. Maintaining leadership in this
ﬁeld within the Department of the Interior has fallen
upon the capable shoulders of Dr. John DeNoyer,
and EROS still has the wisdom, insight, and counsel
of Dr. William Fischer.

The developments of which I speak are well doc-
umented in the literature, particularly in a com-
pilation of papers presented at the 13th Meeting Of
the Panel on Science and Technology, for the US
House Committee on Science and Astronautics (US
Congress, House, Comm. Sci. and Astronautics,
1972). Since then we have seen many of the results

 
of the ﬁrst Earth Resources Technology Satellite,
and even some from the Skylab Earth Resources
Experiments Package.

REMOTE-SENSING TECHNOLOGY

Remote sensing has now begun to appear in sev-
eral academic curricula; it is identiﬁed as measure-
ments remotely made by sensors not in direct con—
tact with the object of interest. Since its explicit
identiﬁcation as a ﬁeld of endeavor, about 12 years
ago, it has constituted an extension of the already
established and accepted practices in aerial photog-
raphy and ph‘otogrammetry, including the follow-
ing innovations:

1. Imaging from space platforms.

2. Imaging in the nonphotographic wavelength re—
gions, particularly the infrared and micro-
wave regions.

3. Attainment of quantitative nonimaging spectro-
radiometric measurements from space and
aerial platforms.

4. Data recording and transmission in high-density
electrical-signal form.

5. Establishment of signal- and data-processing
methodologies, analog and digital, to assist
human interpreters and to extract some in-
formation automatically.

6. Active (that is, illuminated) systems such as
radar and laser systems.

Thus, this ﬁeld has brought to bear the power of

modern computer, space, and electronic technologies.

Remote sensing has expanded our data-gathering

and information-producing capabilities and now is

engaged in enhancing translation from information
to meaningful decisions. The chain we must follow
can be visualized as:

53

54 EARTH SCIENCE IN THE PUBLIC SERVICE

DATA —> INFORMATION -> DECISION -> BENEFITS

The changes introduced are so radical that remote-
sensing technology can be viewed as a totally new
attainment, one greater than the sum of the sepa-
rate innovations.

Some general observations can be made on the
nature of this new technology. As it is heavily in-
volved with the use of information-gathering tools,
it can be deemed a passive technology, one whose
output is without value in itself. Thus, if our pro»
gress through the chain stops when information has
been produced, we will ﬁnd no “demand” in the eco-
nomic sense. As a ﬁeld, remote sensing is interdis-
ciplinary in an integrating sense. It is nearing large-
scale practical utilization. Although essentially
benevolent, remote-sensing technology can be mis-
used. This is dependent upon the decisions made.

Much of what we have just said could also be said
of “bugging” or so-called electronic surveillance.
Such use of implanted sensors for spying purposes,
whether industrial, political, or military, has had
strong and widely discussed repercussions. Illegal
phone tapping can be seen as a clear example of the
misuse of a passive technology. Concern has been
voiced internationally about the possible misuse of
remote sensing from satellites for earth-resources
surveys. Perhaps the most cogent treatment of this
topic was given by the NASA Deputy Associate Ad-
ministrator for Applications, Leonard Jaﬁ'ee (1974),
at the February 25—March 5, 1974, meeting of the
US. Outer Space Committee’s Working Group on
Remote Sensing.

The political aspects of earth-resources surveys
are thus as real as the technological ones and may
well be the pacing elements in the future of this
ﬁeld.

APPLICATIONS

The remarkably successful operation of ERTS—1
has allowed many investigators to demonstrate a
wide range of uses of this particular conﬁguration.
Applications which seem to be at hand, range from
mapping in the cartographic sense at scales on the
order of 1:500,000 or 1:250,000 to many areas of
broad thematic information extraction. One imme-
diate factor is the speed with which large areas are
covered. In almost an instant, the data for mapping
a 185- by 185-kilometre area can be obtained. In a
relatively short time, a State can be covered. The
resulting product is a map of things as they were at
one deﬁnite time, whereas a conventionally made
map may contain old and new information and may
represent things as they never were at any one
moment.

 
Extraction of information on the renewable and
nonrenewable resources has been treated in con-
siderable detail in NASA’s ERTS Symposium (U.S.
Natl. Aeronautics and Space Admin., 1974). Scien-
tists in the U.S.G.S. have made signiﬁcant presenta—
tions at these conferences. Monitoring and inven-
torying of agricultural products have been shown,
within some limitations, to be valid activities, al-
though they require ancillary data such as crop
calendars and so—called “ground truth.” The use of
ERTS data in disaster assessment and as an aid in
directing efforts to alleviate the effects of ﬂoods and
of drought have also been presented. Monitoring of
World Bank projects is an example of a perhaps less
known but practical use of ERTS imagery.

Time does not permit an adequate treatment of the
results already obtained and published. For example,
the activities in Canada and Brazil have been out-
standing. Taken altogether, they represent an ever-
growing truly global capability for use of space
sensors for earth-resource surveys.

RESEARCH

Research in the ﬁeld of remote sensing for earth-
resource surveys is particularly attractive. This has
seemed so obvious that we may have failed to articu-
late its merits properly. Recently, while in Indonesia,
I had occasion to try to do just that. The attributes
that came to mind were these. First, it is applied
research having clearly understandable useful goals.
Remote-sensing research attacks urgent world prob-
lems, among them those of ﬁnite resources of food
and energy. Second, the work is scientiﬁcally chal-
lenging. The intellectual rewards are, accordingly,
satisfying. Third, much of the research can produce
good results reasonably quickly. This is an important
attribute from the point of view of those seeking
thesis opportunities. Fourth, much of the research
work can be founded on and developed from a basis
of earth sciences. Participation in such research in—
evitably brings the scientist into invigorating en-
counters with computer and space sciences. Fifth,
and perhaps most important of all, this research
brings the researcher and the operational user di—
rectly together. This necessary and mutually beneﬁ-
cial partnership is an uncommon extension in inter-
disciplinary interactions, beyond what is normally
found in research. This attribute can be equally true
for all those who engage in remote-sensing research
—the earth scientist, the economist, the lawyer, the
agriculturist, or the political scientist. Of course, not
every program of study brings all disciplines to-

EARTH-RESOUCE SURVEYS 55

gether, but engagement in a series of such works
comes surprisingly close. These ﬁve characteristics
of remote-sensing research can be most relevant
for work by teams in less developed countries, but
they hold true for developed countries as well .

For example, one research area seeks to produce
land-use maps by automatic processing of remotely
sensed data. Our work at the Environmental Re-
search Institute of Michigan, typical perhaps of that
by several research workers in this ﬁeld, has met
with some success already. It involves participants
from the users at State government level as well
as our scientists. Such teamwork is both rewarding
and challenging.

Two other examples come to mind. Our research
in oil-slick detection began with laboratory spec-
troscopy and went through theoretical analyses and
creation of models of predictive calculations, to the
design of system concepts; we then worked with
the ultimate operational user of the system on costs
and reliability. The second example involves the
creation of theoretical and empirical models to allow
radiation-transfer calculations in real atmospheres
and within vegetation canopies. One capability of
these models is used for corrections to radiometric
multispectral data, the other for prediction and an-
alysis of such corrected data for forests and crops.
Again, the involvement with many parties of inter-
est is wide and, even today, growing. The quality
of the work is reﬂected in the scientiﬁc publications
that have resulted.

Much remains to be done, but this will always be
true in such ﬁelds of research. One frontier lies in
the attainment of resource-management models ca-
pable of efﬁcient acceptance of remotely sensed data.
Many gaps exist in our understanding of the connec-
tion between the remotely made measurements of,
say, spectral radiance as a function of wavelength
and the particular properties of the object being ex-
amined. Some applications remain just beyond our
sensor conﬁgurations. Researcher eagerly await
higher resolution multispectral systems having
wider spectral coverage and having the observational
advantages of geostationary platforms.

THE FUTURE

Dr. McKelvey’s letter of invitation to present this
paper stated that the purpose of this symposium
was “. . . to survey the public problems to which
earth science . . . should be addressed.” No one today
could resist such an invitation. One national issue is
clearly evident in the ﬁeld of earth-resource surveys.
We stand, as I said before, technically on the thres-

 
hold of attaining an ability to inventory and monitor
the Earth’s resources. Will there be a national de-
cision to cross that threshold?

Let us be very clear what is at stake here. Simply
having earth-resources surveys does not bestow
social and economic beneﬁts. Such surveys are merely
a step toward the decisions that can bring about a
wiser management of these resources. We cannot
take as an article of faith that better information
leads inevitably to better decisions. We can believe
that the likelihood of better decisions is increased
by having improved information. Indeed, the phrase
“necessary but not sufﬁcient” comes to mind.

The larger problem remains. It has been couched
in many different terms. One that comes to mind is
“distribution of wealth.” If we consider that all the
Earth’s resources —- human, natural, renewable,
nonrenewable, energy, water, food—apply what mod-
iﬁers you wish—all of these are the world’s wealth,
then we realize that the wealth is the world itself.
How shall we divide the world? What share shall we
leave for those to come? Will we consume the Earth,
or husband and cherish it, sharing this wealth evenly
with all humanity today and tomorrow?

Others have pointed to the need for stabilization——
stabilized population levels, stabilized quality of en-
vironment, stabilized growth rates. If we are to
achieve the global-management capability inherent
in such concepts, we must develop far more powerful
tools than mechanistic input-output management
models, however complex these may become. Here
the challenge is the creation of management tools
that include and are responsive to human values. I
suggest that this task is a social and political one.

The decision to cross the earth-resource surveys
threshold is similarly a political one, involving or at
least touching all countries. The international com-
munity of earth scientists cannot stand apart from
active participation in the decisionmaking process.
There is little time left—delay can mean the oppor-
tunity foregone. Not making a decision is as much
of a decision as is any other action.

REFERENCES CITED

Jaﬂ’ee, Leonard, 1974, [Statement at the UN Outer Space
Committee’s Working Group on Remote Sensing, 25
February 1974]: US. Dept. State Bull., Apr. 8, 1974, p.
376.

U.S. Congress, House, Committee on Science and Astron-
autics, 1972, Remote sensing of earth resources. A com-
pilation of papers prepared for the 13th meeting of the
Panel on Science and Technology—1972: Washington,
US. Govt. Print. Off., 224 p.

56 EARTH SCIENCE IN THE PUBLIC SERVICE

 
U.S. National Aeronautics and Space Administration, 1973, 1974, Symposium on signiﬁcant results and projected

Symposium on signiﬁcant results obtained from the applications obtained from the ERTS—l: Edited by O.
ERTS—l: U.S. Natl. Aeronautics and Space Admin. G. Smith and H. Granger: Houston, Tex., U.S. Natl.
Rept. SP—327, X—650—73—127. (Goddard Space Flight Aeronautics and Space Admin, Earth Resources Pro—

Center, Greenbelt, Md.) gram Ofﬁce, Johnson Space Center.

 
EARTH SCIENCE IN THE PUBLIC SERVICE

 
FEDERAL INTERAGENCY COORDINATION OF
NATURAL-RESOURCES STUDIES

By ROBERT M. WHITE
Administrator, National Oceanic and Atmospheric Administration

It is a great honor for me to be invited to par-
ticipate in this seminar on the earth sciences, com-
memorating the dedication of this magniﬁcent new
home of the United States Geological Survey. I bring
you greetings and congratulations from your sister
agency, the National Oceanic and Atmospheric Ad-
ministration. I bring these congratulations with just
a touch of envy. At long last, most of the Geological
Survey in the Washington, D.C., area will be housed
in one place, whereas we in N 0AA live and work in
some 20 different locations. How.wonderful, I some
times think it would be, if all in NOAA could get
together as you are now doing in the Geological
Survey.

I would have hoped that Vince McKelvey would
have asked me to talk about something I enjoy,
such as the weather or ﬁshing, both of which we
have something to do with in NOAA. However, it
is my lot to talk about interagency coordination in
natural-resources studies. My participation in inter-
agency coordination activities is generally something
I would like to forget rather than talk about.

Interagency coordination is about institutions and
processes and is generally regarded as something
apart from scientiﬁc and technical matters. When I
ﬁrst came to Washington a decade ago, the Assistant
Secretary for Science and Technology of the De-
partment of Commerce, Dr. Herbert Hollomon, in
discussing my new duties as Chief of the US.
Weather Bureau, told me that I would be spending
most of my time on matters that would appear at
ﬁrst as irrelevant and far removed from the direction
of the technical activities of the Weather Bureau.
He did not tell me then that it would involve coor-
dination of interagency activities. He was right. I

 
spend more time on interagency coordination than
any other single activity in which I am involved.
After a few months, it was clear that interagency
coordination may not be the stuff of scientiﬁc and
technical substance, but it might very well be real
substance in its own right.

I would like to advance that thesis. After a decade
in Washington, I have become convinced that unless
we learn how to direct and orchestrate the work of
diverse groups, solutions to our problems can 'be

seriously retarded. One of the major substantive

problems we must solve is an institutional one. Our
ability, or lack of it, to establish the necessary net-
works of specialized organizations to attack impor-
tant tasks of society may very well determine suc-
cess or failure.

I have lost count of the number of interagency
boards, committees, and panels in which my organ-
ization, the National Oceanic and Atmospheric Ad-
ministration, participates. You name it, and we have
it. Interagency bodies are ubiquitous. There are in-
teragency bodies for every level and echelon in the
Federal Government, for the big wheels and the
small wheels, for almost every subject and topic,
for satellites and weather, geodesy, oceanography,
geology. We have them in every form—bilateral
agreements, multilateral agreements, informal ar-
rangements, and formal arrangements. We have
cabinet level coordination bodies, such as the Domes-
tic Council Committee on Environmental Resources,
and the Water Resources Council, both chaired by
the Secretary of the Interior. We have the Federal
Council for Science and Technology and its sub-
committees and panels. We have Federal committees
to deal with coordination of weather services and

57

58 EARTH SCIENCE IN THE PUBLIC SERVICE

geodesy. We have bilateral arrangements with the
Geological Survey, Federal Aviation Agency, Na-
tional Aeronautics and Space Administration, the
Coast Guard, the Fish and Wildlife Service. We have
an incredible array.

“What do they all do?” This is the criticism
heard so often. Sometimes that is a hard question
to answer. Are they really as ineffective as some
people feel? Do they really solve problems, or do
they serve only to paper over unresolvable issues?
As with most things in life, the truth is in between.

Interagency bodies reﬂect the existence of trans-
organizational problems. The real world develops
in ways frustratingly different from the ones we
have organized for. We continually make new stabs
at changing organizational structures to meet new
national problems, but we never really succeed in
encompassing all aspects of a problem in a single
organization. Interagency bodies reﬂect the com-
plexity of modern problems. They reﬂect the wide
spectrum of expertise that must be brought to bear
on them. There is no way out, except to cajole, co—
erce, or direct various groups that have the exper-
tise and resources needed to get together. We cannot
reorganize for every problem, and we cannot afford
the duplication of resources that such an organiza-
tional concept implies. What we are really about
when we engage in Federal coordination, whether
it applies to the ﬁeld of natural resources or any
other ﬁeld, is establishing networks of expertise
and resources. We do not have to cast about to
understand what I mean by transorganizational
problems.

Take the problem of greatest concern to us now—
energy. Take one segment of that problem—develop-
ment of oil and gas resources of the Continental
Shelves. Literally, an army of organizations is im-
mediately involved. The Geological Survey has wide
responsibilities for the geology, geophysics, and the
safety of oil and gas drilling on the shelf; the
Bureau of Land Management has the leasing re-
sponsibility; the Environmental Protection Agency
is concerned about pollution problems; the Coast
Guard must monitor; and NOAA is concerned with
the impact of oil development on ﬁsheries. The solu-
tion requires coordination, but even more, it requires
joint participation.

Another kind of resource problem is represented
by the management of the coastal zones of the
United States. Recent legislation, the Coastal Zone
Management Act of 1972, sets up a system for State
management of our coastal zones. It would be hard
to ﬁnd a problem involving more agencies. Some-

 
times I think every single agency in the Federal
Government must have a stake.

The question is, how do you bring all Federal
agencies together so that their interests are repre-
sented. What is more important, how can their
talents be used in establishing the policies and
guidelines?

It is not just that problems are more complex;
other reasons underlie the formation of interagency
mechanisms. Take multiple-application technology——
the technology that applies to many problems. A
good example is space technology. It can be used to
study mineral resources, ﬁsheries, oceanography,
meteorology—and so on. Suddenly we are confronted
with the question of how to deploy such a technology.
We are fortunate enough to have had the wisdom
to establish a space agency to develop the technology
for all space vehicles. The more difﬁcult institutional
question is whose responsibility is it to operate the
space systems and use the data. There is no way to
deal with that problem except by bringing inter-
ested and affected groups together. Again, a need
for interagency bodies.

When you get right down to it, we might very well
ask why there are so few interagency coordinating
bodies rather than so many. I am being only slightly
facetious. Federal coordination, however, is only one
corner of a very much larger problem—one that deals
with a phenomenon that is affecting the way Gov—
ernment operates. It is not only Federal agencies
that have interests. The people “out there”—the
constituencies, interest groups, various State and
local governments, the citizen himself—all are af-
fected. They also want in. They want participation
and they should have it. Coordination needs to be
more than Federal.

I am caught up in an activity that has illustrated
to me the widening circles of who must be involved.
In NOAA we deal with resources of a different kind
from those you deal with in the Geological Survey.
Let us take the conservation of the world’s whales
as an example. I happen to be the United States
Commissioner to the International Whaling Com-
mission. We recently had our annual meeting in
London. The issue we faced was how to establish
conservation programs that would prevent endanger-
ment of whale species and restore depleted stocks
as rapidly as possible. The issue is emotional and
symbolic. It is one on which environmental and con-
servation groups have strong positions. It is also
one in which the structure of the International
Whaling Commission favors those who seek weak
conservation measures. It became absolutely Vital

 
FEDERAL INTERAGENCY COORDINATION OF NATURAL-RESOURCES STUDIES 59

to involve nongovernmental groups in every stage of
our planning in order to arrive at difﬁcult decisions
as to how to proceed. The Coastal Zone Management
Program is also a good example of the necessity of
bringing in the views of many groups at the State
and local levels.

Interagency coordination provides mechanisms for
hearing all sides of a question within the Federal
structure. These mechanisms can be good or bad.
At their best, they can attack very difﬁcult problems
and yield excellent results. At their worst, they are
bureaucratic fortresses of delay and procrastination
and deterrents to innovation. Too often, they take
the latter form. Why are they so often so frustrat-
ing? There are many reasons. Often, the agency
representatives are given no real authority; often,
they have no real standing in their own agencies
and no freedom for compromise or decisions. Often,
the budgetary discipline of the system causes a
built-in reluctance to innovate. We could go on. We
need to look at the set of causes that makes these
coordinating bodies sometimes ineffective. Unless
we can make interagency mechanisms work and un-
less we can get groups together, we are in deep
trouble.

Too frequently we think in terms of developing
new institutions because of dissatisfaction with the
old. In many cases, new institutions are needed, but
in many more cases, the problem is to use institutions
that already exist. I keep plugging away at Federal
interagency coordination because I do see instances
of magniﬁcent results through the establishment of
networks of institutions. It all makes it worthwhile.
Let me comment on a few of these, in areas with
which I am familiar.

A good example was the execution of the Bar-
bados Oceanographic and Meteorological Experiment
(BOMEX) . This was an experiment which took place

 
in 1969, off the island of Barbados. The purpose was
a ﬁeld study of the interaction between the oceans
and the atmosphere. Through the Federal Committee
for Meteorological Services, it was possible to enlist
the efforts of 10 Federal agencies along with aca-
demic and industrial institutions, working together
on a program for 3 years, requiring extensive re-
sources.

Another good example is in the ﬁeld of hydrology.
The International Field Year of the Great Lakes was
a successful ﬁeld program only because of the active
participation of many different agencies of the
Federal Government.

NOAA’s working relationship with the Geological
Survey is a model of bilateral agency cooperation.
The deputy directors of the two organizations meet
regularly to plan joint efforts and resolve issues.
The relationship works because Vince McKelvey
and I both insist that it work. We have similar ar-
rangements with NASA, the FAA, and the Coast
Guard, all of which work excellently.

I suppose we expect too much from interagency
committees. Where they have directive authority
as in many bilateral arrangements, they frequently
work. Where there is a speciﬁc task to be done, they
frequently work. Where they are of a standing
variety, they frequently fail. Where interagency
bodies do not have directive power, they can still be
useful if we do not expect them to do more than
their authority permits.

I see of no way to get our jobs done without them.
Some say they cannot get their jobs done with them.
It sounds like marriage—and maybe that is what
this is all about—the marriage of agencies. It is, in
fact, a phenomenon more enduring than a great
many marriages. It will be with us until death us
do part. There is no alternative but to make it work.

EARTH SCIENCE IN THE PUBLIC SERVICE

LAND RESOURCE—ITS USE AND ANALYSIS

By JOHN C. FRYE

Chief, Illinois State Geological Survey

Organized human society cannot exist without
the basic resources of land to sustain and support it.
Although we speak of food, shelter, and water as the
essential commodities, all of these are derived from
use of a land area. Furthermore, for several thousand
years, mineral raw materials have been an essential
item for human society, and they, also, are derived
from the Earth. Therefore, their procurement is
another form of land use. Indeed, the concept of use
of the land resource is so all encompassing that it is
difﬁcult to consider any societal problem that does
not in some way involve land use.

In spite of this universal dependence, the philo-
sophical approach‘to the use of-land has historically
differed widely among the many human cultures.
In some ancient and in some primitive societies, the
land—that is, the Earth on which we live and its
indigenous plant and animal population—was held
in great reverence. An ancient Sanskrit prayer ex-
pressed the concept in the phrase “0, Mother Earth,
ocean girded and mountain breasted, pardon me for
trampling on you.”

In America, the native Indians had a profound
reverence for the land. Chief Joseph is quoted as
saying, “. . . I never said the land was mine to do
with as I chose.” More than 100 years ago, at a
treaty parley in the Northwest, an Indian leader
said, “The Great Spirit, in placing men on the earth,
desired them to take good care of the ground, and
to do each other no harm.”

In contrast, western culture has generally viewed
the land as being for the exclusive use of man, to be
modiﬁed or exploited as the individual owner or the
local society wishes at the moment. The contrast in
attitude was eloquently stated a half century ago
by Willa Gather.

60

 
When they left the rock or tree or sand dune that had
sheltered them for the night, the Navajo was careful to
obliterate all trace of their temporary occupation. He
buried the embers of the ﬁre and the remnants of food, un-
piled any stones he had piled together, ﬁlled up the holes he
had scooped in the sand. . . . Father L‘atour judged that,
just as it was the white man’s way to assert himself on
any landscape, to change it, make it over a little (at least
leave some mark or memorial of his sojourn), it was the
Indian’s way to pass through a country without disturbing
anything; to pass and leave no trace, like ﬁsh through the
water, or birds through the air.

Against this historical contrast, we must view
present-day North America. The western practice of
unrestricted land modiﬁcation, if carried to an ex-
treme, can result in modiﬁcations of one locality that
seriously interfere with land use in an adjacent area.
Land-use practice by a local group may prevent the
larger society from making desired or necessary use
of the land, including the production of food and raw
materials. Such conﬂicts of land use have forced
upon our collective consciousness the fact that, if
our civilization is to survive, the use of land, par-
ticularly in the urbanizing areas, must be based on
sound factual data and directed in such a way that
it will not cause social deterioration. The numerical
size of our population makes it abundantly clear
that to support our citizens, even at a subsistence
level, we are far past the point of return to the
land ethic of the American Indian—even though
there are those of us who wish that we could do so.
The Honorable John D. Dingell underscored this
fact when he said, “You are not going to sell aes-
thetics to a starving Hindu.”

Because our modern society cannot return to the
ancient and primitive ethic of preservation of the
terrain in its pristine condition nor continue in the
western ethic of “do as you please to any parcel of

LAND RESOURCE—ITS USE AND ANALYSIS 61

land you hold in fee simple title,” we must move to
a position between these two, but quite different
from either. We must say in effect that the owner
of a parcel of land may use it to his own beneﬁt as
long as that use does not conﬂict with the overriding
needs of the populace and of the Nation, and that,
preferably, the use should be compatible with the
long-term needs and desires of the national culture.

Let me state clearly that I am not sufﬁciently
presumptuous to contend that I can deﬁne the long-
term needs and desires of our national culture, but
I am convinced that those groups in our society that
make such long-term decisions should base them on
adequate scientiﬁc and technical data. Here enter
geology, geochemistry, hydrology, geophysics, min-
eral-resource evaluation, and topographic mapping
—all areas of knowledge, or activities, in which
geological surveys have particular and extensive
expertise.

We are here to take part in the dedication of the
National Center of the United States Geological
Survey, and particularly of the John Wesley Powell
Building of that National Center. This is indeed an
appropriate forum for the discussion of the applica-
tion of scientiﬁc and technical data to the wise use
of our land resources. Major Powell was a giant
among pioneers, not only in scientiﬁc exploration
but also in the development of governmental agen-
cies that made possible the generation of data in a
context in which it could be useful to public decision-
makers.

Now, let us take a brief look at techniques avail-
able for attacking this broad basic problem and the
directions that may be taken in the future.

The geological sciences, in all their applied
branches, must be called upon to furnish the needed
information for evaluation of our basic land re-
source. Many of the applications are obvious and
have been described repeatedly and at length. Map-
ping of the topography and of the surﬁcial geology
clearly is part‘of the ﬁrst step, because many of the
essential features of the land are derived from these
basic elements and can be understood only in the con-
text of such background. The distribution and litho-
logic character of the earth materials at the surface,
and to depths of as much as 50 feet, have a direct
bearing on virtually any human use of the land.
However, it is not enough merely to map the distri-
bution of the formally described rock-stratigraphic
or time-stratigraphic units. The mapped units must
be characterized as to lithology, mineral compo-
sition, engineering properties, hydrologic character-
istics, and lateral and vertical variability, and indi-

 
cation must be given of the rock type immediately
underlying each unit mapped. The soils that have
developed on the described deposits should be
mapped from the standpoint of their physical prop-
erties as well as their agricultural utility. Each of
the materials units mapped should be evaluated as
to its suitability for the many specialized uses that
can be made of a particular parcel of land—be it for
residences, large buildings, highways, recreation,
waste management, mineral-resource development,
agriculture, or other use.

The type of map evaluation described is almost
universally needed to determine what use of the
land would be most beneﬁcial to society. However,
this basic evaluation is only the beginning of the
application of the geological sciences. Essential in
some areas, and for some uses, is a Wide range of
specialized data that may pertain to rocks hundreds
or thousands of feet below the surface. Examples
of these supplemental data are the presence or ab-
sence of aquifers containing ground-water supplies,
and the quality and abundance of such potential
water supplies; the presence and distribution of
former or active underground mining that might at
some time affect the use of the land surface; the
character of deep rock units that are potentially
useful for the safe disposal of liquid wastes; the
seismic characteristics of the area, which can be
used to evaluate earthquake hazard; and, of great
future importance, the location and character of mi-
eral resources that have potential for development
so that their availability can be protected until they
are needed. The last point is particularly relevant
in the vast reaches of public land in the western half
of our Nation, where we have been moving from an
early policy of “free-for-all” for mineral claims and
exploitation, toward a policy of preservation, but
without accurate and detailed knowledge of the po-
tential mineral resources that may be needed des-
perately at some future time.

The future availability of mineral resources is a
problem that illustrates the importance of the con-
cept of multiple-sequential use of land. If an area
having an important mineral resource that has the
potential to ﬁll future needs is identiﬁed, the ﬁrst
phase of land use might be for recreation, for “open
space,” or for preservation. The ﬁrst phase can then
be followed by a second phase of mineral production,
after which a possible third phase could be devoted
to waste disposal, urban development, agricultural
production, or recreation, as the needs of society at
that time might dictate. The concept of multiple-
sequential use of land is not new, and in fact it has

62 EARTH SCIENCE IN THE PUBLIC SERVICE

on occasion been practiced by accident. In the future
it should be practiced by deliberate intent, but it
must be based on sound detailed information about
the mineral resource involved and the suitability of
the subseqently disturbed area for a third phase of
use. This last phase clearly indicates the need for
continuing research on the problems of reclama-
tion or restoration of disturbed land areas.

As our social structure becomes more complex,
and as we become increasingly more dependent
upon the products of science and technology, we
require increasingly sophisticated data on which
to base decisions for the specialized uses of our land
resource. This is well illustrated by the area of waste
management. Solid waste is generally contained in
sanitary landﬁlls, which are a specialized form of
land use. Landﬁlls, which now occupy only a very
small segment of the land area, have a potential side
effect for the pollution of water resources that may
move far beyond the site. Research on the leachates
from landﬁlls and the resultant potential for pollu-
tion is only starting at a few places, but it is an area
of research that needs vigorous support in the near
future from the earth-science agencies of the Federal
Government. The efﬂuent from landﬁlls contains an
amazing mix of potentially toxic trace elements and
deleterious ions derived from the refuse in the land-
ﬁll. Basic research is required to determine which
and how many of the many potentially toxic con-
stituents will be carried outward from the ﬁll into
the regional terrain to become potential pollutants
of the regional water supply or will remain trapped
in the surrounding sediments. Such research, al-
though considered by some to be pure science, is
essential to our social existence in the near future.
The hydrologic system through the landﬁll is as
important as the geologic parameters that inﬂuence
the circulation of ﬂuids. Hydrologic data are also
essential in evaluating the potential effects of in-
jection of liquid industrial wastes into deep rock
layers.

Land use may be importantly inﬂuenced by a
group of natural phenomena that have been loosely
called “geologic hazards.” They include ground
movement associated with earthquake shocks, un-
stable ground and potential surface movement, epi-
sode ﬂooding, accelerated shore erosion, and poten—
tial volcanic activity. At least some research is
underway on all these problem phenomena. The best
available information on these potential hazards
must be part of the background data on which land—
use decisions are based.

An aspect of the land-use resource that has been

 
generally disregarded is the societal use of subsur-
face space. Although airspace above the land surface
has been generally, and legally, regarded as being
within the realm of public allocation, the use of
volumes of space below the land surface has been
considered subject to public control in only a few
special circumstances. In our metropolitan areas, the
use of subsurface space is becoming a societal prob-
blem. Subways, sewers, water mains,vand service
access for years have been normally situated under-
ground in metropolitan areas. However, use of the
subsurface for such purposes competes with ground-
water supply, waste disposal, waste-water convey-
ance and storage tunnels, mineral-resource develop-
ment, and underground storage of commodities and
presents a problem that has been given neither legal
nor public consideration. It is to be hoped that, be-
fore future decisions are made on the allocation of
subsurface space that might permanently render it
unusable for any other purpose, the earth sciences
will be asked to provide the technical facts that
should be background to any political decision on
the subject.

In an analysis of land use, we must consider such
problems as reclamation of strip-mined land; possi-
ble future subsidence of undermined land; regional
effects of canalizati‘on, artiﬁcial impoundments, and
levee construction along major rivers; and the con-
version of vast acreages of agricultural land to
urban use. The effects of such actions have long
been predicted by earth scientists, but, unfortu—
nately, the implications of future effects commonly
have not been a component of the decisionmaking
process. Furthermore, continuing research is clearly
indicated. For example, we know more about ef-
fective procedures for reclaiming shallow strip—mined
land with relatively gentle slopes and an original
cover of unconsolidated Pleistocene deposits than
we do about techniques of preventing surface sub-
sidence in undermined areas.

Having considered the areas in which earth sci-
entists should furnish needed data to guide the po-
litical decisionmakers in the use of our limited re-
source of land, we might brieﬂy consider new tech-
niques available to achieve their needed goals. Most
of the approaches used by the geologist, geochem—
ist, geophysicist, and hydrologist are well estab-
lished, but new techniques of data gathering and
predictive capability are constantly evolving. One of
the major technologic changes is in our ability to
analyze smaller and smaller quantities of potentially
toxic substances. Publicly acceptable tolerances tend
to follow our ability to detect. As the level of our

LAND RESOURCE—ITS USE AND ANALYSIS 63

chemical and mineralogical analytical capability in-
creases—particularly our ability to detect trace
quantities—we as a society tend to become conscious
of possible hazards, and we consequently tighten our
standards of acceptance until all tolerance disap—
pears. In the wise use of our land" and water re—
sources, we must be aware of the fact that if we
place our standards of acceptance beyond the level
that existed before modern human societies occupied
an area, we are being ridiculous. As a former Direc-
tor of the United States Geological Survey has
pointed out, nature’s normal functioning is the
world’s greatest polluter. Clearly, therefore, an im-
portant area of basic research is the establishment
of “background” data—that is, the determination
of the levels at which the many constituents existed
in the environment before the advent of western
culture. Furthermore, the concept of zero tolerance
—that is, zero discharge to the environment of the
products of human activity—is totally unrealistic.
We must determine instead what level we can
tolerate.

New technologies have evolved that can aid the
earth scientist in fulﬁlling his needed role of de-
lineating and analyzing the factors involved in our
land resource for the decisionmakers. Prominent

 
among these are remote sensing, including sensors
on satellites, and computer manipulation of data.
Other new and exotic techniques will evolve through
time, but it should be remembered that these are
only new “tools of the trade,” to aid in achieving
the needed results. In themselves, they do not alter
the problem or the basic data needed by the political
decisionmakers.

In conclusion, let me return to the basic problem
with which I started. The demands and needs of
today’s increasing population require that we depart
from the philosophies of earlier cultures—be they
ancient, primitive, or western—in their approach to
the use of our land resources. Social decisions for
land-use must, in the future, be based on the best
and most reliable information that our public de-
cisionmakers can obtain. We can no longer afford
whimsical or emotional decisions, or decisions based
on vicious self-interest. Earth scientists must use all
the developing and advanced technology available to
furnish our public administrators with the needed
data. In turn, governmental bodies must support the
acquisition of the needed data—at Federal, State,
and local levels—by encouragement and funding, and
they must heed the data available to them in their
formulation of public polices.

EARTH SCIENCE IN THE PUBLIC SERVICE

TECHNOLOGY INFORMATION TRANSFER

By JOSEPH S. JENCKES
Administrative Assistant to Senator Paul J. Fannin

I ﬁnd myself in a very unique and ambiguous situ-
ation, in that I don’t know a great deal about geol-
ogy. I do know a little something about politics, and
maybe I might have something to say that will re-
late to some of the talks today. I ﬁrst knew about
this symposium a couple of days ago when Mr.
Bettwy, who is the Land Commissioner of Arizona,
called and said, “Joe, why don’t you go out there;
it’s going to be very informal. Not too many people,
no television—just talk for a little While about land
use and other things in Arizona. No problem.” And
I said, “Well, what’s the topic?” He said, “A very
simple topic.” I’ll read it to you: ‘Interfaces for a
National Response to Resource Demands—A Need
for Interagency Interdisciplinary Coordination,’ sub-
ject of talk: ‘Teohnology Information Transfer.”’I
said, “What does that mean?” He said, “It’s a snap.
It means how we communicate information.” I said,
“Well that ought to be very simple, I’m an expert on
that.”

So, I got the information that he sent, including
a paper that’s so technical I don’t understand it.
That made me even more nervous. I thought, “I’m
going to be speaking to all these technical people
and experts, and I’m not going to know anything,
and I’ll make a fool of myself.” And then I thought,
“I ought to be able to just (stand up there and talk
a little bit about Arizona and tell some of the prob-
lems we have.” Then I began to think of the title of
my topic, “Technology Information Transfer.” The
title is so complicated, and it has to do with com-
municating ideas, communicating data. And I
thought, “The very thing I’m suppose to talk about
is so complicated that the man on the street doesn’t
understand it.”

Then I began to wonder if the farmer, the city

64

 
planner, and the water man in Arizona would under-
stand these data when they get them. To illustrate
that, I must tell you a little story that’s true. It did
not happen in Arizona. There’s a farmer out west
and the coyotes are eating his sheep. He says to
himself, “My gosh, I can’t control this thing. I have
to go to the Government. They’ll help me out.” So
he comes to Washington, and he meets a bureaucrat
in one of the departments. The bureaucrat says,
“There’s no problem, Mr. Farmer. We’ll handle this
just like we handled the screwworm problem. We’ll
feed the coyotes the same stuff and that will sterilize
them and you’ll have no more problems.” And the
farmer said, “Sir, you don’t seem to understand. The
coyotes aren’t making love to the sheep, they’re eat-
ing them!”

So maybe that’s part of our problem. Maybe the
politicians and the bureaucrats and the technicians
somehow are not getting the point across.

I come from Arizona. We’re very conservative in
Arizona. Let me tell you a little bit about Arizona’s
land. Arizona is a pretty big State: It covers an
area of 114,000 square miles. Public land in the
State, owned by the State, consists of about 11/2
million acres or 13 percent of the total. That’s just
State land and it is scattered all through Arizona.
The Federal land is 45 percent of the total. The
Indian land is 27 percent. Private land is 13 percent.
I don’t want to get too political here, but we had a
talk on land use, and if you go to Phoenix, Ariz.,
and you tell them there that somebody in Washing-
ton is going to tell them how to run their land,
they’re unhappy. They want to control what little
land they have. They are concerned that perhaps the
Federal Government—some of the people in the Fed-
eral Government—care more about the national in-

TECHNOLOGY INFORMATION TRANSFER 65

terest than they do about the poor guy who lives in
Arizona. Now that may be right, it may be wrong,
but that’s what they’re concerned about.

Let me tell you a little about some of the problems
that relate to this data business that we’re all sup-
posed to be talking about. How do you get the data
out? How do you communicate it? How do you trans-
fer it? I read through a technical paper about the
ERTS satellite. As I was talking about what to speak
on, I asked, “Well, is the farmer getting that infor-
mation? Does the farmer know when half his graz-
ing land is dead?” Remember it comes up white
instead of red on one kind of image, because it’s
dead and doesn’t have any heat anymore. I was told,
“Well, we’re trying to get it to them.” I said, “Is the
Geological Survey giving the Department of Agri-
culture this information?” “Well, we’re starting to.”
And I said, “How about the miners?” One percent of
the land in Arizona is used for mining, and we pro_
duce 50 percent of the Nation’s copper. So, we have
to be concerned about our things, and we’re a little
concerned about some of these data. I asked, “How
is it working?” and was told, “The satellite is work-
ing grea .”

You can get ERTS data. A satellite is great. It
doesn’t have a vested interest, and they say it’s
working ﬁne. In Arizona, they found out that they
don’t even have to make a ﬁeld inspection anymore
when they’re looking for powerlines because they
have all these photographs. There are problems, but
good things are also happening. Arizona is getting
a land-use plan that they want on a local level, and
with the help of the Geological Survey, ERTS, and
other data-gathering systems, they’re getting a plan
together.

Let me tell what else Arizona has done. They have
a system called the Arizona Trade Off Model
(ATOM). Here’s what it does. They have a big com-
puter, and they feed in a lot of demographic infor-
mation—population, transportation, how the air is
here, and how the water is there. They put it all in,
and then a corporation will say, “We may want to
move to Arizona. What can you tell us? Where should
We move?” The computer is asked a question, and
out comes the little card. It says, “Based upon your
power need, your water needs, your electric needs,
your real estate needs, the type of people, the skills
that you have, and the people that you have, you
should move to this point.”

Maybe what I would like to see is this. A build-
ing, a square building. A person walks into the build-
ing and says, “I want to know X about this piece of

 
land.” And he would get a transparency—just pick
it up and there the information is. Now they’ve got
something like that, I know. At the Land Ofﬁce you
can ﬁnd out a little bit about land management. At
the Agricultural Oﬂ‘ice you can learn a little about
that. You can go to Soil Conservation, and you can
go to AEC. You’ve got to go all over the lot. Then I
ﬁnd out that nobody speaks the same langauge any-
more! Remember this title—“Technology Informa-
tion Transfer.” I don’t know what it means! So
there’s a problem; it has a technical name—“non-
compatible data.” This agency’s got one mouthful
and this one’s got another. Example, I can only
live by examples. You know what an arroyo is? It
may be many things. It may be a dried creek. It may
be an ear muff. It may be a Mexican freeway. It may
be contraband. So we have to get our data right.
How do you do that? Scientists speak in gobbledy-
gook, farmers speak in gobbledy—gook, AEC people
speak in gobbledy-gook, and nobody understands
anybody. Maybe we have to do something about our
terminology; maybe we’ll have to go back to school
and learn to use a simple language, like how do
you communicate data or how do you communicate
information? I don’t even know what interagency—
interdisciplinary coordination means! We ought to
be simple. Hopefully, we can take politics out of
data systems. What we do with our land is a political
decision; it’s a policymaking decision. But if data
and systems get all confused and all wrapped up in
the policy matter, you don’t come out with a very
good conclusion. I don’t know what the answer is.
I don’t know whether it’s one agency or not. I don’t
know Whether we just have to call it a Government
data agency, and no connection with any depart-
ments. But you’ve got to get back to “square one,”
you have to let people know, and you have to let the
public know; we can’t make proper decisions without
proper data.

As a politician, I know we ought to make things
as simple as we can make them. We need the Geo-
logical Survey. When I saw all of this equipment out
here, I was impressed; you can do great things, and
it will help. So, keep it simple, keep the data coming,
and don’t take all of Arizona’s land away. Leave us
that 13 percent, and if we get the information, I
think the people of Arizona will work up a good
land-use plan.

To get serious for a moment here, and I will end.
The Governor of Arizona, Jack Williams, has writ-
ten a letter to Mr. McKelvey. Mr. Radlinski, I think,
is here to accept this letter and memento:

66 EARTH SCIENCE IN THE PUBLIC SERVICE

Dear Mr. McKelvey:

On this occasion of the dedication of the new John Wesley
Powell Federal Building, it is my pleasure to present this
plaque, representative of over 100 years of historical ties
between John Wesley Powell’s most signiﬁcant accom-
plishment in the State of Arizona. John Wesley Powell ex-
plored this great land for over 40‘ years before Arizona
ever became a State. He recognized the signiﬁcance not
only of the land and its resources, but he pioneered studies
of the linguistics of the inhabitants of this land—the Ameri-
can Indians—who today occupy over 14 of our State. It is
highly signiﬁcant that this new building be named after

 
this great man. Arizona is proud of our long standing re-
lationship with the U.S. Geological Survey and we are
looking forward with high expectations to future accom-
plishments which will take place in this new structure.

Sincerely,

Jack Williams
Governor, State of Arizona

It’s a tremendous structure; you’ve got tremen-
dous people there. Just keep it simple.

 
EARTH SCIENCE IN THE PUBLIC SERVICE

 
INTERDISCIPLINARY APPROACH TO
OF NATURAL-RESOURCES

THE SOLUTION
PROBLEMS

 
By NATHANIEL P. REED
Assistant Secretary of the Interior

for Fish and Wildlife and Parks

 
We must not, at the outset, consider the interdis-
ciplinary approach to problem solving as itself new
or in any way unique to this decade. Many of the
so—called great individualists of the past in truth
were great because they were adept at orchestrating
a diverse collection of talents and resources into a
focused effort to attain their objectives. Explorers
before and after John Wesley Powell have enjoyed
success substantially proportional to their ability to
meld several disciplines in the pursuit of an over-
riding objective and to pursue that objective with
determination. The same can be said of the captains
of industry and the famous generals of military
history.

More recently, we have been bemused with the
mechanisms of operations research, systems analysis,
and the like. Again, the emphasis was on the means
of getting a mission accomplished, usually within
a cost-effectiveness framework. Inputs and outputs
were generally measured in dollars, or, varying non-
dollar outputs were compared with alternative in-
puts of dollars. The variants were many and were
fully capable of earning a niche in history for their
perfector.

What We are talking about, then, is not a new
concept but rather an expansion in the use of new
planning tools, concepts, techniques, and disciplines,
many of which were not available earlier or were not
considered necessary. What we are considering, also,
is the basic decision and its alternatives as well as
the alternative means of implementing the decision
once it is made. That is a basic change.

To be speciﬁc, the construction agencies have been
making decisions for decades to build water projects
on the basis of engineering and economic analyses.

 
The time has come to add systematic environmental
analysis to the considerations that lay the basis for
a go, no—go decision—to proceed or to halt. The en-
vironmentalists must be a part of the basic decision-
making appartus.

At issue in the 1970’s is a belated recognition that
factors heretofore ignored must be brought to bear
in decisions that affect, particularly, the husbandry
of scarce resources. Some resources are renewable,
assuming that they are not irreversibly damaged by
man’s activities; others are so ﬁnite in supply as to
be exhaustible in terms of economic recovery.

In short, we must look critically not only at the
alternatives of how we do things, in the traditional
sense of maximizing revenues, but also at whether
there are more basic alternatives to the action that
would maintain a measure of resource values for
future generations; whether the decision should be
made now, or whether the options should be held
open; and whether to take no action, or whether to
pull ahead, counting on the genius of our technicians
to do something better later—buggies outclassed by
autos, whale oil replaced by petroleum.

Will petroleum be replaced by fusion, solar power,
or other sources of energy to power this great econ-
omy? Or must we settle for a more conservative
level of growth? The full range of these decisions
requires environmental knowledge and viewpoint. In
short, both the depth and breadth of our considera-
tions must be much greater. We now must consider
not only whether to take oil and gas from the Gulf
of Mexico off Louisiana but also whether energy
alternatives are available to the Nation that would
have improved prospects for sparing our national en-
vironment. This requires the advice, counsel, and, I

67

 
68 EARTH SCIENCE IN THE PUBLIC SERVICE

submit, the consent of discipline not previously
privy to decisionmaking of the more profound type.

The National Environmental Policy Act (NEPA)
mirrors the public interest and concern in looking
at national problems in a multidisciplinary context.
It requires that all agencies of the Federal Govern-
ment “utilize a systematic, interdisciplinary ap—
proach which will insure the integrated use of the
natural and social sciences and the environmental
design arts in planning and decisionmaking which
may have an impact on man’s environment.”

The courts have restated the essence of the NEPA

requirement thus:
NEPA mandates a case—by-case balancing judgment . . . in
each individual case, the particular economic and technical
beneﬁts of planned action must be assessed and then
weighed against the environmental cost; alternatives must
be considered which would affect the balance of values.
The magnitude of possible beneﬁts and possible costs may
lie anywhere on a broad spectrum . . . in some cases the
(economic and technical) beneﬁts will be great enough to
justify a certain quantum of environmental costs; in other
cases they will not be so great and the proposed action
may have to be abandoned or signiﬁcantly altered so as to
bring the beneﬁts and costs into a proper balance.

To be redundant, the full meaning is that the mod-
ern concept of multidisciplinary planning requires
that the planning team must include persons skilled
in the environmental arts and sciences, and they
must be included at the earliest stage of planning
and at the critical decision points so that the basic
decision is the right one, in terms of the long-term
well-being of man.

This well—being of man is now the critical issue.
There must be a clear recognition that, along with
the Biblical authorization for domination by man of
his environment goes a stewardship responsibility,
which, if not discharged wisely, will eventually “do
him in,” or at least Whittle down his numbers to
some level more in keeping with a natural carrying
capacity of his environment. You, as scientists,
know that, and it is not necessary to belabor the
point.

Man is in every sense a part of the Earth’s
ecoystem—a closed loop in which any disturbance
to one sector reverberates through the whole web.
The general public senses this relationship and, I
fear, is more concerned with the implications than
many scientists. Thank God for the public concern!

If the NEPA mandates the interdisciplinary ap-
proach, the principles and standards of the Water
Resources Council provide the planning framework.
They are, on ﬁrst examination, so complex that
they threaten to fall of their own weight. It is the
challenge of the planning wizards to make them

 
function. The standards do take into account mul-
tidisciplinary considerations. What they do not yet
take into consideration is the need for multiagency
interaction.

I can see little merit in adding environmental
planners to the planning staffs of the water-develop-
ment agencies, expecting thereby to have those
agencies turned around from their traditional way
of maximizing dollar beneﬁts for a select clientele
bent on a single objective—development. What is
needed is the informed input of such agencies as
the Fish and Wildlife Service, the Environmental
Protection Agency, and the Geological Survey in
the planning of Federal and federally assisted
projects. There must be a planning team represen—
tative of advocate agencies—and of the general
public—in a planning environment that invites in-
teraction, opposing viewpoints, and outright friction
at times. Alternatives representing the points of
View must be formulated and compared. Tradeoﬁ's
must be evaluated and selections made. There must
be recognition that some environments must be let
alone and that nonstructural alternatives are the
test. I believe that this interaction among agencies
must take place and that, properly directed, it will
produce enlightened results.

As an example of the institutional aspect, the
question of what agency performs the ﬁsh and wild-
life aspects of planning is covered in the Fish and
Wildlife Coordination Act. This Act requires that
the Service be consulted in such instances and that
the Secretary of the Interior provide a report based
on such ﬁndings. It also mandates certain considera-
tions of ﬁsh and wildlife.

As environmentalists we are ill prepared for this
kind of venture. The linkage between environmental
excellence and human well-being is now only ob-
«scurely traced in many facets. There is a dearth of
basic information on the exact characteristics of
ecosystems and the reactions of those ecosystems
to disturbances of various kinds. “What can we
reason but from what we know ?”, to restate
Alexander Pope’s query. We must know more, and
quickly.

Generally, Federal missions concerning the en-
vironment are pointed toward increasing our knowl—
edge of the total environment, toward protection of
the environment, and toward control and abatement
of pollution. Understanding, describing, and predict-
ing environmental phenomena require the investi-
gation or study of weather, ocean—current patterns,
earthquakes, and a host of other environmental dis-
turbances and interactions. Basic inventories, which

 
INTERDISCIPLINARY APPROACH TO THE SOLUTION OF NATURAL—RESOURCES PROBLEMS 69

describe the extent, location, and quality of natural
resources must be compiled; probably the most im-
portant are studies to understand the impact of
man upon the environment.

This is no simple task. It means that we must
learn something of the composition of the biological
community being affected, including species, num-
bers, biomass, life history, and distribution in space
of populations. It means that we must study the
quantity and distribution of the nonliving materials
such as nutrients, water, and soil types, and it means
that we must examine the range or gradient of con-
ditions in the community such as temperature, light,
and other factors.

After learning these basics, we must ultimately
relate them to man and to man’s impact on those
systems. Our environmental protection and enhance-
ment activities must include preservation of unique
natural areas and endangered species. These activi-
ties must include conservation and management of
our ﬁsh and wildlife resources; recreation and his-
toric preservation and conservation must also be
included.

The greatest effort is in the area of pollution-
control and abatement activities, including ﬁnancial
assistance to State and local governments for p01-
lution-control programs, regulation of pollution and
enforcement standards, research involving control
and abatement of pollution, and the control of pol-
lution from Federal installations.

Superimposed upon individual agency programs
are national commitments that cross agency bound-
aries and shape the future of our natural resources.
One program, as discussed in the President’s Bud-
get Message for ﬁscal year 1975. is a comprehensive
energy program to deal with current shortages and
to reestablish our ability to be self-sufficient. This
national energy program includes

. reorganization of Federal administrative machinery to
deal more effectively with short— and long-term energy
needs; stringent energy conservation measures . . . and
allocation of petroleum products . . . reporting of oil pro:
duction, inventories, reserves and costs; modernization of
regulations for railroads in order to permit energy sav-
ings; policies to accelerate development of domestic oil and
gas reserves . . . and development by private industry of
western oil shale and offshore oil and gas deposits; meas—
ures to permit increased use of our vast coal reserves, in-
cluding environmental safeguards for surface mining, con-
version of oil-ﬁred electric power plants to coal, improve
ment of mining techniques and accelerated efforts to de-
velop technology for coal gasiﬁcation, coal liquefaction, ad-
vanced combustion systems, and pollution control; develop—
ment of fast breeder nuclear reactors which it is hoped
will greatly increase the amount of energy recoverable from
our nuclear fuel resources; more timely approval of sites

 
for energy facilities and accelerated construction of nuclear
power plants; and increaSed research on advanced energy
sources including fusion power, and geothermal and solar
energy.

I believe that several environmental problems re-
lated to this energy program need special attention
because of their massive size and the industrial
and urban changes associated with them. I would
like to mention one or two of these which I con-
sider particularly important, but this list is not all
inclusive by any means.

Western coal and oil-shale resources—The pro-
posed development of the largest coal deposit in
the world in Colorado, Wyoming, and the Dakotas,
as well as increased production in other sections of
the Nation, and the development of extensive oil-
shale deposits have the potential for enormous
damage to ﬁsh and wildlife resources. Proper at-
tention must be applied to these resources and to
their associated values during development of both
coal and oil-shale resources to prevent destruction
and degradation of land and water resources. The
Appalachian syndrome—the wrecking of land and
man—must not be transmitted to the American
West.

Power plants.-—Power—plant development is ac-
celerating at a rapid pace. By December 1972, the
Atomic Energy Commission had issued operating
licenses for 29 nuclear power plants. Another 84
nuclear power plants are either-under construction
or under operating permit review. Nuclear and
other forms of power development have the poten-
tial for effecting irretrievable and irreversible en-
vironmental losses. The impact of nuclear power
plants on our national ﬁsheries must be evaluated.
Impingement, entrainment, loss of juvenile ﬁsh,
and improperly designed screens must be mini-
mized.

Coastal ecosystems—The Nation’s coastal areas,
including tidal wetlands, estuaries, contiguous
oceans, and the Great Lakes, are being altered by
man through dredging, ﬁlling, channelization, pol-
lution, and related actions. These fragile environ-
ments provide basic habitat requirements and food
sources for more than 60 percent of the Nation’s
ﬁshery resources. Coastal areas further serve as an
important nesting, resting, and/or feeding habitat
for a variety of animal life forms, including migra-
tory birds, fur animals, and sea mammals, as well
as endangered wildlife. Without proper planning and
remedial management efforts, renewable natural re-
sources and their environments will continue to be
degraded signiﬁcantly or may be virtually lost in

70 EARTH SCIENCE IN THE PUBLIC SERVICE

the near future. We may not need the protein base
of our coastal ﬁsheries now, but our grandchildren
may. We would be a foolish people if we continue
to allow the desecration of our estuarine system.

Stream alteration—This problem, I believe, is
particularly appropriate for discussion, because the
Geological Survey has a long history of involvement
in water-resource problems through its collection of
basic information and its basic and applied research
programs. Stream alterations, including channeliza-
tion, clearing, snagging, dams, and diversions, are
common water—control and storage methods. The
long-term ecological signiﬁcance of such alterations
has been largely ignored. These alterations affect the
total ecosystem, which includes the channel proper
and the ﬂood plain. Flood-plain ecosystems general-
ly are recognized as the most productive inland habi-
tat in North America.

As Federal, State, and local construction agen-
cies have broadened their environmental perspec—
tives in water use, demands for answers to ﬁsh,
wildlife, recreation, and ecological questions have
increased. Our capacity to respond has not kept
pace with the need. Our ability to evaluate biologi-
cal and socio-economic aspects of water-project de—
velopment accurately is inadequate. It is necessary
for various local, State, and Federal agencies to
work together to prevent further degradation of our
streams and rivers.

This country is currently in a position where
massive programs are going forward with inade-
quate knowledge or consideration of environmental
consequences. We can no longer afford the luxury
of compartmentalizing each segment of a resource
problem so that it may fall neatly into the techni-
cal, scientiﬁc, or legal jurisdiction by law or ex-
pertise of a speciﬁc agency. It is time to look at
the entire system, the interactions of that system’s
parts, and the required basic information for effec-
tive and efﬁcient management of these systems.

We are living in an age of real or supposed crises.

 
The real crises of overpopulation and overconsump—
tion of ﬁnite materials, of food, and of declining
energy reserves will be with us from now on. If
light is to penetrate the darkness, if change is
going to occur speedily to keep us on an even keel,
then some old dogs must learn new tricks.

Paul Ehrlich brilliantly pointed out that it is

not the starving have-not nations that are creat—
ing such a terrible strain on the world’s ecosystems.
It is we—the inhabitants of the highly industrialized
nations—who generate the spiraling never-ceasing
demands that overload our systems and resources.
He stated in a recent speech:
We have got to end the insane growth of consumption in
the overdeveloped countries, and this can be done with a
great increase in the quality of life. We can reduce our
energy consumption and live better.

We have got to stop population growth in the over-de-
veloped countries because it is the most serious population
growth in the world, and it is starting to climb. We have
got to convince under-developed countries that imitating the
kind of development that we have done, say in the United
States, would be a lethal mistake, and hope that they will
choose diﬂerent development goals, and that in particular
as they choose their options, they will try and take ones
which will lead among other things to lower birth rates as
rapidly as possible. We will never convince them to do that
unless we change our own ways . . . and if people cannot
change their behavior rapidly enough, then we just will
not get the job done, and like many other species that have
overshot the carrying capacity of their environment, we will
pay the price.”

The American people cannot continue their ac-
celerating growth binge. Sooner or later, even with-
out our intervention, limiting factors Will halt the
growth. The major question is whether or not con—
trol of the growth syndrome will be the result of
rational carefully planned human action or of chaos.

The scientists of the Geological Survey will be
part of the great decisions which we as the world
leader must make. The verdict on our success in
this mission has not yet been rendered. The de—
cision is in the hands of you, the educated. You
must prepare a constituency to face up to the
realities of the hard choices we collectively face.

EARTH SCIENCE IN THE PUBLIC SERVICE

NATURAL-HAZARDS REDUCTION

By FRANK PRESS
Chairman, Department of Earth and Planetary Sciences,
Massachusetts Institute of Technology

Up to this point in the symposium we have heard
about energy and mineral resources and their de-
velopment in the context of the need to conserve the
environment. The same forces that created the hos-
pitable and rich environment that enabled life to
develop and civilization to progress beyond the Stone
Age also trigger earthquakes, volcanic eruptions,
tsunamis, and landslides and contribute to climatic
change and destructive weather.

The human need to understand nature in order to
discover her material wealth and to gain protection
from her vagaries survives to this day as the major
motivation of earth scientists. It is ﬁtting therefore
to take up the question of the Nation’s response to
natural hazards at the dedication of the new capital
of earth sciences here in Reston, Va.

I should like to review for you some of the scien-
tiﬁc progress of recent years and to say something of
the response required by our public agencies to
match the technical advances.

To begin with, let me ﬁrst document the need for
a national program dealing with natural-hazards re—
duction. Some years ago, when I presented a pro-
posal for research in earthquake prediction and
earthquake engineering to the President’s Science
Advisory Committee, one member questioned the
need for a major investment in research, pointing
out that in the history of our country only a few
hundred lives were ever lost to earthquakes and that
the apparent loss from earthquakes in this century
could not have averaged more than about $20 million
per year. What was overlooked in this critique was
the future loss potential from a reoccurrence of a
great earthquake such as those in San Francisco in
1906, Los Angeles in 1857, and New Madrid, Mo., in
1811. Tens of billions of dollars and tens of thou-

 
ands of casualties are the kinds of numbers that have
been appearing in sudden-loss estimates. Catas-
trophic earthquakes have occurred in the past and
will occur in the future, as any geologist would
vouch. The new ingredient is the astronomic growth
in population and investment in the earthquake-
prone regions of our country. Some 30 million people
now live in the 20 States that are in seismic-risk zone
3—the most dangerous category in the seismic—risk
map of the United States. An additional 40 million
live in seismic-risk zone 2. The San Fernando earth-
quake of 1971 was a sobering experience to geolo—
gists and engineers. This relatively small tremor
(much less than 1 percent of the energy released in
the San Francisco quake) occurred in a densely
populated region. The damage bill came to $500 mil-
lion. Too few people know that one dam was stressed
to near the failure point and that a slightly larger
shock on another day would have resulted in casualty
ﬁgures in the tens of thousands.

When one considers tsunamis, volcanism, hurri-
canes, storm surges, tornadoes, and landslides, no
communities in our country are immune to loss from
natural hazards.

On the bright side is the remarkable progress that
man has made in understanding the natural systems
that constitute his environment. In the limited time
available to me I will highlight our new insights con-
cerning the Earth’s internal forces, although an
equally impressive report could be made about our
new understanding of the atmosphere and oceans.

The past decade has been a period of great dis—
covery and excitement in geology. For the ﬁrst time
an all-encompassing theory—that of plate tectonics
—ties together the large-scale geological phenomena
of our planet. Most earthquakes and volcanoes, for

71

72 EARTH SCIENCE IN THE PUBLIC SERVICE

example—their location and the forces that cause
them—can be explained in terms of the relative mo-
tions of about a dozen plates that make up the outer
shell of the Earth. In the laboratory, rocks have been
stressed under the conditions of high pressure and
temperature that exist in the Earth’s interior, and
physical changes that precede rupture have been
found and explained. In research pioneered in the
U.S.S.R. and extended here, these same changes have
been shown to exist in the Earth’s crust prior to an
earthquake. Volcanoes have been instrumented, and
the progress of magma from the deep interior to the
place of eruption has been charted. To draw an
analogy with medical research, it is as if the etiology
of 90 percent of cancers was understood for the ﬁrst
time. We have reached a point where prediction of
earthquakes and volcanic eruptions and accurate
forecasting of tsunamis and landslides are achievable
goals.

Rapid progress has been made in another aspect
of hazard mitigation—the physical description of
the hazard, mapping its geographic extent, and al-
lowing for the response of structures to the forces
involved. For example, more data have been accumu-
lated on ground motion and soil response due to
earthquakes in the past few years than in all preced-
ing time. A whole new approach to risk analysis is
being developed involving a physical description of
the hazard, its probability of occurrence, and hazard-
resistant design alternatives, all of which raise de-
cisionmaking from the level of guesswork to a highly
professional act. In citing these few examples, I
want to make the point that science and technology
are opening the possibility of signiﬁcantly reducing
man’s vulnerability to natural hazards. As exciting
as this progress has been, the effort has been sup-
ported at below the critical level needed to achieve
these goals, in an operational sense, in this century.

Regardless of progress on the technical front, sig-
niﬁcant hazard mitigation cannot be achieved with—
out a Federal policy and an organized program. For
example, a policy decision to augment support in
earthquake-prediction research can bring this goal to
fruition in years rather than decades. The Govern-
ment, through the many ways it inﬂuences construc-
tion—disaster insurance, impact statements, US.
Army Corps of Engineers approvals, Government
construction, subsidies, disaster relief—can mandate
land-use and construction-engineering practice on
the basis of the new technology. Information trans-
fer from the research centers to the communities can
be expedited in this way. It is an interesting yet sad
commentary that in hazard—risk analysis both in this

 
country and in the U.S.S.R., specialists have de—
veloped powerful techniques to rationalize decision-
making in land use and construction, yet these spe-
cialists have difﬁculty is ﬁnding customers for their
new technology.

Just as natural hazards know no geographic boun-
daries and affect man and his culture in many ways,
so does the Government responsibility cut across de—
partmental lines. The Departments of Housing and
Urban Development, Health, Education, and Wel-
fare, Defense, Interior, and Transportation and the
Atomic Energy Commission, Veterans Administra-
tion, and the Food and Drug Administration have
legitimate roles to play, as do State and county gov—
ernmental units. There are not many precedents for
pol‘icymaking involving so many agencies, some of
which are potential users of new technology, some
developers of new technology, and some serving in
both capacities. Then there is the matter of relative
urgency. If a major catastrophe were to strike to-
morrow, the following day would almost certainly
see a government-Wide policy in natural—hazards
mitigation. How does one sell preventive medicine
for a future aﬂiiction to agencies beleaguered with
current illnesses?

I believe that scientists and engineers must as-
sume a role of advocate and even special pleader
When they perceive a sluggishness in the Govern-
ment’s response to some new opportunity or to
some future danger. It is not outside of the scien-
tiﬁc tradition for scientists to make a case before
the Executive Ofﬁce or to brief Congress on an im-
portant issue. Einstein did it in his famous letter
to President Roosevelt on the possibility of an atom
bomb. The possible stress to the environment from
a ﬂeet of SST’s, the nongovernmental expert testi-
mony on ABM’s, the design of a national cancer-
research program, the campaign against cigarette
smoking—these are famous examples where experts
have reached and inﬂuenced branches of govern-
ment.

Earth scientists anticipated the energy and min-
eral—resource crises. They knew years ago that these
critical shortages would trouble us, beginning with
the last decades of the 20th century, yet they are
liable to the criticism that they did not speak out
loudly enough or did not reach the right pressure
points to inﬂuence Government policy.

Earth scientists have a case to make. They can
point to housing tracts placed in fault zones or on
unstable hillside slopes. They can cite newly built
hospitals that collapsed when shaken by a moderate
earthquake. They can question the policy of a de-

NATURAL-HAZARDS REDUCTION 73

partment of the Government that spends billions in
construction yet is unable to support research that
would safeguard its investment. They can question
the wisdom of budgeting less than 0.1 percent of
the total construction investment for hazard-miti-
gation research. They can show how a research
dollar invested today can yield an enormous return
in lives saved and property preserved tomorrow. At
a time when basic research budgets have not kept
pace with the growth in the GNP, earth scientists
can point up the practical value to society of their
new comprehension of the forces that have shaped
our planet.
What kind of Government policy is needed to
encourage and then to exploit progress in the tech-
nology of hazard mitigation? After we list the in-
gredients of such a policy, it will become clear
where in government the responsibility should lie
for organizing and implementing a program.
I list some of the ingredients of a national policy:
1. Goals for hazard prediction, with adequate re-
search support to implement these goals; for
example, earthquake prediction in California
in 10 years.

2. Goals for hazard control; for example, hurri-
cane modiﬁcation in 20 years.

3. Regi‘onalization of the country according to
disaster potential.

4. Land-use policy according to disaster potential,
including regulations and incentives.

5. Research and development in antihazard engi-
neering and risk analysis.

6. Development of construction codes in accord-
ance with latest research and development re-

 
sults.

7. Use of new approaches to risk analysis in siting,
selection of alternatives, and investment de-
cisions.

8. Insurance, disaster relief, and reconstruction
policies consistent with the preceding.

9. Information-transfer and public education pro-
gram.

This list covers several disciplines and cuts across
the responsibilities of various departments of the
Government. Indeed, the budget for such a program
would appear as a crosswalk table involving many
agencies and many technologies.

It seems clear that a disaster-mitigation program
must receive a charter and guidelines from the
highest levels of the Government. Management, co-
ordination, and interdepartmental budgeting are
essential elements, as are the involvements of state—
of-the-art science and technology. I believe that a
task force, chaired by the President’s science ad-
Visor, which should include senior representatives
of the Ofﬁce of Management and Budget (OMB) and
the cognizant government departments, is called for.
The coordinator must have authority, and he must
enjoy the conﬁdence of OMB, both of which go with
proximity to the Executive Ofﬁce. I believe a strong
Government-wide program would receive the support
of Congress. Does any one doubt that we would
have a program similar to the one that I have de-
scribed after the next magnitude 8 earthquake in
a western State? Why not reduce the severity of
future catastrophe by organizing a national program
now. Earth scientists should take the lead in selling
this concept and then getting on with this challenge.

‘1' U.S- GOVERNMENT PRINTING OFFICE: 1974 0‘585—470 /49

 
V 7 DAY.

;., Oligocene Marine Mollusks from the
3%: Pittsburg Bluff Formation in Oregon
, 9.

/

 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 922

 
UUCUMENTS DEPARWENT
MAY 4 7975 USS-9”“
L
UNIVERSln'HiJRI-ﬁlgauronm
,‘
APR 5 1976

ESSDO

 
Oligocene Marine Mollusks from the "
Pittsburg Bluff Formation in Oregon

By ELLEN JAMES MOORE

 
GEOLOGICAL SURVEY PROFESSIONAL PAPER 922

Systematic paleontology and stratigraphic
relations of the mollusks—48 species
representing 31 families are described;

6 taxa are new

 
UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1976

UNITED STATES DEPARTMENT OF THE INTERIOR

THOMAS S. KLEPPE, Secretary

GEOLOGICAL SURVEY

V. E. McKelvey, Director

Library of Congress Cataloging in Publication Data

Moore, Ellen James
Oligocene marine mollusks from the Pittsburg Bluff Formation in Oregon.

(Geological Survey Professional Paper 922)

Bibliography: p. 56—60.

Includes index.

Supt. of Docs. no.: I 19.16z922

l. Mollusks, Fossil. 2. Paleontologyioligocene. 3. Paleontology#0regon. I. Title. II. Series. United States. Geological
Survey Professional Paper 922.

QE801.M774 564'.09795 76—608010

 
For sale by the Superintendent of Documents, U.S. Government Printing Ofﬁce
Washington, DC. 20402
Stock Number 024—001—02775—5

CONTENTS

 
Page Page
Abstract __________________________________________________ 1 Systematic descriptions—Continued
Introduction ______________________________________________ 1 Class Gastropoda—Continued
History of investigation ________________________________ 1 Family Fusinidae __________________________________ 36
Purpose and scope ______________________________________ 2 Family Fasciolariidae ______________________________ 36
Preparation of collections ______________________________ 2 Family Turridae __________________________________ 37
Abbreviations __________________________________________ 3 Family Pyramidellidae ____________________________ 40
Annotated chronology of reports dealing with Oligocene Family Acteonidae ________________________________ 40
formations and fossils, with primary emphasis on Oregon Family Scaphandridae ______________________________ 41
and Washington, 1892—1975 __________________________ 3 Class Scaphopoda ______________________________________ 41
Acknowledgments ______________________________________ 10 Family Dentaliidae ________________________________ 41
Pittsburg Bluff Formation __________________________________ 10 Class Pelecypoda ______________________________________ 42
Stratigraphy __________________________________________ 10 Family Nuculidae __________________________________ 42
General features and geographic distribution ________ 10 Family Nuculanidae ______________________________ 43
Type locality ______________________________________ 11 Family Mytilidae __________________________________ 44
Type area ________________________________________ 11 Family Carditidae ________________________________ 45
Check list of Pittsburg Bluff species ____________________ 14 Family Lucinidae __________________________________ 45
Ecology ______________________________________________ 16 Family Ungulinidae ________________________________ 46
Relation to other Oligocene faunas in Oregon ____________ 19 Family Cardiidae __________________________________ 47
Summary __________________________________________ 23 Family Veneridae __________________________________ 47
Age __________________________________________________ 23 Family Mactridae __________________________________ 49
Correlation ____________________________________________ 25 Family Mesodesmatidae ____________________________ 50
Systematic descriptions ____________________________________ 29 Family Tellinidae __________________________________ 50
Class Gastropoda ______________________________________ 29 Family Solenidae __________________________________ 51
Family Trochidae __________________________________ 29 Family Hiatellidae ________________________________ 52
Family Architectonicidae __________________________ 29 Family Periplomatidae ____________________________ 53
Family Turritellidae ______________________________ 29 Family Thraciidae ________________________________ 54
Family Epitoniidae ________________________________ 30 Class Cephalopoda ____________________________________ 54
Family Calyptraeidae ______________________________ 31 Family Nautilidae ________________________________ 54
Family Naticidae __________________________________ 31 US. Geological Survey fossil localities in the Pittsburg Bluff
Family Neptuneidae ______________________________ 33 Formation, middle Oligocene, northwestern Oregon ________ 55
Family Buccinidae? ________________________________ 35 References cited ____________________________________________ 56
Index ____________________________________________________ 61

ILLUSTRATIONS

[Plates follow index]

PLATE 1. Architectonica, Crepidula, unidentiﬁed trochid?, Cryptonatica, Sinum, and Polinices.
2. Neverita.
3. Bruclarkia, Opalia, Odostomia, Turritella, and Priscofusus.
4. Eosiphonalia.
5. Molopophorus.
6. Perse.
'7. Spirotropis, Taranis, S uavodrillia, Dentalium, Scaphander, Acteon?, Acteon, and Aforia.
8. Acila and Nucula.
9. Litorhadia, Cyclocardia, and Yoldia.

10. Lucinoma, Felaniella, and Nemocardium.

‘ 11. Tellina? and Tellina.

, 12. Pitar, Callista, and Crenella.
13. Selena and Solen.
14. Spisula.

15. Panopea and Aturia.
16. Thracia, ?Ervilia, and Cochlodesma.
17. N aticids, Molopophorus, Perse, Acila, and Macrocallista.

III

IV

FIGURE

TABLE

005103014;me

1.

CONTENTS
Page
. Map showing location of area of study at Vernonia, Oreg ___________________________________________________________ 10
. Photograph showing type locality of Pittsburg Bluff Formation _____________________________________________________ 11
. Geologic sketch map of the Vernonia area showing fossil localities and location of measured sections _________________ 12
. Measured sections of the Pittsburg Bluff and adjacent formations, Vernonia area _____________________________________ 13
. Photograph showing contact between siltstone of the Keasey Formation and sandstone of the Pittsburg Bluff Formation ,,,,, 13
, Photograph showing siltstone rip-up clasts in Pittsburg Bluff Formation _____________________________________________ 13
Correlation chart of selected middle Tertiary stratigraphic units in Alaska, Washington, and Oregon _________________ 27
. Sketch of growth-line sinus on Turritella pittsburgensis, n. sp _______________________________________________________ 30
TABLES
Page

Checklist of species at US. Geological Survey localities in the Pittsburg Bluff Formation arranged in approximate strati-

graphic order ________________________________________________________________________________________________ 15
Holocene genera in the Pittsburg Bluff Formation and their preferred bottom sediment and water depth _______________ 17
Distribution of molluscan genera in the lower, middle, and upper parts of the Keasey Formation and their occurrence in

the Pittsburg Bluff and Eugene Formations ____________________________________________________________________ 22

. Distribution of Pittsburg Bluff species in some other formations of late Eocene, Oligocene, and early Miocene age - _____ 26

. Checklist of Oligocene mollusks in the upper part of the Eugene Formation in Oregon _______________________________ 28

OLIGOCENE MARINE MOLLUSKS FROM THE
PITTSBURG BLUFF FORMATION IN OREGON

By ELLEN JAMES MOORE

ABSTRACT

The ﬁrst recorded collection of fossils from the Pittsburg Bluff
Formation was identiﬁed by W. H. Dall in 1896 and was assigned to
the Oligocene. This was the ﬁrst marine fauna on the Paciﬁc coast to
be assigned to the Oligocene. Although the fauna was brieﬂy regarded
as Eocene in the early 1900’s, it has since been referred to the
Oligocene, then more precisely to the middle Oligocene, an assign—
ment that still stands.

The Pittsburg Bluff Formation occurs in northwestern Oregon,
where fossiliferous exposures are found in streambanks and in cuts on
highways, logging roads, and railways. The type area of the formation
is along the Nehalem River near Pittsburg, Oreg., where a highway
cut affords a good exposure of its lower part. Exposures of the
Pittsburg Bluff Formation are relatively scarce; they are interrupted
by broad areas of thick soil cover and dense vegetation. The formation
is cut by minor Visible faults, and there may be others that are not
visible, so the mapping is uncertain in some places.

The Pittsburg Bluff Formation conformably overlies the Keasey
Formation (late Eocene and early Oligocene) and is conformably
overlain by the Scappoose Formation (late Oligocene and early
Miocene). Because parts of all these formations are lithologically
similar, the stratigraphic position of a nonfossiliferous exposure is
sometimes uncertain. New stratigraphic studies indicate, however,
that contrary to the opinion of some previous investigators, the
Pittsburg Bluff Formation is conformable with the underlying Keasey
Formation.

The estimated maximum thickness for the entire formation is 200

m; the thickest continuous measured section of the Pittsburg Bluff

Formation is 100 In thick.

In the present investigation, fossils were collected from newly
measured sections. In addition, all the collections from the Pittsburg
Bluff Formation on deposit in the US. National Museum have been
studied, as well as those at the California Academy of Sciences,
Stanford University, and the University of California at Berkeley.

A total of 48 species of Oligocene mollusks representing 43 genera
and 31 families are described; of these, 5 species and 1 subspecies are
new, representing the genera Turritella, Opalia, Cryptonatica, Perse,
N ucula, and Felaniella. The biologic afﬁnities of all the species in the
formation are reconsidered, and the fauna is correlated with other
Oligocene faunas.

The fossil mollusks represent a death assemblage; it seems likely
that three habitats may be represented, one of deep water (about
100 In), one of moderately shallow water (about 20 m), and one of
shallow nearshore water, partly intertidal. The remains of mollusks
living in these dissimilar habitats were brought together by sub-
marine grain ﬂowage before being fossilized. The bottom sediment

was sandy mud. Comparison with ranges of related living genera'

indicates that the ocean temperature off the northern coast of Oregon,
though cooler than it was in the Eocene and Miocene, was perhaps
warmer than it is today.

 
INTRODUCTION
HISTORY OF INVESTIGATION

The ﬁrst description of the rocks in the bluff near
Pittsburg was written by J. S. Diller (1896). In his re-
port, Diller assigned the fossil mollusks collected from
these rocks to the Oligocene on the basis of iden-
tiﬁcations made by W. H. Dall. This was the ﬁrst marine
fauna on the Paciﬁc coast to be regarded as Oligocene. In
1903, however, Dall described Callista pittsburgensis
from Pittsburg and assigned it to the Eocene. But Clark
(1915), after comparing the fossils from this section with
other mid-Tertiary taxa of the Paciﬁc coast, some of
which had been dated by comparison at the generic level
with mollusks in the type sections in Europe and by
Lyell’s method of percentage of living taxa, reassigned
the molluscan fauna from the bluff near Pittsburg to the
Oligocene, stating that it was distinct from those of both
the Eocene and the Miocene.

The term “Pittsburg Bluffs” was ﬁrst used for early
Oligocene strata of Oregon in a correlation diagram by
Hertlein and Crickmay (1925, p. 254), but these men did
not formally describe the formation. In 1927 Schenck
described what he called the “Pittsburg Bluff
sandstone,” which he said overlaid the Keasey Shale,
was of middle Oligocene age, and could be correlated
with the Eugene Formation (early and middle
Oligocene), the Tunnel Point Sandstone (middle
Oligocene), and the Yaquina Formation (late Oligocene
and early Miocene).

In 1936 Schenck (1936, p. 44) deﬁned the Acila
shumardi Zone as delimited by the range of Acila
shumardi and as being further identiﬁed by such forms
as Bruclarkia columbiana (Anderson and Martin),
Callista pittsburgensis Dall, and Molopophorus gabbi
Dall. All are common in the Pittsburg Bluff Formation.

Schenck and Kleinpell (1936) proposed the west coast
term “Refugian Stage” for rocks laid down after the
Tejon and before the Zemorrian. The Refugian Stage
included the Acila shumardi Zone, and its upper part
marked the last appearance of Acila shumardi, Callista
pittsburgensis, Molopophorus gabbi, and Bruclarkia
columbiana.

2 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Weaver (1937) suggested that the term “Pittsburg
Bluff Formation” be applied to the entire middle
Oligocene sequence of sedimentary rocks in Columbia
County, Oreg., and that the type area of the formation
be considered the exposures between Pittsburg and Mist
on the Nehalem River in Oregon. In 1942, in a publi-
cation on the paleontology of the marine formations of
Washington and Oregon, he described and illustrated
all of the then known species of mollusks from the
Pittsburg Bluff Formation.

Durham (1944) restricted the Pittsburg Bluff fauna to
his Molopophorus gabbi Zone. Acila shumardi occurs in
both his early and middle Oligocene faunas.

Warren, Grivetti, and Norbisrath (1945) mapped the
areal extent of the Pittsburg Bluff Formation in
northwestern Oregon and divided the formation into
two members. On the basis of the molluscan faunas,
they believed the lower member and the lower part of
the upper member to belong to the middle Oligocene
Molopophorus gabbi zone (as used by Weaver and
others, 1944).

In 1946, Warren and Norbisrath described the
Pittsburg Bluff Formation as follows:

In the lower part of the Pittsburg Bluff Formation are ﬁne-grained
marine sandstones containing numerous fossils in layers along the
bedding and in calcareous concretions. These richly fossiliferous
sandstones seem to pass upward into coarser massive sandstone which
interﬁngers with cross-bedded, nearshore, marine and brackish-
water sandstone. Upward in the formation fossiliferous bands are less
common. Toward the top of the formation fossils are few and thick beds
of tuffaceous material are prominent.

No subsequent reports dealing primarily with the
Pittsburg Bluff Formation have been published; its age,
however, has been regarded as provincial middle
Oligocene in references to and correlations with the
formation since 1946.

PURPOSE AND SCOPE

The original descriptions of mollusks found in the
Pittsburg Bluff Formation are in many papers, none of
which deal primarily with the fauna. Many of the
original photographs, moreover, are inadequate, and
much of the taxonomy is out of date. In this paper all the
described mollusks are reillustrated and redescribed,
and some needed corrections have been made in their
taxonomy. Five new species and a new subspecies,
representing six genera, are described and illustrated.
Also included are new stratigraphic sections of the
Pittsburg Bluff Formation measured in Columbia and
Washington Counties, Oreg., near the type area; these
are presented together with a geologic sketch map.

The middle Oligocene mollusks found in the
Pittsburg Bluff Formation are compared with other
known Oligocene faunas of the Paciﬁc coast of North
America, and the geologic and geographic ranges of

 
each species are given. Information on the ecology of
related modern genera is tabulated, and this data,
together with lithologic data, have been used to infer
generalities concerning the Oligocene paleoenvi-
ronment.

The type locality of Acila (Truncacila) shumardi
(Dall) (sec. 23, T. 5 N., R. 4 W., Vernonia quadrangle) is
in the type locality of the Pittsburg Bluff Formation.
This mollusk lived throughout the Acila shumardi
Zone, which has been recognized by various authors at
localities ranging from Alaska to California. Schenck
(1936, p. 42) proposed the “Acila shumardi biozone” and
accepted the deﬁnition of a biozone as “a deposit formed
during the total existence of a species.” He goes on to
deﬁne the Acila shumardi Zone (1936, p. 44) as being
“that group of beds *** identiﬁed by an assemblage of
fossils including Acila (Truncacila) shumardi (Dall),
Bruclarkia columbiana (Anderson and Martin),
Macrocallista pittsburgensis Dall, and Molopophorus
gabbi Dall, and limited by the upper and lower range of
Acila shumardi.” It would seem that he may have had
an assemblage zone in mind when he proposed the Acila
shumardi biozone. Although A. shumardi is especially
useful in stratigraphic correlation, its usefulness is
enhanced if the entire molluscan assemblage living
with it is recognized and understood. This paper seeks to
fulﬁll that purpose.

PREPARATION OF COLLECTIONS

Each collection of fossils taken from the Pittsburg
Bluff area in the 1890’s and early 1900’s was given a
U.S. Geological Survey locality number that designated
a geographic position without regard to its stratigraphic
interval. This was, of course, the usual practice at the
time, but it gave a false impression regarding the taxa
that were actually found together in a given lens or
layer of rock.

During ﬁeld investigations conducted in the 1940’s
for the U.S. Geological Survey, H. E. Vokes collected
many fossiliferous slabs from the Pittsburg Bluff
Formation to aid in paleoecologic studies. The slabs
average perhaps 8 X 15 X 20 cm in overall size; two of
them are shown on plate 17. These slabs, most of them
from USGS localities 15264 and 15310, have been in—
dividually prepared as part of the present study, and on
each specimen taken from a single slab the same letter
has been put after the U.S. Geological Survey Cenozoic
locality number, for example 15264a, to indicate what
fossils were found together in the same slab. In other
words, 15264 covers the general locality and 15264a,
15264b, and so forth, refer to specimens from different
slabs from that locality.

Some pieces of rock that could not be prepared by
ordinary mechanical means without loss of specimens

INTRODUCTION 3

were disintegrated by being soaked in kerosene and
then heated in an oven at a temperature of 120°C. The
samples were then washed through a 0.177-mm screen,
which retained mollusks of larger diameter and ﬁsh
remains. Part of the ﬁnes from each sample was then
washed through a 0.125-mm screen, but the only ad-
ditional complete organic remains thus recovered were
two globigerinid foraminifers.

ABBREVIATIONS

The following abbreviations are used in this report:

USGS: US. Geological Survey, Washington,
D. C., Cenozoic locality register.

USGS M: US. Geological Survey, Menlo Park,
Calif, Cenozoic locality register.

UCMP: California University, Museum of
Paleontology, Berkeley, Calif.

CAS: California Academy of Sciences, San
Francisco, Calif.

SU: Stanford University, Stanford, Calif.

UW: University of Washington, Seattle,
Wash.

UO: University of Oregon, Eugene, Oreg.

ANSP: The Academy of Natural Sciences of

Philadelphia, Philadelphia, Pa.

ANNOTATED CHRONOLOGY OF REPORTS DEALING
WITH OLIGOCENE FORMATIONS AND FOSSILS, WITH
PRIMARY EMPHASIS ON OREGON AND WASHINGTON,

1892—-1975l

1892. Dall, W. H., and Harris, G. D.

Assign the Eugene Formation of Oregon [now
considered early and middle Oligocene] to the
Miocene (p. 227).

1896. Diller, J. S.

Describes and assigns strata on the banks of the
Nehalem River at Pittsburg Bluff, Oreg. to the
Oligocene on the basis of fossil identiﬁcations made
by W. H. Dall. None of the names used in Diller’s
report are currently applied to Pittsburg Bluff
mollusks, as they were subsequently recognized as
new species and so described. This is the ﬁrst notice of
the occurrence of Oligocene strata in the Paciﬁc
Northwest. The report includes a photograph of
Pittsburg Bluff (pl. 7, opp. p. 466).

Diller describes the lithology of strata at Pittsburg
Bluff as follows: "The upper soft gray sandstone is
very fossiliferous in places, and about 30 feet thick.
Below are 20 feet of dark shales which weather gray
*** Some of the layers of sand are indurated so as to
form slabs, thickly set with perfectly preserved

‘Stratigraphic nomenclature used herein is that of the references cited and is not
necessarily in accord with that ofthe US. Geological Survey. My comments are in brackets.

 
fossils.” [Diller did not always distinguish between
the Keasey Formation, a shale now considered late
Eocene and early Oligocene, and the shale that occurs
in the Pittsburg Bluff Formation (p. 466).] On the
Nehalem River “1 mile beyond Vernonia,” he con-
sidered the Keasey to be part of the Pittsburg Bluff
Formation. But at Wilson’s Bluff on the river 3 miles
above Vernonia, he does recognize a difference and
states, “it is evident the shales above Vernonia are
older than those at Pittsburg.”
1898. Dall, W. H.

Tentatively assigns the Tunnel Point “beds” of
Oregon [middle Oligocene] to the Oligocene (table
opp. p. 334).

1903 [1890—1903]. Dall, W. H.

Describes and assigns Callista (Macrocallista)
pittsburgensis from the strata at Pittsburg Bluff to
the Eocene (p. 1253).

1906. Arnold, Ralph.

Assigns the Tunnel Point “beds” to the Oligocene
and correlates them with part of the San Lorenzo
Formation [late Eocene to middle Oligocene] of
California (p. 10). A list of San Lorenzo Formation
fossils is given (p. 17).

1909. Dall, W. H.

Describes two new species, Molopophorus gabbi (p.
45) and Eosiphonalia oregonensis (p. 51), from strata
at Pittsburg Bluff, and gives the species, previously
identiﬁed by Dall as Acila decisa (Conrad), the speci-
ﬁc name shumardi (p. 103). Dall regards these fossils
as Eocene.

1914. Washburne, C. W.

States (p. 73), in commenting on the fossils collected
from beds exposed near Pittsburg that Dall called
Eocene and Miocene, that those which Dall called
Eocene appear to be higher stratigraphically than
those that he called Miocene; he suggests (p. 74) that
these fossils may in fact all be Oligocene. The fossil
identiﬁcations made by Dall are given on page 31.

1914. Anderson, F. M., and Martin, Bruce.

Describe Agasoma columbiana from the Pittsburg

Bluff Formation.
1915. Clark, B. L.

Assigns the fauna at Pittsburg Bluff to the
Oligocene and lists the mollusks, comparing them
with faunas from the Lincoln [Lincoln Creek] For-
mation of Washington [late Eocene to early Miocene],
and the Oligocene of California.

1916a. Weaver, C. E.

Refers the Oligocene rocks of western Washington
to the Clallam Formation [now considered middle
Miocene], which he divides into three zones, char-
acterized, in ascending order, by Molopophorus lin—
colnensis, Turritella porterensis, and Acila gettys—

1916c.

1916e.

1917.

OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

burgensis. He calls the rock units containing these
zones the Lincoln, Porter, and Blakeley “horizons,”
respectively. He notes that Acila shumardi and
Callista pittsburgensis, two species common in the
Pittsburg Bluff Formation, are especially common in
the Molopophorus lincolnensis Zone.

1916b. Weaver, C. E.

Assigns mollusk species common in the Pittsburg
Bluff Formation to the Molopophorus lincolnensis
Zone of western Washington (p. 167).

Weaver, C. E.

Recognizes the Oligocene age (p. 17) of the Gries
Ranch Formation [early Oligocene].
1916d. Weaver, C. E.

Gives the sequence of post-Eocene for western
Washington as follows:

Montesano horizon—Yoldia strigata Zone—upper

Miocene

Wahkiakum horizon—Area montereyana Zone—

lower Miocene

Blakeley horizon—Acila gettysburgensis Zone—

Oligocene
Porter horizon——Turritella porterensis Zone—
Oligocene
Lincoln horizon—Molopophorus lincolnensis
Zone—Oligocene
[The Molopophorus lincolnensis and Turritella
porterensis Zones contain mollusks that occur in the
Pittsburg Bluff Formation.]
Weaver, C. E.

Gives a faunal list for the Acila gettysburgensis
Zone, which he assigns to the late Oligocene.
Dickerson, R. E.

Describes 35 new species from the vicinity of the
Grecco Ranch House, 4 miles east of Vader, Wash.
[Gries Ranch Formation, early Oligocene]. He regards
this fauna as being littoral, of early Oligocene age,
and subtropical; and he believes it to be a lower facies
of Weaver’s Molopophorus lincolnensis Zone.

1918. Clark, B. L., and Arnold, Ralph

Assign the Oligocene marine rocks of western
Washington to the San Lorenzo Group and include
Weaver’s Lincoln, Porter, and Blakeley horizons and
also the SookerFormation of Vancouver Island (p.
298). They believe the Oligocene of Oregon and
Washington was deposited in geosynclinal depres-
sions partly enclosed by land; one of these was proba-
bly a large trough between the Cascades and the
Olympics. They recognize three faunas in
Washington; these are, in decreasing order of age, the
Agasoma acuminatum beds, the Molopophorus
lincolnensis Zone, and the Acila gettysb urgensis Zone.
They believe the differences between the lower two
faunas to be related to temperature.

1921.

 
1918. Van Winkle, K. E.

Divides the Porter beds of southwestern
Washington into an upper part that she calls the
Turritella porterensis Zone, and a lower part [Gries
Ranch Formation] that she calls the Barbatia mer-
riami Zone. She regards Lincoln Creek “beds” as
equivalent to the Molopophorus lincolnensis Zone and
to the middle part of the Porter beds.

1918. Clark, B. L.

Reports that Acila shumardi and Callista
pittsburgensis, species common in the Pittsburg Bluff
Formation, occur in the Kirker Tuff [Oligocene] of
California and assigns the Pittsburg Bluff locality to
the lower Oligocene (footnote 18, p. 59). He records
the occurrence of Callista pittsburgensis Ball and
N uculana lincolnensis (Weaver) in the Kreyenhagen
Shale of California [Eocene and Oligocene], which he
assigns to the San Lorenzo Series (p. 63).

Because certain species that occur in either the
Molopophorus lincolnensis or the Acila gettys-
burgensis Zones occur together in the San Lorenzo in
the Mount Diablo area, he does not believe that these
zones represent distinct geologic horizons.

His paper includes a comprehensive historical
summary of the literature on the marine Oligocene of
the Paciﬁc coast (p. 57—72).

1919. Smith, J. P.

Points out that the Oligocene has fewer tropical
genera than the Eocene and believes that although
Oligocene faunas were already provincial, climatic
zones had not yet been deﬁnitely established. He
regards the Oligocene as oriental in its afﬁnities, but
considers both the Astoria [Miocene] and the San
Lorenzo [late Eocene to middle Oligocene] Formations
as Oligocene.

Clark, B. L.

Places all the Oligocene in the San Lorenzo, which
he divides into two parts, on his correlation chart—a
generalized section for Oregon, Washington, and
northern California. He notes the occurrence of the
typical Pittsburg Bluff species Acila shumardi and
Callista pittsburgensis in the lower part of the San
Lorenzo which he calls the “Molopophorus lincolnen—
sis Zone”. He correlates this zone with the
Kreyenhagen Shale of California and the Vicksburg
Group of the southeastern United States (table opp. p.
586). He divides the Oligocene of the west coast into
two subepochs; these subepochs are represented by
the Molopophorus lincolnensis and Acila gettys—
burgensis Zones which are equivalent to the Lincoln
and San Lorenzo Formations (p. 591—592).

1923. Wagner, C. M., and Schilling, K. H.

Correlate the San Emigdio [late Eocene and
Oligocene] and Pleito [Oligocene] Formations of

INTRODUCTION 5

California with the Pittsburg Bluff Formation and
give a list of fossils for the Pittsburg Bluff Formation.
1925. Clark, B. L.
Describes two new species, Tellina pittsburgensis
and Spisula pittsburgensis, from the type area of the
Pittsburg Bluff Formation.

1925. Hertlein, L. G., and Crickmay, C. H.

First recognize the rocks exposed at Pittsburg Bluff
as a stratigraphic unit and ﬁrst call them the
"Pittsburg Bluffs.” They believe these rocks to be of
undoubted Oligocene age, possibly early Oligocene,
and possibly equivalent to those exposed in San
Emigdio Canyon, California (p. 254).

1927. Schenck, H. G.

Correlates the Yaquina Formation [late Oligocene
and early Miocene], the Eugene Formation [early and
middle Oligocene], and the Tunnel Point Sandstone
[middle Oligocene], at least in part, on the basis of
faunal evidence and reports that diagnostic species in
each of these formations also occur in the Pittsburg
Bluff Formation, which he assigns to the middle
Oligocene.

1928. Cushman, J. A., and Schenck, H. G.

Tentatively regard the Bastendorf [Bastendorff]
Shale and Keasey Formation as lower Oligocene;
these formations are said to be of the same age and
similar facies and to contain certain distinctive
species of foraminifers.

1928. Schenck, H. G.

Describes the Pittsburg Bluff Formation, cites
some of its molluscan fossils, and correlates it with
the Eugene Formation [early and middle Oligocene],
the Tunnel Point Formation [middle Oligocene], and
the Yaquina Formation [late Oligocene and early
Miocene]. He lists mollusks from the Eugene For-
mation, which in his opinion is equivalent to at least a
part of the Molopophorus lincolnensis Zone of
Washington.

1929. Schenck, H. G.

Gives evidence that the Pittsburg Bluff Formation
is younger than the Tejon Formation [Eocene] and
older than the Nye Shale [early Miocene] and that it
probably represents the Lincoln-Porter horizon of
Washington. He notes that some of the diagnostic
species occurring in the Pittsburg Bluff Formation
also occur between rocks of Tejon and Vaqueros
[Eocene and Miocene] age in California.

1929. Clark, B. L.
Divides the Oligocene into three "faunal horizons.”
In Washington, he recognizes three horizons, in
decreasing order of age, the Gries Ranch, Lincoln, and
Restoration Point, but in California he recognizes
only two horizons which he calls the Lincoln and San
Ramon. He ﬁnds the following typical Pittsburg Bluff

 
species in the “Lincoln horizon” of the San Emigdio
Mountains of California: Acila shumardi, Callista
pittsburgensis, and Bruclarkia columbiana (p. 18).

1932. Clark, B. L.

Believes the fauna of the Poul Creek [middle
Oligocene to early Miocene] and Yakataga Forma-
tions [middle Miocene to early Pleistocene] of Alaska
is the same and belongs to one zone—the Blakeley
horizon of Washington. He regards the Blakeley
horizon as late Oligocene and correlates it with the
San Ramon Formation of California and the Sooke
Formation of Vancouver Island.

1936. Schenck, H. G.

Correlates the Pittsburg Bluff Formation in part
with the San Emigdio Formation [late Eocene and
Oligocene] of California, and in part with the Lincoln
[Lincoln Creek] Formation [late Eocene to early
Miocene] of Washington (p. 65).

He gives the name Acila shumardi Zone to a unit
delimited by the range of Acila shumardi (Dall) (p.
44). This unit is said to be about 3,000 feet thick in
Columbia County, Oreg. Among its other diagnostic
species are Bruclarkia columbiana (Anderson and
Martin), Callista pittsburgensis Dall, and Molopo-
phorus gabbi Dall.

1936. Schenck, H. G., and Kleinpell, R. M.

Propose the name Refugian Stage for rocks laid
down after the Tejon Stage (restricted) and before the
Zemorrian Stage. This stage includes the Eugene
[early and middle Oligocene], Pittsburg Bluff [middle
Oligocene], Tunnel Point [middle Oligocene], Keasey
[late Eocene and early Oligocene], and Bastendorf
[Bastendorff] [late Eocene and early Oligocene]
Formations of Oregon, together with the Lincoln
[Lincoln Creek] Formation [middle Oligocene] and the
Gries Ranch Formation [early Oligocene] of
Washington. The Refugian Stage includes the Acila
shumardi Zone. The upper part of the Refugian Stage
is marked by the last occurrence of Acila shumardi,
Callista pittsburgensis, Molopophorus gabbi, and
Bruclarkia columbiana, all of which are common in
the Pittsburg Bluff Formation.

1937. Weaver, C. E.

Suggests that the term Pittsburg Bluff Formation
be applied to the entire middle Oligocene sequence of
sedimentary rocks in Columbia County, Oreg. and
that the type area be considered the exposures be-
tween Pittsburg and Mist on the Nehalem River,
Oreg. (p. 113). He states that fossils are scattered
throughout the Pittsburg Bluff Formation but are
especially abundant in lenses 2 to 6 inches thick, where
they are so compacted as to form calcareous nodules (p.
171).

1937. Clark, H. L.

Reports that a fossil sea urchin has been found in

6 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

the waste from a well dug in sec. 12, T. 3 N., R. 4 W.,
that it is supposed to have come from the Pittsburg
Bluff Formation. [Recent mapping done in connection
with my report shows that it probably came from the
Scappoose Formation of late Oligocene and early
Miocene age.]

1938. Efﬁnger, W. L.

Correlates the Gries Ranch Formation with the
Keasey Formation and the lower part of the Pittsburg
Bluff Formation, both of which he believes to be early
Oligocene (ﬁg. 3, p. 359). He regards the Gries Ranch
fauna as subtropical and believes it to represent a
nearshore or littoral facies (p. 360).

1938. Clark, B. L., and Anderson, C. A.

Show the Pittsburg Bluff and Eugene Formations
as “lower Oligocene” on a correlation chart and
correlate them with the Lincoln [Lincoln Creek]
Formation of southwestern Washington and the San
Lorenzo Group of California. They correlate the
Wheatland Formation with the Keasey and Bas-
tendorf [Bastendorff] Formations in Oregon and the
Gries Ranch Formation in Washington and consider
them to be of late Eocene or early Oligocene age (p.
944).

1938. Kleinpell, R. M.

Assigns the type Lincoln [Lincoln Creek] Forma—
tion of Washington and the Eugene, Pittsburg Bluff,
and Tunnel Point Formations of Oregon to the upper
Refugian. He regards the Bastendorf [Bastendorff]
Shale and Keasey Formation of Oregon as lower
Refugian and believes that the Gries Ranch Forma-
tion of Washington also is probably lower Refugian.

He notes that the molluscan assemblages of the
Acila shumardi Zone of Schenck are deﬁnitely as-
sociated with upper Refugian foraminifers. These
foraminifers are believed to have lived in deeper
water, or at least cooler water, than those of the lower
Refugian Turritella variata Zone of California (p. 152).

To Kleinpell the foraminifers of the Refugian Stage
suggest a cool-water habitat near the edge of the
continental shelf, but not necessarily in a boreal prov—
ince. Foraminifers characteristic of shallower water
are numerous only locally, and there is a notable
decrease of the open—sea types so abundant in the late
Eocene. Southern foraminifers are scarcer on the
whole than in the two directly overlying stages,
suggesting that the climate was somewhat cooler in
the middle Oligocene.

1942. Weaver, C. E.

Describes and illustrates all the known species of
mollusks from the Pittsburg Bluff Formation and
includes a checklist of all the species known to occur
in the Tertiary formations of Oregon and
Washington.

 
1943. Forrest, L. C.

Includes a chart of Oligocene formations in
California and compares current age assignments
with former age assignments (pl. 3).

1943. Hanna, G. D., and Hertlein, L. G.

Note the occurrence of Callista pittsburgensis in the
Kreyenhagen Shale [Eocene and Oligocene] in
California.

1944. Zimmerman, John, Jr.

Regards the Tumey Sandstone, exposed in Fresno
County, Calif, as late Eocene and early Oligocene,
but believes that if the Acila shumardi zone is upper
Refugian, the Tumey faunule is also. He correlates
the Tumey with at least a part of the San Emigdio
Formation, which also contains Acila shumardi. He
notes that the Tumey Sandstone contains several
mollusks characteristic of the Pittsburg Bluff
Formation.

1944. Allen, J. E., and Baldwin, E. M.

Consider the Bastendorf [Bastendorff] Shale mostly
latest Eocene but possibly in part early Oligocene.
They report it consists predominantly of shale and is
2,095 feet thick.

They note that the Tunnel Point Sandstone is mid—
dle Oligocene, overlies the Bastendorf [Bastendorff]
Shale with apparent conformity, consists mainly of
sandstone, and is 800 feet thick.

1944. Durham, J. W.

Reports the occurrence of Acila shumardi in the
Molopophorus stephensoni, M. gabbi, Turritella
olympicensis, and T. porterensis Zones, which col-
lectively make up the Gries Ranch, Pittsburg Bluff,
and Lincoln [Lincoln Creek] Formations. He states
that the Pittsburg Bluff fauna is restricted to the
Molopophorus gabbi Zone and is characterized by
Bruclarkia columbiana, Molopophorus dalli, Perse
olympicensis quimpersensis, P. pittsburgensis, and
Mactra pittsburgensis.

1944. Keen, A. M., and Bentson, Herdis

Show that a marked decrease in the total number of
Tertiary molluscan species occurred in California
during the Oligocene (ﬁg. 3, p. 8).

1945. Warren, W. C., Grivetti, R. M., and Norbisrath,
Hans

Report the Pittsburg Bluff Formation to be dis—
conformably underlain by the Keasey Shale [late
Eocene and early Oligocene] and disconformably
overlain by beds of Blakeley age [late Oligocene or
early Miocene]. The basal member of the Pittsburg
Bluff Formation is a moderately indurated, massive,
quartzose sandstone, marine at the type locality, but
terrestrial on Pebble Creek. This basal member is at
least 500 feet thick. It is overlain by a massive to
poorly stratiﬁed, sandy tuffaceous shale member

INTRODUCTION 7

which includes numerous ash beds that are mostly
less than 1 foot thick. The thickness of the Pittsburg
Bluff Formation along the United Railway is about
850 feet.

Fossils at the type locality (USGS 15264) occur in
the sandstone member and belong to the Molo-
pophorus gabbi Zone, but the upper part of the shale
member may belong to a slightly younger zone. The
authors list 40 species of mollusks, identiﬁed by H. E.
Vokes.

1946. Warren, W. C., and Norbisrath, Hans

Describe the lower part of the Pittsburg Bluff
Formation as composed of ﬁne-grained marine
sandstone containing numerous fossils in layers
along the bedding and in calcareous concretions.
These beds apparently pass upward into coarser
massive sandstone which interﬁngers with
crossbedded, nearshore, marine, and brackish-water
sandstone. Higher in the section there are fewer
molluscan fossils and more brackish-water beds
containing plant remains. Near the top there are few
fossils and many thick beds of tuffaceous material.
The type locality, on the Nehalem River Highway
near Pittsburg, displays marine fossiliferous beds and
is near the base of the formation. The formation as a
whole is characterized by a nearshore megafauna
that is rich in the number of individuals of certain
species. Representative mollusks are listed (p. 230).

The rocks disconformably overlying the Pittsburg
Bluff Formation are named the Scappoose Formation
[late Oligocene and early Miocene] (p. 231).

The authors regard the fauna of the Pittsburg Bluff
Formation as similar to that of the Molopophorus
gabbi Zone of Durham (1944, p. 112), but believe that
the middle part of the Quimper Sandstone and the
beds at Clatskanie, Oreg., correlated by Durham with
the Pittsburg Bluff, are equivalent to the Gries Ranch
Formation and therefore older.

1946. Detling, M. R.

Believes that the Bastendorf [Bastendorff] Shale is
either Eocene or Oligocene and that it may have been
deposited in warm or temperate shallow water near
the shoreline.

1947. Lowry, W. D.

States that the shoreline of the Oligocene sea in
northwestern Oregon almost paralleled the present
coastline and was east of Eugene, Albany, and Sil-
verton and west of Portland, Oreg. (p. 3).

Believes that the coal that occurs in the Pittsburg
Bluff Formation 21/2 miles west of Scappoose and 1
mile south of Deer Island, Oreg., indicates the
shoreline was nearby (p. 6).

1948. Vokes, H. E., and Snavely, P. D., Jr.
Report that in the Eugene area the earliest middle

 
Oligocene sediments were deposited in a restricted
seaway north of the Eugene quadrangle. The con-
tinental deposits of the Fisher Formation had been
laid down throughout this area, and the sea advanced
over them toward the south. In the transgressing sea,
the Eugene Formation was deposited in shallow
offshore water.
1948. Rau, W. W.

Believes that all or part of the Porter Shale of
northwestern Washington may be late Eocene, and
possibly none of it of middle Oligocene age (p. 157).
Reports that ﬁve species of foraminifers, and 20
closely related forms found in the Porter Shale, also
occur in the Tumey Formation [early and middle
Oligocene], and that one foraminifer has also been
found in the Keasey Formation [late Eocene and early
Oligocene].

The Porter Shale was deposited offshore in a fairly
shallow, temperate to warm sea.

1952. Durham, J. W.

Finds that the Stepof Bay fauna [Oligocene] of

Alaska has subtropical or warm-temperate afﬁnities.
1953. Moore, R. C., and Vokes, H. E.

Brieﬂy consider in discussing the age of the Keasey
Formation, the Pittsburg Bluff Formation, and
compare the mollusks occurring in the crinoid-
bearing beds of the Keasey with those in the Pittsburg
Bluff Formation. They show part of the Pittsburg
Bluff Formation on an outcrop map of the area in
which the crinoid beds occur. They report that the
Keasey Formation includes the latest Eocene and
early Oligocene and that the crinoid-bearing beds are
probably early Oligocene.

They believe that the Keasey Formation was de-
posited in relatively deep water, below effective wave
action, but near the shoreline. The crinoid—bearing
middle member of the Keasey was deposited in water
ranging to a depth greater than 500 fathoms [914 m].

1953. Weaver, C. E.

States that the Refugian is coeval with the
“Keasey,” “Lincoln,” and "Blakeley” Stages, in
ascending order. He regards the San Ramon Forma-
tion [early Miocene (‘2) ] as Oligocene and correlates it
with the “Blakeley” Stage.

1956. Stewart, R. E.

Considers the Toledo Formation of western Oregon
late Eocene to middle Oligocene in age and assigns
the Moody Shale Member to the late Eocene. He
regards the Bastendorf [Bastendorff] Shale of
southwestern Oregon as late Eocene and early
Oligocene; the upper 700 feet are Oligocene (p. 59).

1958. Brown, R. D., Jr., and Gower, H. D.

Divide the Twin River Formation of Arnold and

Hannibal (1913) in northwestern Washington into

1961.

OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

three members, which they believe, on the basis of
fossil mollusks, foraminifers, and plant leaves, to be
late Eocene to early Miocene (p. 2510). They correlate
the Lincoln [Lincoln Creek] Formation of Weaver
with the middle and upper members of the Twin River
Formation.

1960. Kanno, Saburo

States that the mollusks Cyclocardia (Cyclocardia)
hannibali and Lucinoma columbiana, which occur in
the Pittsburg Bluff Formation, also occur in the
Ushikubitoge Formation [Oligocene] of central Ja-
pan.

MacNeil, F. S., Wolfe, J. A., Miller, D. J., and

Hopkins, D. M.

Show the Acila shumardi Zone as middle and late
Oligocene, the Stepovak Series as early and middle
Oligocene, and the Poul Creek Formation as middle
Oligocene to early Miocene (on a correlation chart of
Tertiary formations exposed in Alaska).

They state that some stocks of the mollusks were of
Asiatic origin and occur in older rocks in Alaska than
in Oregon and California.

1963. Snavely, P. D., Jr., and Wagner, H. C.

Describe marine Oligocene rocks of western Oregon
and Washington as consisting of massive tuffaceous
siltstone and ﬁne-grained sandstone with interca-
lated beds of pumiceous lapilli, tuff, and glauconite (p.
16). They include a paleogeologic map showing the
Oligocene coastline (ﬁg. 13, p. 15).

1964. Brabb, E. C.

Subdivides the San Lorenzo Formation of the
central California Coast Ranges into the Two Bar
Shale Member [late Eocene] and the Rices Mudstone
Member [late Eocene and Oligocene]. The foraminif—
ers Uvigerina cocoaensis, "Planulina” haydoni, and
Cibicides hodgei (p. 677) occur in the lower part of the
Rices Mudstone Member. [These species are present
in the Bastendorff Shale] The type section of the
Rices Mudstone Member contains the Pittsburg Bluff
mollusks Litorhadia washingtonensis and Nemocar—
dium lorenzanum (p. 677).

He reports that many or all of the mollusks found by
Arnold (1908) in the San Lorenzo Formation occur in
the upper part of the Rices Mudstone Member or the
Vaqueros Sandstone (p. 675).

1964. Zullo, V. A., Kaar, R. F., Durham, J. W., and
Allison, E. C.

List the occurrence of 36 taxa, representing 7 phyla,
in the Keasey Formation, which they believe to have
been deposited in water about 200 fathoms (350 m)
deep. They believe the undisturbed echinoids indicate
either rapid live burial or a scarcity of scavengers and
detritus feeders.

1965. Burke, C. A.

 
Reports that collections of Oligocene fossils from
the Alaska Peninsula are characterized by Acila
shumardi and resemble those of the Lincoln Creek
Formation in Washington (p. 113—114).

1965. MacNeil, F. S.

Believes the Oligocene faunas of Alaska are pre-
dominantly of Asiatic origin and many Asiatic species
appeared earlier in Alaska than in Oregon or
California.

[Mollusks that occur in the Pittsburg Bluff For-
mation are found in the Stepovak Formation, early
and middle Oligocene]

1966. Oakeshott, G. B.

Considers, on a correlation chart (ﬁg. 3, opp. p. 36),
the following marine formations of the California
Coast Ranges to be at least in part middle Oligocene:
Tumey Formation, “Kirker” Sandstone, San Ramon,
San Lorenzo, and Alegria Formations.

1966. Dibblee, T. W., Jr.

Reports that the Alegria Formation near Santa
Barbara, Calif., contains Callista sp. cf. C.
pittsburgensis and Acila shumardi, species that occur
in the Pittsburg Bluff Formation. The entire fauna
indicates an Oligocene (Refugian) age, as does the
fauna from the Gaviota Formation.

1967. Wolfe, J. A., and Hopkins, D. M.

State that a sharp cooling took place during the
middle Oligocene (p. 72, ﬁg. 3), and that radiometric
dates indicate this cooling took place within an in—
terval no longer than 2 million years and possibly as
short as 1 million years.

1967. DeLise, K. C.

Lists the following Pittsburg Bluff mollusk species
as occurring in the upper sandstone unit of the San
Emigdio Formation of California (p. 16): Acila
shumardi, Bruclarkia columbianum?, and Polinices
washingtonensis. [Also cites Molopophorus dalli, a
species that seems in Oregon to be restricted to the
early Oligocene]

1969. Hickman, C. J. S.

Describes two new species that occur in both the
Pittsburg Bluff Formation and the Eugene Formation
[early and middle Oligocene]: Tellina aduncanasa
and Neverita thomsonae. Seventeen species common
to both the Eugene and Pittsburg Bluff Formations
are described.

She states that the Eugene Formation is early and
middle Oligocene and contains a fauna of mixed
Keasey and Pittsburg Bluff afﬁnities.

1969. Denton, G. H., and Armstrong, R. L.

State that the Poul Creek Formation in southern
Alaska is of late Oligocene or early Miocene age, is
1,875 m thick, and consists of marine sediments de-
posited in a temperate or subtropical climate (p. 1137).

INTRODUCTION 9

1969. Fairchild, W. W., Wesendunk, P. R., and
Weaver, D. W.

Report a slight cooling throughout the area of the
present California Coast Range during the time that
the San Lorenzo Formation, of late Eocene to middle
Oligocene age, was being deposited.

1969. Snavely, P. D., Jr., MacLeod, N. S., and Rau,
W. W.

Refer the Oligocene siltstone of the Newport area,
Oreg., informally called “siltstone of Alsea” and
previously included in the upper Toledo Formation, to
the upper Refugian and the Zemorrian Stages.
[Mollusks indicate a middle Oligocene to late
Oligocene or early Miocene age for this unit]

1970b. Addicott, W. O.

Considers the Oligocene “Lincoln Stage” equiva-
lent to the biozone of Acila shumardi, which is as-
signed to the Refugian Stage. He believes less than 10
percent of the still-living genera from the Acila
shumardi Zone of the San Emigdio Mountains, Calif,
are tropical or subtropical.

He believes the mollusks of the lower part of the
“Lincoln Stage” are marginally subtropical to warm
temperate.

He reports that more than half of the molluscan
genera from the lower part of the “Lincoln Stage”
today range northward into the temperate Oregonian
molluscan province. He believes the late Oligocene
Echinophoria rex Zone of Durham (1944) was proba-
bly warm temperate.

He believes that the decreases in warm-water
genera and taxonomic diversity show cooling during
the middle Oligocene.

1971. MacNeil, F. S.

Reports that species of mollusks and closely related
forms found} in the Pittsburg Bluff Formation are
found in the Poul Creek Formation [middle Oligocene
to early Miocene].

1972. Berggren, W. A.

Considers the Refugian Stage late Eocene and the
Zemorrian Stage Oligocene.

1972. McKeel, D. R., and Lipps, J. H.

Believe planktonic foraminifers and coccoliths
from the middle part of the siltstone of Alsea, exposed
along the north side of Alsea Bay, near Newport,
Oreg., suggest a latest Eocene or earliest Oligocene
age for this unit.

1973. Addicott, W. 0.

Reports thatBruclarkia columbiana (Anderson and
Martin), a Pittsburg Bluff species, occurs in the
Cymric Shale Member [Oligocene] of the Temblor
Formation in California. Neverita thomsonae
Hickman, Panopea ramonensis (Clark), and Den—
talium laneensis Hickman, also Pittsburg Bluff

 
species, occur in the Wygal Sandstone Member
[Oligocene] of the Temblor Formation.

He notes that Bruclarkia columbiana is restricted
to the upper part of the Refugian Stage in California
but is found in the middle and upper part in western
Washington, which is equivalent to the Acila
shumardi Zone and the “Lincoln Stage.” He states
that beds containing Bruclarkia columbiana can be
traced into the lowermost part of Kleinpell’s type
Zemorrian section suggesting that the Refugian and
Zemorrian Stages are in part coeval.

1973. Jeletzky, J. A.

Recognizes the post-late Eocene regional molluscan
stages—Keasey (in part), Lincoln, Blakeley, and
Clallam—of the Paciﬁc northwest from southeastern
Alaska to southwestern Oregon. Within this northern
region of the Paciﬁc coast, these zones persist through
intertidal pebble conglomerate, grit, and sandstone to
outer neritic or bathyal siltstone and shale. The
southern molluscan faunas of the Paciﬁc coast served
as a basis for another regional sequence of molluscan
stages—Lorenzian, Vaquerosian, Temblorian, Monte-
reyan, and Margaritan. He suggests that the post-late
Eocene molluscan and foraminiferal faunas of western
North America were controlled by water temperature.

He believes that the northern set of Tertiary
molluscan stages and zones, when used within the
northern region, are equal or superior to the regional
foraminiferal zones and stages.

He correlates the Lincoln molluscan stage of the
northern Paciﬁc coast with the upper Refugian
foraminiferal stage, and places part or all of the
Keasey molluscan stage of the northern region in the
uppermost Eocene.

1974. Watkins, Rodney

Names four communities of mega-invertebrates in
the Kreyenhagen Formation [Eocene and Oligocene]
in the Arroyo Ciervo area, Calif, that he considers
mappable ecologic units. Two are named for
characteristic Pittsburg Bluff species, the “Mac-
rocallista pittsburgensis Community,” which consists
largely of M. pittsburgensis, and the “Nuculana
washingtonensis Community,” which consists almost
entirely of N. washingtonensis and associated M.
pittsburgensis. The Pittsburg Bluff Formation of
Oregon is in a “Northern Province” with 17 or less
percent of warm-water genera. The fauna probably
lived in a littoral or very shallow sublittoral en-
vironment. Macrocallista pittsburgensis is eurytropic
and maintains large populations in several envi-
ronments.

1975. Snavely, P. D., Jr., MacLeod, N.S., Rau, W. W.,
Addicott, W. 0., Pearl, J. E., and Quin-
terno, P. J.

10

Name and describe the Alsea Formation [early to
late Oligocene], exposed along the shore of Alsea Bay,
Oreg., and correlate it with the Eugene and Pittsburg
Bluff Formations and the upper part of the Keasey
Formation in Oregon, and with the Lincoln Creek and
Blakeley Formations and the middle and upper
members of the Twin River Formation in
Washington.

ACKNOWLEDGMENTS

I am indebted to my colleagues Warren 0. Addicott,
US. Geological Survey; W. P. Woodring, US. National
Museum; F. Stearns MacNeil, Fort Myers, Fla.; Arnold
Ross and George E. Radwin, San Diego Natural History
Museum, for helpful discussions, advice, and assistance.
The late Leo G. Hertlein, California Academy of Sci-
ences, provided me with type specimens and informa-
tion pertinent to them and was helpful in many other
matters. Joseph H. Peck, University of California, and
Horace G. Richards, Academy of Natural Sciences of
Philadelphia, kindly made available to me type fossils
that I needed. To Kenji Sakamoto, US. Geological
Survey, I am especially indebted for his patience and
care in taking the photographs that illustrate this
report.

The San Diego Natural History Museum kindly made
ofﬁce space available to me, and Mrs. Azalea Gorby,
Librarian, obtained needed references. Anthony
D’Attilio graciously agreed to draw the suture sketch of
Turritella pittsburgensis, n. sp. To the entire staff of the
museum I would like to extend my thanks for their
kindness and willingness to offer assistance when
needed.

Kenneth W. Ciriacks, Amoco Production Co., Tulsa,
Okla., provided me with information relating to the
occurrence of Pittsburg Bluff species in Alaska. The
release of this information was granted by Amoco
Production 00., Denver Division, Colo.

The Crown Zellerbach Corp., Vernonia, Oreg., kindly
made available a map of the corporation’s tree farm.

I am indebted to the late Frank C. Calkins, formerly a
geologist in the US. Geological Survey, who at the age
of 95 increased the readability of the nontechnical parts
of my manuscript.

PITTSBURG BLUFF FORMATION
STRATIGRAPHY
GENERAL FEATURES AND GEOGRAPHIC DISTRIBUTION

The Pittsburg Bluff Formation is conﬁned to north-
western Oregon (ﬁgs. 1—3). Most of its exposures are in
the Vernonia 15-minute quadrangle and in the north-
western quarter of the Forest Grove 15-minute quad-
rangle, but a few exposures of it, containing fossils, are
found in the Cathlamet and Svenson 15—minute quad-
rangles. The formation is characterized by gentle

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

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FIGURE 1.—Location of area of study at Vernonia, Oreg.

northwest—trending folds superimposed on an eastward
regional dip of about 5°. It is underlain by the Keasey
Formation (late Eocene and early Oligocene) and over-
lain by the Scappoose Formation (late Oligocene and
early Miocene) (ﬁg. 4).

The precise stratigraphic assignment of some fossil
localities within the Pittsburg Bluff Formation is un-
certain owing to discontinuity in outcrops. Local struc-
ture compounds the stratigraphic uncertainty. South-
eastward from the type locality, for example, many of
the richest collections, all of approximately the same

PITTSBURG BLUFF FORMATION 1 1

 
FIGURE 2.-—Type locality of Pittsburg Bluff Formation 1 km northeast
of Pittsburg, Oreg. The calcite-cemented concretions are aligned
with a bed rich in molluscan fossils. Trough-shaped sedimentary
structure (at top) may have formed when sand slid downward on
submarine slope.

age, were taken at widely separated localities in a long
anticlinal valley drained by the East Fork of the
Nehalem River.

TYPE LOCALITY

The type locality, which exposes the lower part of the
Pittsburg Bluff Formation, but not quite the base, is a
roadcut on Oregon State Highway 47, 1 km northeast of
Pittsburg, where the exposed section is about 10 m
thick. The typical sequence in this cut consists of a
2-m-thick layer of sandstone showing prominent
bioturbation overlain by a 10-cm-thick fossiliferous
limy layer or a layer of concretions. These are overlain
by a laminated sandstone with laminae about 5 mm
thick, which becomes bioturbate 1 m above its base. The
entire section is highly fossiliferous, but shells are most
abundant in the limy layers.

TYPE AREA

The type area of the Pittsburg Formation extends
along the Nehalem River between Pittsburg and Mist,
Oreg. The Pittsburg Bluff Formation is about 200 m
thick. The olive-gray siltstone of the Keasey Formation
(late Eocene and early Oligocene) is conformably over—
lain by 30 m of massive olive-gray ﬁne-grained
sandstone (ﬁg. 5). The sandstone is characterized by
fossiliferous concretions (ﬁg. 2), by trough-shaped
prisms possibly resulting from internal shear during
aggradation, and locally by siltstone rip-up clasts (ﬁg.
6). Thin-bedded light-olive-gray ﬁne—grained sandstone
and siltstone with foreset beds and local coal beds near
the top occupy the next 70 In (ﬁg. 4). The uppermost 100
In consists of massive friable olive-gray ﬁne-grained
sandstone. The Pittsburg Bluff Formation is overlain by

 
dusky-yellow ﬁne-grained tuffaceous sandstone of the
Scappoose Formation. Locally the contact is marked by
a cobble conglomerate.

A faunal break occurs approximately in the middle of
the Pittsburg Bluff Formation. This break possibly may
be only an apparent one, and may merely reﬂect the
facts that the lower part of the formation is generally
more fossiliferous than the upper parts and that it in-
cludes the easily accessible classic exposure on State
Highway 47. Nonetheless, a difference in the molluscan
fauna exists and may reﬂect a real change in the com—
position of the Pittsburg Bluff fauna. At one locality,
USGS 15588, at the base of the upper part of the forma-
tion, species elsewhere conﬁned to the upper or lower
parts occur together.

The following mollusks occur only in the lower 100 m
of the Pittsburg Bluff Formation (excluding USGS loc-
ality 15588).

Gastropods
Opalia (Dentiscala?) hertleini, n. sp.
Crepidula pileum (Gabb)
Polinices washingtonensis (Weaver)
Sinum aff. S. obliquum (Gabb)
Priscofusus stewarti (Tegland)
Perse pittsburgensis vernoniensis, n. subsp.
Taranis columbiana (Anderson and Martin)
Spirotropis kincaidi (Weaver)
Odostomia winlockiana Efﬁnger

Pelecypod
Crenella porterensis Weaver
The following mollusks occur only in the upper 100 m
of the Pittsburg Bluff Formation (excluding USGS 10-
cality 15588).

Gastropods
Architectonica blanda Dall
Aforia campbelli Durham

Pelecypods
Cyclocardia (Cyclocardia) cf. C. hannibali (Clark)
Spisula (Mactromeris?) veneriformis Clark
The following mollusks occur throughout the entire
thickness of the Pittsburg Bluff Formation.

Gastropods
Turritella pittsburgensis, n.sp.
Cryptonatica pittsburgensis, n. sp.
Neverita (Glossaulax) thomsonae Hickman
Eosiphonalia oregonensis (Dall)
Bruclarkia columbiana (Anderson and Martin)
Molopophorus gabbi Dall
Perse pittsburgensis Durham
Suavodrillia winlockensis (Efﬁnger)
Acteon chehalisensis (Weaver)
Scaphander stewarti Durham

12

45° 55'

45° 50'

45°45'

OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

 
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Oligocene

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EXPLANATION

 
Astoria Formation

 
Columbia River Group

 
Scappoose Formation

TERTIARY

Pittsburg Bluff Formation

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Keasey Formation

 
Contact

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FIGURE 3.——Geologic sketch map of the Vernonia area, northwestern Oregon, showing fossil localities and location of

measured sections.

PITTSBURG BLUFF FORMATION 13

 
N S
Coal Creek
EXPLANATION
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Siltstone Cobble
conglomerate Buxton
Scappoose Formation W‘—‘)o 0 cocoooooooo
E Pittsburg Bluff Formation
Tuffaceous Coal
sandstone
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With concretions FEET METRES
100
Divide 30°
M3858
200
Vernonia 50
Type locality of Pittsburg Bluff "
Formation lies between Moran 100
Farm and Pittsburg
(Dilier, 1896)
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. Pittsburg Bluff Formation

M3860

Keasey Formation

 
6 MILES

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FIGURE 5.——Contact between siltstone of the Keasey Formation (be—
low) and sandstone of the Pittsburg Bluff Formation (above), in
roadcut along logging road 1 km southeast of Pittsburg, Oreg.

FIGURE 6.—Si1tstone rip—up clasts in Pittsburg Bluff Formation in
roadcut along logging road 2 km southeast of Pittsburg, Oreg.

 
14

Scaphophod
Dentalium (F issidentalium?) laneensis Hickman

Pelecypods

Nucula (Leionucula) vokesi, n. sp.

Acila (Truncacila) shumardi (Dall)

Litorhadia washingtonensis (Weaver)

Yoldia (Kalayoldia) oregona (Shumard)

Mytilus cf. M. snohomishensis Weaver

Lucinoma columbiana (Clark and Arnold)

Felaniella (Felaniella) snavelyi, n. sp.

Nemocardium (Keenaea) lorenzanum (Arnold)

Spisula (Mactromeris) pittsburgensis Clark

Tellina (E urytellina) aduncanasa Hickman

Tellina? pittsburgensis Clark

Solen townsendensis Clark

Solena (Eosolen) eugenensis (Clark)

Panopea snohomishensis Clark

Panopea ramonensis Clark

Cochlodesma bainbridgensis Clark

Thracia (Thracia) condoni Dall

The pelecypods do not indicate any striking faunal

break, but the gastropods do; 9 of 23 species are re-
stricted to the lower part of the Pittsburg Bluff Forma-
tion. This break suggests, therefore, that two faunal
zones may be present in the Pittsburg Bluff Formation
in its type area, one in the lower 100 In and one in the
upper.

CHECKLIST OF PITTSBURG BLUFF SPECIES

Exposures of the Pittsburg Bluff Formation are
found in an area of about 150 kmz; they indicate a
maximum thickness of approximately 200 In. As
paleontologists and geologists have been collecting fos-
sil mollusks from the formation since the early 1900’s, it
is reasonable to assume that their collections contain
specimens of most of the animals with preserved hard
parts that lived in the middle Oligocene sea of that part
of northwestern Oregon. A checklist of the Pittsburg
Bluff mollusks is given in table 1.

As most of the collections studied were made by other
workers and had already been prepared, it was not
possible to determine if all the specimens were collected
from one stratigraphic interval, nor if each collection
represented all the specimens available. Parts of the
U.S. Geological Survey collections made by H. E. Vokes
and others in the early 1940’s had not been prepared.
For these and my own collections, abundance could be
accurately noted, and it was noted during my own
collecting in the ﬁeld.

The number of specimens representing a species in a
collection of fossils is not necessarily related to the
abundance of that species at a given fossil locality. If a
species is easily removed from the enclosing rock, as are
many of the naticids and also some pelecypods such as

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Acila, it is apt to be collected in large numbers. If one
attempts to remove a fragile valve of a pelecypod from
its matrix in the ﬁeld, it is likely to break up into small
pieces which may or may not be brought back with the
collection. If a genus, such as Turritella, Liracassis, or
Acila, is known to be of special value for age determi-
nation, or is uniquely sculptured, the collector is likely
to make a special search for it, and to exercise great care
in removing it from the enclosing rock.

Even when a geologist is trying to collect a complete
assemblage, he may fail to do so unless he collects ev—
erything he ﬁnds, for it is often difﬁcult to distinguish
similar species in the ﬁeld. The abundance and variety
of species in a collection may depend on the purpose for
which the collection was made; fewer specimens are
required for a determination of age than for a thorough
study of a fauna.

In an attempt to estimate the relative abundance of
species in the Pittsburg Bluff Formation as exposed in
the area dealt with here, I have noted the number of
specimens of each observed in the ﬁeld and in collections
prepared from slabs of rocks. For some species, the
results thus obtained may be far from accurate, but no
better method seems to be available. I have not given
numbers of specimens for each locality but have adopted
the terminology that Smith and Gordon (1948) used in
reporting the abundance of species of living mollusks in
Monterey Bay, Calif, and applied it to the fauna as a
whole:

Abundant: found nearly everywhere, usually more
than 20 specimens.

Common: usually found in moderate abundance (10
to 20 specimens).

Scarce: found at several localities, usually singly or
only a few together

Rare: A total of only a few specimens found by me or
known to have been collected by others.

The following list gives the relative abundance of
species found in the Pittsburg Bluff Formation:

Gastropods

Abundant
Cryptonatica pittsburgensis, n. sp.
Polinices washingtonensis (Weaver)
Neverita (Glossaulax) thomsonae Hickman
Bruclarkia columbiana (Anderson and Martin)
Molopophorus gabbi Dall
Perse pittsburgensis Durham

Common
Perse pittsburgensis vernoniensis, n. subsp.
Taranis columbiana (Anderson and Martin)
Spirotropis kincaidi (Weaver)
Suavodrillia winlockensis (Efﬁnger)
Scaphander stewarti Durham

15

PITTSBURG BLUFF FORMATION

 
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16

Scarce
Turritella pittsburgensis, n. sp.
Eosiphonalia oregonensis (Dall)
Priscofusus stewarti (Tegland)
Acteon chehalisensis (Weaver)
Raw
Architectonica blanda Dall
Opalia (Dentiscala?) hertleini, n. sp.
Crepidula pileum (Gabb)
Sinum aff. S. obliquum (Gabb)
Aforia clallamensis wardi (Tegland)
Odostomia winlockiana Efﬁnger
Scaphopod
Cmnmmz
Dentalium (F issidentalium?) laneensis Hickman
Cephalopod
Rare
Aturia angustata (Conrad)
Pelecypods
Abundant
Acila (Truncacila) shumardi (Dall)
Litorhadia washingtonensis (Weaver)
Callista (Macrocallista) pittsburgensis Dall
Spisula (Mactromeris) pittsburgensis Clark
Cmnmmz
Yoldia (Kalayoldia) oregona (Shumard)
Felaniella (Felaniella) snavelyi, n. sp.
Tellina (Eurytellina) aduncanasa Hickman
Tellina pittsburgensis Clark
Solen townsendensis Clark
Solena (Eosolen) eugenensis (Clark)
Panopea ramonensis Clark
Thracia (Thracia) condoni Dall
Scarce
Nucula (Leionucula) vokesi, n. sp.
Lucinoma columbiana (Clark and Arnold)
Nemocardium (Keenaea) lorenzanum (Arnold)
Pitar (Pitar) dalli (Weaver)
Spisula (Mactromeris?) veneriformis Clark
Panopea snohomishensis Clark
Rare
Cochlodesma bainbridgensis Clark
Mytilus cf. M. snohomishensis Weaver
Crenella porterensis Weaver
Cyclocardia (Cyclocardia) cf. C. hannibali (Clark)
?Ervilia oregonensis Dal]

ECOLOGY

The Pittsburg Bluff Formation contains 43 identiﬁed
genera of mollusks represented by 48 species, almost
equally divided between pelecypods and gastropods and
including one scaphopod and one cephalopod. Five of the
gastropod genera are extinct: Eosiphonalia, Molo-
pophorus, Bruclarkia, Perse, and Priscofusus, and three

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

are locally extinct: Architectonica, Sinum, and Turri-
tella. The pelecypod subgenus Eosolen is apparently
restricted to the Eocene and Oligocene, and so is
Litorhadia, which some authors classify as a subgenus
of N uculana.

Thirteen of the total of 48 species are so abundant that
almost any persistent collector would ﬁnd them.
Fourteen species are so rare that only one to ﬁve
specimens of each have been found, presumably as the
result of exhaustive collecting. The remaining 21
species are represented, on the average, by about 20
specimens each and may be assumed to constitute an
important part of the fauna. A striking characteristic of
the Pittsburg Bluff fauna is that an enormous number of
fossils of a few species are tightly packed in the cal-
careous concretions and lenses within the formation.
These are Callista (Macrocallista) pittsburgensis, Acila
(T runcacila) shumardi, Molopophourus gabbi, Perse
pittsburgensis, and the four naticid species that the
formation contains.

The pelecypods, with the exception of two small
mytilids represented only by incomplete shells, are
characteristic of an infauna (Thorson, 1957) that lived
buried or burrowing in muddy sand on the sea bottom.
Of the gastropods, all but Crepidula (represented by one
well-preserved and three poorly preserved specimens)
lived on or within the sediment of the sea ﬂoor. Rare or
absent are forms that lived only on rocky shores or on an
open sandy beach. Several of the genera that are par-
ticularly abundant in the fauna—for example Polinices
and Neverita—are known to be voracious feeders on
clams (Hedgpeth and Hinton, 1961; Keen, 1971).
Gastropods of the extinct genera Eosiphonalia,
Bruclarkia, Perse, and Molopophorus, which lack the
round aperture usually possessed by herbivorous snails,
have long siphonal canals, indicating that they may
have been detritus feeders or carnivores, preying upon
clams; their familial assignments, if correct, imply that
they were carnivores. The drill holes found in some
pelecypod valves are straight sided, similar to the holes
made by the Muricacea, none of which are known from
the Pittsburg Bluff Formation, unless one of these
extinct genera is missassigned. The formation also
contains Turritella, which is known to live buried just
beneath the sea ﬂoor and to feed upon detritus; Opalia,
which is a carnivorous genus, with some species known
to feed upon sea anemones and corals (Keen, 1971); and
Odostomia, which is known to be parasitic upon other
mollusks such as Ostrea, Pecten, and Crepidula, and
upon polychaete worms (Keen, 1971). The only
scaphopod represented is Dentalium, which lives buried
under a thin layer of sediment on the sea ﬂoor (Keen,
1963), and the only cephalopod is Aturia, which
presumably inhabited moderately shallow water and

PITTSBURG BLUFF FORMATION

was carnivorous, perhaps feeding on decapod crus-
taceans (Miller, 1947, p. 13) or mollusks.

The Pittsburg Bluff molluscan fauna contains none of
the rock dwellers of the littoral zone with the possible
exception of M ytilus, and no snails that are known to be
herbivorous. None of the mollusks found in the for-
mation, except the turrids, are considered indicative of
deep water. No remains of echinoderms or crabs have
been found, and foraminifers are represented by two
poorly preserved globigerinids. Some ﬁsh remains have
been found; the teeth identiﬁed are of sharks and rays.
Welton (1972, p. 168) makes the following statement

concerning the shark teeth:

***the lower sections of the Pittsburg Bluff Formation yield
numerous teeth of a small squalid shark Centroscymnus and not
uncommonly teeth of Raja, Squatina, Odontaspis, Squalus, Pris-
tiophorus, and Notorhynchus. These genera, plus several additional
forms, collectively constitute the most diverse assemblage yet known
from the middle Oligocene of Oregon.

Otoliths from USGS 15310, in the middle part of the
Pittsburg Bluff Formation, were identiﬁed by John E.
Fitch, California Department of Fish and Game, as
belonging to the families Congridae (conger eels) and
Macrouridae (rat tails), both bottom-dwelling families
that typically inhabit moderate (200 m) to great depths
(500 m), and, although found in all oceans of the world,
are least common in tropical seas (John E. Fitch, writ-
ten communs., May 23, 1973, and June 18, 1973).

From the preserved molluscan fauna, a picture
emerges of an infaunal community of ﬁlter feeders,
detritus feeders, and carnivores living on or within the
sediment of the sea ﬂoor.

The table below (table 2, compiled from Abbott, 1954;

TABLE 2.—Holocene genera in the Pittsburg Bluff Formation and their
preferred bottom sediment and water depth

17

TABLE 2.—Holocene genera in the PittsburgBluff Formation and their
preferred bottom sediment and water depth—Continued

 
Genera Bottom sediment Depth of water

 
Gastropods

 
,,,,,,,,,,,, Common in sand and Tideﬂats to 60 m.

sand-mud bottom.

Architectonica

 
Genera Bottom sediment Depth of water
Scaphopod
Dentalium (Fissidentalium) __________________________ 7 to 1,200 m.
Pelecypods
Nucula (Leionucula) A _. Clay, sand. 20 to 1,800 m.
Acila (Truncacila) H 10 to 1,300 m.

 
Yoldia (Kalayoldia) _
Mytilus

Crenella ,,,,,,,,,,,,,,,,,,
Cyclocardia ,,,,,,
Lucinoma
F elaniella

 
Nemocardium (Keenaea), W _
Pitar ,,,,,,,,,,,,,,,,,,,,,,

Callista (Macrocallista) ”ﬂ

Spisula (Mattromeris) ,,,,,,

Emilia ,,,,,,,,,,,,,,,,,,,,
Tellina (Eurytellina)

Solen

Panopea ,,,,,,,,,,,,,,,,,,

Cochlodesma ______________
Thracia

Mud.

Sand.

Sand or mud, under rocks,
usually in nest of
agglutinated rubble;
intertidal sand-beach and
sand ﬂats; nearshore
sand and sand-mud.

Outer shelf, sand bottom.

Coarse sand; intertidal
sand-beach and sand
ﬂats; nearshore sand
and sand-mud.

Fine sand.

Sand of exposed beaches;
ﬁne sand or ﬁrm sandy
mud of bays, sloughs, or
estuaries; ﬁne sand or
sandy mud of protected
open coast.

Sand or mud; coarse,
shifting sand near
entrances to bays,
lagoons, or estuaries;
sand or mud in bays;
intertidal sand-beach
and sand ﬂats; nearshore
sand and sand<mud;
outer shelf, sand.

Sandy mud of sheltered
bays, sloughs, or
estuaries; sandy
beaches, coves.

Sandy mud of bays,
sloughs, or estuaries
buried about 1 m.

Mud, rubble-reef, rock

Intertidal to 1,800 m.

Intertidal to 50 m or
perhaps more.

2 to 450 m.

20 to 1,800 m.

Intertidal to 540 m.

Intertidal to 75 m.

20 to 140 m.
Intertidal to 180 m.

Common in shallow water;
not uncommonly washed
ashore after storms.

Intertidal to 45 in.

Just offshore to 90 m.
Intertidal to 140 m.

Intertidal to 75 m.

Intertidal to possibly subtidal.

20 to 90 m.
Intertidal to 140 m, nestling.

Turitella __________________ Soft bottom, sand or mud. Subtidal to 180 m.
Opalia (Dentiscala) ,,,,,,,, At base of sea anemones, Usually less than 15 but may
under kelp. he as much as 90 m.
Crepidula ________________ Rock or shell, Intertidal to 160 m.
Cryptonatica ______________ Sand. Intertidal to 1,600 m.
Polinices (Polinices) ,,,,,,,, Bay sand ﬂats, mud ﬂats, Intertidal to 2,500 m.
clay.
Neverita (Glossaulax) ______ Sand bars, bay sand ﬂats. Intertidal to 45 m.
Sinum ,,,,,,,,,,,,,,,,,,,, Sand or mud ﬂats Intertidal to 45 m.

among small stones.

Aforia ,,,,,,,,,,,,,,,,,,,,

 
60 to 2,500 m.

Bipolar; descends into deep
equatorial waters for requis-
ite bottom temperature.

180 to 750 m.

730 to 3,650 m.

Odostomia ________________ Parasitic on mollusks; Intertidal to 640 m.
common near eelgrass
roots.

Acteon ,,,,,,,,,,,,,,,,,,,, Sand, bayAmud ﬂats. Intertidal to 75 m.

 
, 20 to 5,200 m.

 
cavities, sponge beds.

 
Berry, 1954; Burch, 1944—46; Eyerdam, 1960; Fitch,
1953; Hedgpeth and Hinton, 1961; Javidpour, 1973;
Keen, 1963, 1971; McLean, 1969; Oldroyd, 1924; Pack-
ard, 1918; and Parker, 1963) shows the known depth of
water and bottom sediment inhabited by Holocene
genera represented in the Pittsburg Bluff fauna.

Although none of the Pittsburg Bluff molluscan fos-
sils have been found in life position, many pelecypods
are preserved as articulated specimens; this fact
suggests that they were transported rapidly or a re-
latively short distance. Fragments of shells make up 50
percent of the matrix, and these fragments represent

18 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

the same species of mollusks that are found as entire
specimens. All the species found together did not
necessarily live together in identical environments or at
the same depth. Three habitats are suggested—one of
deep water, perhaps at least 100 In; one of moderately
shallow water, perhaps about 20 m; and one of shallow,
nearshore water, less than 20 and some of it intertidal.
None of the genera lived in high-energy coastal
environments.

The following genera and subgenera are considered
indicative of sand or mud ﬂats, bars, or shallow
protected bays:

Gastropods

Opalia (Dentiscala)
Polinices (Polinices)
Neverita

Sin um

Acteon

Pelecypods

F elaniella

Pitar

Spisula (Mactromeris)
Tellina (Eurytellina)
Solen

Panopea

Genera and subgenera that usually occur together at
depths of 20 m or more, but not as a rule intertidally,
include the following:

Gastropods

Turritella
Scaphander

Scaphopod

Dentalium
(Fissidentalium?)

Pelecypods

N ucula (Leionucula)
Acila (Truncacila)
Yoldia (Kalayoldia)
Crenella

Cyclocardia
Nemocardium (Keenaea)
Ervilia

Cochlodesma

Thracia

Of these, Yoldia and Thracia occur intertidally as well
as at depths of more than 20 m.

The turrids Taranis, Spirotropis, and Aforia have
been found at depths no shallower than 180, 730, and 60

 
m respectively. But of the 10 collections made at
localities in which the turrids are common, 2 contain
Neverita (Glossaulax), which lives intertidally to 45 m, 1
contains S pisula, which lives intertidally to 45 m; and 4
contain Panopea, which is intertidal to possibly subti-
dal. These facts indicate either that the turrids lived in
much shallower water during middle Oligocene time
than they do now, or that their shells were mixed, before
being fossilized, with the shells of genera with which
they did not live.

Thin coal seams, found in the Pittsburg Bluff For—
mation, indicate that the marine environment of the
Pittsburg Bluff Formation was at times intertidal or
supratidal. None of the mollusks found near the coal
beds, however, are indicative of brackish water.

If the Pittsburg Bluff fauna is regarded as primarily
representing a single habitat, it must have lived for the
most part in water from about 20 to about 50 m in depth.
Mytilus and Panopea perhaps were carried in
mechanically from shallower water, although M ytilus is
found at a depth of 45 m andPanopea is believed to enter
the subtidal realm. In addition, the fossilized valves of
Panopea in the Pittsburg Bluff fauna are usually ar-
ticulated, so that if they were moved any appreciable
distance, they must have moved rapidly. The shoreline
must presumably have ﬂuctuated sufﬁciently to include
the coal. The turrids, unless the bathymetric data for
the Holocene genera are nonrepresentative, are in-
compatible with a 20- to 50-m depth habitat. It seems
more probable that the Pittsburg Bluff fauna includes
species from three distinct habitats, brought together
by transportation. Some of the mollusks must have been
moved about for long periods of time or have been
abraded in a high-energy environment for, as stated
earlier, about half of the matrices of the mollusks con-
sist of worn shell fragments of the same species as those
that are found whole. The complete shells enclosed in
this fragmental material are well preserved, and most
of the pelecypod valves are articulated and closed.

In addition to the closed and articulated valves of
strongly hinged Acila, less strongly hinged Callista,
Spisula, Solen, Eosolen, and Panopea are usually
preserved with both valves closed, and ﬁne sculpture is
preserved on most of the gastropods. These well-
preserved shells could not have been rolled by waves or
currents for long distances; they cannot, on the other
hand, have been fossilized where they lived, as none
have been found in life position, and fossil remains of
organisms that must have lived at different depths, in
terms of modern known bathymetric ranges, are
commonly assembled.

The concentrated fossilized shells and shell frag-
ments may have been brought together in stormy
periods. At the present time, after a storm on the coast of

PITTSBURG BLUFF FORMATION 19

southern California, one may ﬁnd on the shores of coves
large quantities of newly assembled worn shell debris
mixed with unworn whole shells of Cypraea, Olivella,
Astraea, Haliotis, F issurella, Tegula, and other gas-
tropods, and often large numbers of pelecypods, such as
Mytilus, that have been washed in while they were
alive, with their valves articulated and closed. After one
fall storm at Jones Beach on the Atlantic Ocean side of
Long Island, New York, mature specimens of Spisula
solidissima Dillwyn, Neverita duplicata (Say), and the
seastar Brisaster were piled up along the shore to a
depth of 0.3 In over a distance of about 0.8 km. All these
animals were alive, and the valves of Spisula were
articulated and closed; none of them are commonly
found on the beach in calm weather (Anthony D’Attilio,
oral commun., 1973). Similar accumulations of live but
displaced animals may be formed even more commonly
in the subtidal zone.

If the intertidal genera cited lived on sand or mud
bars in a bay, they would have been especially vulnera-
ble to transportation and fairly rapid redeposition dur-
ing storms.

The composition of the molluscan fauna remained
generally the same throughout the deposition of the
Pittsburg Bluff Formation. Mixtures of shells and shell
debris from animals that lived at different depths occur
throughout the section.

The Pittsburg Bluff Formation is a transgressive unit
that prograded westward over the deeper water Keasey
Formation. Its thickness of 100 m or more from the base
to the ﬁrst coal bed may give a rough measure of the
greatest water depth during its deposition. The sed-
iments in the lower part of the formation and much of
the sediments in the upper part are believed to have
been carried to their present position by grain ﬂowage
(Stauffer, 1967) on a seaward-building slope at the
margin of a basin. Sediment continuously spilled over
the shelf edge and was then moved periodically into
deeper water by grain ﬂowage. This mechanism was
responsible for the mixing of faunas characteristic of
different depths. It also, by juxtaposing species of dif-
ferent facies at a time of fairly rapid speciation and
extinction, contributed to the sharp faunal contrast
between the Pittsburg Bluff Formation and the un-
derlying Keasey Formation.

Evidence regarding the temperature at which the
Pittsburg Bluff fauna lived is somewhat contradictory.
Modern Truncacila prefers a cool-temperate habitat.
Most species of Crenella live in cool water, and
Lucinoma prefers cool water. Panopea is usually found
in areas of temperate climate, although it ranges into
warm temperate waters. Yoldia (Kalayoldia) cooperi,
probably a close relative of the extinct species of Yoldia
in the Pittsburg Bluff Formation, now lives no farther

 
north than central California. The extinct Litorhadia,
which is common in the Eocene of Alabama and is there
associated with warm-water genera, probably preferred
warm water, unless it had a broad tolerance. Callista is
usually found in warm water.

Cryptonatica is commonly a boreal form and Aforia
prefers cool water. Neverita (Glossaulax) reclusiana,
probably closely related to the extinct Pittsburg Bluff
species, lives no farther north than southern California.
The extinct genera Eosiphonalia, Bruclarkia,
Molopophorus, Priscofusus, and Perse are all moder—
ately well sculptured, a fact indicating that they may
have preferred warm water, and all these extinct genera
except Eosiphonalia and Bruclarkia occur in the Eocene
of California, a further indication of possible preference
for warm water. Architectonica, a tropical genus, is
found in the upper part of the Pittsburg Bluff sections
near coal beds, perhaps indicating shallower and,
therefore, warmer water.

Some species, such as Acila (Truncacila) shumardi
and Callista (M acrocallista) pittsburgensis, ranged from
the Alaska Peninsula to California in middle Oligocene
time. This wide geographic range may result from any
one of three causes: these species may have been able to
tolerate unusually wide temperature ranges; the
favorable temperature may have been produced by
differences in local water depth or by upwelling; or the
surface temperature of the sea may have been more
uniform in Oligocene time than it is today.

In summary, the fauna is neither tropical nor boreal
in overall aspect; it seems to indicate a warm-temperate
sea.

Tropical and subtropical molluscan genera lived only
at low latitudes during the Oligocene and at higher
latitudes during the Miocene, after which they steadily
retreated southward. Addicott (1969, 1970a) has infer-
red from these facts that there was a marked cooling in
middle Oligocene time, but the Pittsburg Bluff fauna
does not seem to support this view.

RELATION TO OTHER OLIGOCENE FAUNAS IN OREGON

Only a few species are common to both the Keasey and
Pittsburg Bluff Formations in the Vernonia area. In the
past this was explained by assuming that the two
formations were separated by an unconformity or
disconformity, marking a time interval sufﬁciently long
to account for the faunal change; but if the two for-
mations are conformable, as indicated by the present
study, this explanation is no longer valid. The species
common to both formations are:

Gastropods Pelecypods
Sinum aff. S. obliquum Crenella porterensis
(Gabb) Weaver
Scaphander stewarti Nemocardium
Durham lorenzanum (Arnold)

20 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

A few more genera are common to the two formations
but are represented by different species. They are:

Gastropods Pelecypods
C ryptonatica N uc ula
Polinices Acila
B ruclarkia Yoldia
Spirotropis Thracia
Pitar

Most of the molluscan genera do not occur in both
formations. Genera that occur only in the Keasey or
only in the Pittsburg Bluff Formation are:

Keasey Formation Pittsburg Bluff Formation

Gastropods Gastropods
Turcicula Architectonica
Epitonium (2 species) Opalia
Echinophoria Crepidula
Gyrineum Neverita
Olequahia Eosiphonalia
Mitra Molopophorus
Cancellaria (3 species) Priscofusus
Conus (2 species) Perse
Exilia Aforia
"Gemmula” Taranis
Nekewis (2 species) Suavodrillia

Pelecypods Odostomta

Acteon
$052,232? Pelecypods
Tindaria? Litorhadia
Porterius Mytilus
Delectopecten Cyclocardia
Lima Lucinoma
Cardiomya Felaniella
Thyasira Callista
Macoma Spisula

Ervilia?

Tellina

Solen

Solena

Panopea

Cochlodesma

Although none of the Pittsburg Bluff genera in these
lists, except for the turrids, now usually live in mod-
erately deep water at depths below 50 In, several Keasey
genera do; among these are Turcicula, Phanerolepida,
Solemya, Delectopecten, and Thyasira. The entire
Keasey fauna suggests depths greater than 50 m, as the
average modern bathymetric range of the Holocene
genera represented is about 40—130 m.

The fauna of the middle Keasey, which is especially

well preserved, includes many forms that have seldom‘

 
been found fossilized in other Tertiary sections (Zullo
and others, 1964, p. 333). The echinoid Salenia is
represented at one locality by several hundred
specimens, many of which have their spines still intact.
At the same locality, the crinoid Isocrinus is found with
the arms attached to the calyx. The following taxa are
reported from the upper middle Keasey Formation at
Mist, Oreg. (Zullo and others, 1964, p. 334—335):

Taxa Abundance
Foraminifera
Operculina sp __________________ Rare
Plectofrondicularia packardi
Cushman and Schenck ,,,,,,,, Abundant

Coelenterata
Caryophyllia sp. indet ,,,,,,,,,,
F labellum hertleini Durham

One specimen
Thirty-two specimens
in a block with
a surface area
of 520 cm 2,
One specimen

Gorgonid coral __________________
Pelecypoda
Acila (Truncacila)
nehalemensis Hanna __________
Delectopecten sp ________________
Ennucula sp.
Minormalletia sp.
N uculana aff. N. washingtonensis
(Weaver)
Propeamussium n. sp.
Solemya (Acharax)
willapaensis Weaver __________
Tellina sp.
Yoldia (Portlandella)
chehalisensis (Arnold)
Gastropoda
”Cancellaria” sp.
Epitonium keaseyensis Durham __
Exilia lincolnensis Weaver
Fulgurofusus n. sp.
Polinices n. sp.
Scaphander stewarti Durham
Arthropoda
Fragmentary crustacean remains__
Crinoidea
Isocrinus nehalemensis
Moore and Vokes
Isocrinus oregonensis
Moore and Vokes
Asteroidea
Brisingid? n. sp ________________
Astropecten? n. sp ______________
Unidentiﬁed asteroids __________
Ophiuroidea
Unidentiﬁed ophiuran __________
Echinoidea
Brisaster maximus Clark?
Salenia schencki Kaar ,,,,,,,,,,
Vertebrata
Fish scales
Plantae
Coralline algae ________________
'“Zostera” sp. (with attached
diatoms) ,,,,,,,,,,,,,,,,,,,,,,

Several
Several

Few

One specimen

Few

Several

Common

One specimen
Three specimens
Two specimens

One specimen

One specimen
Several hundred

____________________ Common

One fragment

Few

PITTSBURG BLUFF FORMATION 21

Taxa—Continued A bundance—Continued
Plantae—Continued

Quercus consimilis Newberry

Myrica sp.
Thuja sp ______________________ Few
Ocotea eocernua Chaney and
Sanborn ______________________ One specimen

This biota represents a mixed depth assemblage. It
includes, for example, the eelgrass Zostera, which lives
at depths of less than 15 m, and the coral Flabellum and
the echinoid Salenia, which both suggest a depth of
about 360 m (Zullo and others, 1964, p. 335). The intact
skeletons of the echinoids, seastars, and crinoids further
suggest that these animals lived at a depth of more than
150 m, undisturbed by waves and currents. The gas-
tropod Phanerolepida has been found in the middle
member of the Keasey Formation; it lives today at
depths of 600—800 In (Hickman, 1972). Moore and Vokes
(1953, p. 140) inferred, from the abundance of tuff in the
middle and upper members of the Keasey Formation,
which also contains lapilli at least 1 cm in diameter,
that the source of the volcanic debris was nearby. Since
no evidence of submarine volcanic activity was seen to
account for the ash, Moore and Vokes (1953, p. 118)
believed that the Keasey shoreline was only a few miles
away.

About 4 km north of Mist, Oreg., fossiliferous con-
glomerate and massive sandstone are exposed. Warren,
Grivetti, and Norbisrath (1945) assigned them to the
Gries Ranch Formation of early Oligocene age. They
believed that this part of the Gries Ranch Formation
might be equivalent to the upper part of the Keasey
Formation at Vernonia and that part of the Keasey
contains species found in the type Gries Ranch fauna.
Warren and Norbisrath (1946, p. 228) believed that the
faunal differences between the two might be ascribed to
different ecologic conditions. The Gries Ranch at this
Oregon locality contains the following genera that do
not occur in either the Keasey or Pittsburg Bluff
Formations:

Gastropods Pelecypods
Puncturella Glycymeris
Alvania Arca
Barbatia
Loxocardium

As species of all these genera now live in intertidal
environments, some of them on or under loose frag-
ments of rock, it seems likely that at least the upper part
of the Gries Ranch Formation was deposited within a
few kilometres of the shoreline. Absence of the genera in
the Keasey may be due to an uncongenial depth of
water.

 
The upper part of the Keasey Formation contains the
deepwater genus Turcicula. Theupper part does not
contain the generally deep-water genera Solemya,
Propeamussium, Delectopecten, Thyasira, and Spiro-
tropis. This fact may indicate a slight shoaling of the sea
in late Keasey time.

One fossil collection (USGS M3874) from a siltstone of
Keasey-like lithology taken near the base of the
Pittsburg Bluff Formation contains Nemocardium
lorenzanum. This species also occurs in the upper
Keasey. In the type locality of the Pittsburg Bluff
Formation, however, sandstone only a few metres above
the base yields a typical Pittsburg Bluff fauna. The
distribution of N . lorenzanum at this place is believed to
have been ecologically controlled; it could live in the
facies represented by the siltstone but not in the
sandstone facies.

Acila (Truncacila) nehalemensis was collected in the
Keasey Formation about 2 m below its top (USGS
M3864). Acila (Truncacila) shumardi is common
throughout the lower part of the Pittsburg Bluff
Formation in the type area. These two very distinct
species of Acila occur only a few metres apart, the one in
the Keasey and the other in the Pittsburg Bluff. They
are, however, in different kinds of rock, A. (T.)
nehalemensis in shale and A. (T.) shumardi in
sandstone. In the Gries Ranch Formation in north-
western Oregon, the Pittsburg Bluff species A. (T.)
shumardi is found rather than the Keasey species A.
(T.) nehalemensis, but as the Gries Ranch Formation
was deposited in much shallower water than the
Keasey, this difference can be attributed to a difference
of environment.

In the Eugene area, about 200 km south of Pittsburg,
Oreg., the Eugene Formation, of early and middle
Oligocene age, contains both Keasey and Pittsburg
Bluff species. Although some typical Pittsburg Bluff
species, such as Callista pittsburgensis, Acila shumardi,
and Bruclarkia columbiana, do not appear until high in
the section, other Pittsburg Bluff species, such as Tel-
lina pittsburgensis, Solena eugenensis, Thracia con-
doni, Litorhadia washingtonensis, Tellina aduncanasa,
Polinices washingtonensis, andNeverita thomsonae, are
present lower in the section, and are all associated with
typical Keasey forms (Hickman, 1969, p. 11). The
Eugene Formation, which interﬁngers with terrestrial
deposits, consists entirely of coarse- to ﬁne—grained
sandstone, whereas sediments of presumably the same
stratigraphic interval are represented in northwestern
Oregon by ﬁne-grained sandstone and siltstone of the
Pittsburg Bluff Formation and shale of the Keasey
Formation. These differences of lithology indicate that
the two areas offered somewhat different ecologic
habitats.

22 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

High in the Eugene Formation, where typical
Pittsburg Bluff species are common, the following gen—
era were found that do not occur in the Pittsburg Bluff
Formation:

Gastropods Pelecypods

Epitonium Modiolus

Acrilla Parvicardium

Calyptraea Pse udocardium

Ficus Macoma

Oleq uahia Semele

Exilia M ya

Gemmula Pandora

Cylichnina Opertochasma
M artesia

Most of these mollusks from the Eugene Formation
could have lived within the environmental range of the
Pittsburg Bluff Formation, both as to depth and sea-
surface temperature. The following genera occur in the
Keasey but not in the Eugene Formation:

Gastropods Pelecypods
Turritella Solemya
Echinophoria E nn ucula
Gyrineum M inormalletia
M itra Tindaria?
Cancellaria Porterius
Spirotropis Delectopecten
N ekewis Lima
K nefastia Cardiomya
Thyasira

As the mean depth at which many of these genera now
live (40—100 m or more) is greater than the mean in-
dicated by the inner neritic Eugene fauna as a whole,
some of the Keasey Formation may have been deposited
in deeper water than any part of the Eugene Formation.
Crinoids are not found in the Eugene Formation,
reinforcing the conclusion that the habitat was different
from that of the Keasey and that it differed in some
respect other than sea-surface temperature, since the
two geographic areas are only about 200 km apart.

The known distribution of genera in the lower, mid-
dle, and upper Keasey is shown in table 3 along with
genera that also occur in the Eugene and Pittsburg
Bluff Formations.

In the Coos Bay area, about 260 km southwest of
Pittsburg, Oreg, the middle Oligocene Tunnel Point
Sandstone rests conformably upon the Bastendorff
Shale (late Eocene and early Oligocene). The molluscan
fauna of the Tunnel Point is reported to contain typical
Pittsburg Bluff species and no Keasey species. Genera
found by Weaver (1945, p. 51) in the Tunnel Point but
not in the Pittsburg Bluff are:

 
Gastropods
Exilia
N eptunea

Pelecypods

Corbis

M acoma
Pachydesma
Pecten
Pholas
Thyasira

The underlying Bastendorff Shale contains no Tunnel
Point species. Its meager molluscan fauna includes
Acila aff. A. decisa (Conrad),Nuculana cf. N. merriama
(Dickerson), Spisula cf. S. packardi Dickerson,
Cylichnina turneri Efﬁnger, and Dentalium cf. D.
porterensis Weaver. Of the 16 foraminifers reported by
Weaver (1945, p. 49) in the Bastendorff, 7 occur in the
Keasey. The foraminifers in the upper 300 m of the
Bastendorff Shale indicate moderately deep to abyssal
water depths (Kleinpell, 1938, p. 102). So even though
Coos Bay is much farther south and nearer to the pre-
sent coast, the depositional-faunal sequence is analog-
ous to that of the Keasey and Pittsburg Bluff Forma-
tions in northwestern Oregon.

TABLE 3.—Distribution of molluscan genera in the lower, middle, and
upper parts of the Keasey Formation and their occurrence in the
Pittsburg Bluff and Eugene Formations

[Compiled from Moore and Vokes, 1953, and Hickman, 1969]

 
Keasey Formation

Genera PitBtsburg

Eugene

Lower Middle Upper Formation

part part part

Form ation

 
Pelecypods:

Solemya ________________ ><
Ennucula ____________________
Acila (Truncacila) ,,,,,,,, X
N uculana
Yoldia ______________________
M inormalletia
Porterius ____________________
Propeamussium ______________
Delectopecten ________________
Lima ________________________ _
Crenella ____________________ ><

Thracia ____________________ ><

Thyasira ________________ X X "1, ____ ____
Nemocardium ><
Fimbria ________________ >< __,v ____ ____ 11--
Pitar ____________________ >< __ __ u i _ x x
Tellina _______________________ X , __ _ X X

Gastropods:
Turcicula ________________ >< __ _ X ",1 __,,
E pitoni um __________________
Polinices ____________________
Turritella _____________________
Echinophoria ________________
Gyrineum
Oleq uahia __________________
B ruclarkia __________________
Cancellaria __________________
Conus __________________ ><

Exilia ______________________
F ulgurof us as ________________
"Gemmula” __________________
N ekewis ____________________
Scaphander __________________

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PITTSBURG BLUFF FORMATION

In northwestern Oregon the Keasey Formation,
represented by shale, and the Pittsburg Bluff For-
mation, represented by sandstone, are comformable but
have almost no species in common; in southwestern
Oregon, the Bastendorff Shale and the Tunnel Point
Sandstone are conformable and contain no species in
common. In both areas, depth of water is believed to be
the controlling factor explaining the abrupt faunal
break between early and middle Oligocene formations.

In the Newport area, on the coast of Oregon north of
Coos Bay, the Alsea Formation, considered early,
middle, and late Oligocene by Snavely, MacLeod, Rau,
Addicott, Pearl, and Quinterno (1975), is conformably
overlain by the Yaquina Formation (late Oligocene and
early Miocene) and unconformably underlain by the
Nestucca Formation (late Eocene). The Alsea Forma-
tion has yielded 35 species of mollusks (Vokes and
others, 1949); and 13 of these also occur in the Pittsburg
Bluff Formation. The upper part of the Alsea Formation
contains mollusks of provincial late Oligocene age
(Warren 0. Addicott, written commun., 1973).

The following genera are represented in the Alsea
Formation but not in the Pittsburg Bluff Formation:

Gastropods Pelecypods
Calyptraea Lucina (Here)
Liracassis Loxocardi um?
Exilia M acoma
Ancilla Apolymetis

There are no obvious differences in ecologic re-
quirements between these genera and those in the
Pittsburg Bluff Formation.

Two small, poorly preserved molluscan faunas were
collected in the Newport area, one of which has been
correlated with a fauna from the Gries Ranch For-
mation, the other with a fauna from the Keasey For-
mation (Vokes and others, 1949). Further investigation
may show that there was a close ecologic relation
between the Newport area and the Pittsburg area dur-
ing early and middle Oligocene time.

SUMMARY

Many of the genera found in the Keasey Formation
are not found in the Pittsburg Fluff Formation. This
curious fact can perhaps be explained as a result of
differing habitats; the extinction of genera is not in-
volved as most of these genera are still living today. The
Keasey fauna lived predominantly in moderately deep
water, at depths greater than 50 m, on a bottom of silt,
whereas the Pittsburg Bluff fauna lived predominantly
in water shallower than 50 m, on a bottom of ﬁne sand. A
similar ecologic difference existed near Coos Bay during
the deposition of the Bastendorff and Tunnel Point

 
23

Formations, equivalent to the Keasey and the Pittsburg
Bluff Formations, respectively. The Gries Ranch
Formation, a shallow-water equivalent of the upper
part of the Keasey Formation, contains 10 Pittsburg
Bluff species, a strong indication that ecology is the
limiting factor.

The Eugene Formation may have been deposited in
an environment in which the elements of the Keasey
fauna that could tolerate shallower water, of 50 m or
less, could live.

AGE

The ﬁrst Paciﬁc coast fossils to be assigned to the
Oligocene were the mollusks collected by Diller near
Pittsburg, Greg, and later identiﬁed by Dall (Diller,
1896, p. 466). Presumably Dall’s assignment was based
on a comparison of the genera with those of the
Oligocene of Europe and on the percentage of living
taxa. Dall’s ﬁrst assignment of the Pittsburg Bluff
fauna to the Oligocene has been endorsed by most other
molluscan specialists, on the basis of comparison at the
generic level of its mollusks with those from the
Oligocene of the Gulf Coast and of Europe, of super-
position, and of the marked change in the molluscan
fauna at the end of the Eocene, when many genera
disappeared and others made their ﬁrst appearance.

In 1936 Schenck and Kleinpell proposed the Refugian
Stage for part of the Paciﬁc coast Tertiary. They de-
signated as the type locality for this stage Canada de
Santa Anita, on the south side of the Santa Ynez
Mountains, Santa Barbara County, Calif:, about 5 miles
west of Gaviota Pass. Schenck and Kleinpell (1936, p.
219) stated that “***the Refugian stage comprises the
rocks deposited after the strata usually included within
the Tejon Formation (restricted) were laid down and
before the Zemorrian Stage.” They believed that the
Refugian Stage is “probably equivalent in age to a
portion of the upper Eocene or lower Oligocene series of
Europe.” They considered it to be represented in Oregon
by the Eugene, Pittsburg Bluff, Tunnel Point, Keasey,
and Bastendorff Formations, in Washington, by the
Lincoln [Lincoln Creek] and Gries Ranch Formations.
They also. believed that the Refugian Stage included the
Acila sh umardi Zone and was roughly equivalent, in its
type area, to the Turritella variata Zone.

According to Schenck and Kleinpell, the Keasey
species Acila (Truncacila) nehalemensis Hanna ﬁrst
appears in the basal part of the Refugian Stage (1936, p.
220—221). The Pittsburg Bluff species Acila (Truncaci-
la) shumardi (Dall), Callista pittsburgensis Dall,
Molopophorus gabbi Dall, and Bruclarkia columbiana
(Anderson and Martin) make their last appearance in
the uppermost part of the Refugian Stage (Schenck and
Kleinpell, 1936, p. 221).

Addicott (1972), in a paper on the provincial mollus-

24

can stages of the Temblor Range in California, discusses
the Refugian Stage (p. 5), calls it early Oligocene (p. 4,
ﬁg. 3), and states that the Refugian and Zemorrian
Stages in this area are at least in part coeval. He bases
this conclusion on the occurrence of the Refugian index
species Bruclarkia columbiana in strata that can read-
ily be traced to the lowermost part of the type Zemorrian
Stage of Kleinpell (1938).

In 1963 Weaver and Kleinpell published an exhaus-
tive study of foraminiferal and molluscan faunas from
the Gaviota and Alegria Formations in the Santa
Barbara embayment of California, which contains the
type area of the Refugian Stage. One of the most
noteworthy provincial correlations made by Weaver
and Kleinpell on the basis of foraminifers and mollusks
was that of the Bastendorff and Keasey Formations
with the middle and upper members of the Gaviota
Formation and an implied correlation of the lower 200
feet of the Alegria Formation (the uppermost part of the
"Turritella variata Zone”) with the Lincoln Creek
Formation of Washington and its equivalents, which
would include the Pittsburg Bluff Formation (Weaver
and Kleinpell, 1963, p. 45).

Weaver and Kleinpell believe that several West
Coast formations usually considered to be of early or
middle Oligocene age, are on the basis of mollusks, in
whole or in part of the same age as the Turritella variata
lorenzana Zone of Santa Barbara. These formations are
the middle and upper parts of the Bastendorff, the
Tunnel Point, the Keasey, the Pittsburg Bluff, the Gries
Ranch, and the Lincoln Creek Formations (Weaver and
Kleinpell, 1963, p. 113—114). Although they found few
molluscan species that are common to the Paciﬁc
Northwest and the Santa Ynez Mountains of California,
they felt that these few are exceptional in their ap—
parent stratigraphic ﬁdelity. The occurrence of Acila
nehalemensis in the upper Gaviota beds of the Santa
Ynez Range makes it possible to correlate these beds
with the middle and upper Bastendorff and the Keasey
Shale. The Lincoln Creek Formation can be correlated
with the lower part of the Alegria Formation—the
Turritella variata-bearing members A to .C. They
conclude that the Turritella variata Zone, since it
contains 1—2 percent of living species and some giant
venericards, is late Eocene and perhaps early
Oligocene, and that the Refugian Stage is therefore late
Eocene and perhaps very early Oligocene (Weaver and
Kleinpell, 1963, p. 118).

Schenck and Kleinpell (1936) deﬁned the Refugian
Stage on the basis of its carefully delineated type sec-
tion, and although they used local ﬁrst and last ap-
pearances of both benthonic foraminifers and mollusks
to mark the boundaries, they then did not intend strati-
graphic range extensions to change the deﬁnition of the

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

stage (p. 221). Although other stages have been deﬁned
on the basis of provincial fossil zones, the Refugian was
originally intended to be of ﬁxed geologic age—the age
of its type section. In recent years the Refugian has
taken on more the character of a stage based exclusively
on foraminiferal zones. This reduces its usefulness in
molluscan paleontology because the provincialism of
both benthonic foraminifers and mollusks is measura-
bly signiﬁcant over the distance from the type locality of
the Refugian to, for example, the type locality of the
Pittsburg Bluff Formation. Whereas in original concept
the Refugian Stage might have had lasting utility in
broad-scale West Coast stratigraphy, at this time it
seems difﬁcult, if not impossible, to use it judiciously.

The type locality for Acila (Truncacila) shumardi of
the Acila shumardi Zone of Schenck (1936) is at the type
locality of the Pittsburg Bluff Formation, and the Acila
shumardi Zone has been recognized since 1936 in all the
Paciﬁc coast states, including Alaska, and has always
been assigned to the Oligocene.

Durham (1944) proposed magafaunal zones for the
Tertiary of southwestern Washington; one of these was
the M olopophorus gabbi Zone. M. gabbi is a common and
characteristic species of the Pittsburg Bluff Formation.
Presumably because M. gabbi is not as widespread
geographically in its occurrence as Acila shumardi, the
Molopophorus gabbi Zone is not as widely used as the
Acila shumardi Zone. The Molopophorus gabbi Zone is,
however, roughly equivalent to at least the lower part of
the Acila shumardi Zone.

Durham listed as characteristic of the Molopophorus
gabbi Zone the species Bruclarkia columbiana,
Molopophorus dalli, Perse olympicensis quimpersensis,
P. pittsburgensis, and Spisula pittsburgensis; all but
Perse olympicensis and Molopophorus dalli occur in the
Pittsburg Bluff Formation. Molopophorus dalli, which
Durham includes in the Molopophorus gabbi Zone, does
not occur at the same horizon as M. gabbi in northwest-
ern Oregon; it seems to be an older species, restricted to
the early Oligocene.

The position of the provincial Oligocene-Miocene
boundary has been in dispute for many years (Moore,
1963, p. 1‘2), and complete agreement still has not been
reached. The problems concerning the Eocene-
Oligocene boundary seemed to be nearing solution, with
generally good agreement, until fairly recent years. In
the most extreme example of these recent problems,
Eames, Banner, Blow, Clarke, and Cox (1962) published
a paper on mid—Tertiary correlation in which they de-
nied that there is Oligocene at all on the western coast of
North America.

David Bukry (written commun., 1973) considers a
sample from USGS locality M3865, about 100 m below
the top of the Keasey Formation, to be late Eocene or

PITTSBURG BLUFF FORMATION

earliest Oligocene in age on the basis of the following
coccoliths that he was able to identify.
USGS locality M3865. Railroad cut adjacent to
State Highway 47, 0.5 km south of main street of
Vernonia, Oreg., at 45°51.3’ N., 123°11.8’ W.
Braarudosphaera bigelowii (Gran and Braarud)
Chiasmolithus oamaruensis (Deﬂandre)
Coccolithus eopelagicus (Bramlette and Riedel)
Coccolithus pelagicus (Wallich)
Cyclicargolithus sp., cf. C. ﬂoridanus (Roth and
Hay)
Dictyococcites bisectus (Hay, Mohler, and Wade)
Dictyococcites scrippsae Bukry and Percival
Isthmolithus recurvus Deﬂandre
Many authors have cited the difﬁculties of provincial
correlation in the Oligocene. Whereas the Eocene
permits fairly easy correlations over wide areas, and the
Miocene permits reasonable correlations, the Oligocene
has always been troublesome in this respect. The usual
explanations for the difﬁculty with the Oligocene have
been (1) that the basins of deposition were isolated and
(2) that distinctive Caribbean elements in the Eocene
faunas migrated southward in Oligocene time. The
problem of precise correlation is further complicated by
the fact that since the most useful planktonic species of
foraminifers and coccoliths do not commonly occur with
the nearshore molluscan faunas either on the Paciﬁc
coast or at the European stratotype localities, detailed
studies of interﬁngering of facies are required in both
regions. And, the original series and stages in Europe
were not as carefully deﬁned as might have been desired
(Fischer and others, 1971). However, the age deter-
mination by David Bukry given above, based on coc-
coliths from the middle Keasey as deﬁned by Moore and
Vokes (1953, p. 1 15, ﬁg. 28), provides new evidence from
this cosmopolitan planktonic fossil group for a late
Eocene and early Oligocene age for the Keasey For—
mation and its correlatives. On the basis of superposi-
tion and its contained fauna, the overlying Pittsburg
Bluff Formation is assigned to the middle Oligocene.
The sum of all paleontologic and stratigraphic evidence
now available indicates that the Pittsburg Bluff
Formation is of provincial middle Oligocene age.

CORRELATION

The marine lower and middle Oligocene sedimentary
rocks of the Paciﬁc Northwest range in facies from
conglomerate (Gries Ranch Formation) through
sandstone (Eugene Formation) and ﬁne-grained
sandstone and siltstone (Pittsburg Bluff Formation) to
deepwater shale (Keasey Formation). In some areas,
such as those around Newport and Eugene, Oreg.,
depositional conditions during the Oligocene were
apparently fairly constant. In other areas, such as those

 
25

around Pittsburg and Coos Bay, Oreg., an abrupt
change took place at the end of the early Oligocene from
relatively deepwater to relatively shallow-water dep—
osition as evidenced by both the character of the
sedimentation and the fauna.

In the Paciﬁc Northwest, a heavy cover of vegetation,
discontinuous exposures, interruption by faults, and the
recurrence of similar sediments at various horizons
throughout the Tertiary make even local correlation
difﬁcult and make regional correlation impossible in
unfossiliferous rocks. The Pittsburg Bluff molluscan
fauna, however, although small in number of species, is
distinctive and it includes some species of short time
range that occur as far north as Alaska and as far south
as southern California. It therefore permits consider-
able conﬁdence in provincial correlation.

The distribution of Pittsburg Bluff species in some
other formations of late Eocene, Oligocene, and early
Miocene age and Pittsburg Bluff species not known to
occur outside the Pittsburg Bluff Formation is given in
table 4. A total of 48 species of mollusks has been
identiﬁed in the Pittsburg Bluff; 9 of these are not now
known to occur elsewhere. The number of species that
occur in other formations with which the Pittsburg
Bluff Formation has been precisely or approximately
correlated, listed in north to south order, is as follows:

Number of
Formation species
m Common

Stepovak Formation of Burk (1965) ______ 3
Poul Creek Formation __________________ 9
Quimper Sandstone of Durham (1942) _-_- 9
Gries Ranch Formation __________________ 10
Lincoln Creek Formation ________________ 14
Alsea Formation ________________________ 13
Eugene Formation ______________________ 17
Tunnel Point Sandstone ________________ 11
San Lorenzo Formation __________________ 3
Wygal Sandstone Member of

Temblor Formation __________________ 3
Cymric Shale Member of

Temblor Formation __________________ 1
Kirker Tuff _____________________________ 2
Tumey Formation of Atwill (1935) ______ 3
San Emigdio Formation ________________ 2
Alegria Formation of Dibblee (1950) ______ 1

Of the total number of Pittsburg Bluff species, 28
species, or 58 percent, are known to occur in other
formations of middle Oligocene age; 12 species, or 25
percent, occur in early Oligocene formations; and 10
species, or 22 percent, occur in formations assigned to
the late Oligocene or early Miocene. Only two species
are found in late Eocene formations.

The correlation chart (ﬁg. 7) indicates graphically the

OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

26

 
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28

formations believed to be correlative entirely or in part
with the Pittsburg Bluff Formation. Pittsburg Bluff
molluscan species are most abundant in the Tunnel
Point Sandstone at Coos Bay, the upper part of the
Eugene Formation in the Willamette Valley, and the
Alsea Formation near Newport, Oreg. Other probable
time-stratigraphic equivalents of the Pittsburg Bluff
Formation on the basis of mutual occurrence of species
are: parts of the Stepovak Formation of Burke (1965)
and Poul Creek Formation in Alaska, the Lincoln Creek
Formation and Quimper Sandstone of Durham (1942) of
Washington, and the Wheatland Formation of Clark
and Anderson (1938), Tumey Formation of Atwill
(1935), San Emigdio Formation, Wygal Sandstone and
Cymric Shale Members of the Temblor Formation,
Alegria Formation of Dibblee (1950), and Kirker and
San Lorenzo Formations of California.

A mixture of Keasey and Pittsburg Bluff species oc-
curs throughout the Eugene Formation, as pointed out
in the section on ecology; some typical Pittsburg Bluff
species such as Callista pittsburgensis, Acila shumardi,
and Bruclarkia columbianum occur only in its upper
part. Table 5 gives all the Oligocene species that were
found high in the Eugene Formation by Hickman (1969,
p. 16—19).

TABLE 5.——Checklist of Oligocene mollusks in the upper part of the

Eugene Formation in Oregon
[Locality numbers and occurrence are from Hickman (1969)]

 
Eugene area Salem area
Locality No.
12 28 34 35 39 41 42 44 46 47
Pelecypods
Acila (Truncacila) nehalemensis (G.
D. Hanna) ____________________________ W W W W X W
Acila (Truncacila) nehalemensis
minima Hickman ______________ X X W W W W W W W 1
Acila(Truncacila)shumardi(Dall) W W W X X X X X W ,
Nuculana washingtonensis
(Weaver) ______________________ X X W W W W X X W W
Yoldia (Kalayoldia) oregona
(Shumard) ______________________ >< __ W W X X W W W
Modiolus eugenensis Clark ________ X X W W W W W W W W
Mytilus snohomishensis Weaver W W W W W W W X W W W
Parvicardium eugenense (Clark) W X X X X X __ X W X W
Lucinoma acutilineata (Conrad) W W W W W W X W W W W
Diplodontaparilis (Conrad) ______ X X W X W X x __ X X
Callista pittsburgensis(Dall) ,,,,,, X W X X W W X W X W
Callista n. sp _____________________ X X W X W W W W W W
Pitar (Pitar) dalli (Weaver) ______ X X X X X W X W X W
Pitar (Pitar) n. sp.? ,,,,,,,,,,,,,, X X W W W W W W W W
Pitar (Lamelliconcha) clarki
(Dickerson) ____________________ X X W W W W W W X W
Spisulapittsburgensis Clark WWW W W W W W W X X W W
Spisula eugenensis (Clark) ,,,,,,,, X X X X W W W W W W
Pseudocardium sp. ________________ X X W W W W W W X
Tellina pittsburgensis Clark ______ X X W W W W W X X W
Tellina aduncanasa Hickman ______ X W W W W X X W W

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

TABLE 5.—Checklist of Oligocene mollusks in the upper part of the
Eugene Formation in Oregon—Continued

 
Eugene area Salem area
Locality No.
12 28 34 35 39 41 42 44 46 47
Pelecypods—Continued
Tellina? n. sp. __________________ X X W W W W W W W W
Tellina eugenia Dall ,,,,,,,,,,,,,, W W W X W W W W W W
Tellina (Moerella) lincolnensis
(Weaver) ______________________ X X W X W W W W W W
Macoma aff. M. inquinata (De-
shayes) ________________________ X X W W W W W W X __
Macoma (Heteromacoma) van-
couverensis (Clark and Anderson) X X W W W W W W W W
Semele willamettensis Hickman W W X W W W W W W W W
Selena (Eosolen)eugenensis (Clark) X X X X __ W X X x X
Solen sicarius Gould 111111111111 X X W X W W X W W W
Mya (Arenomya?) kusiroensis
(Nagao and Inoue) ______________ X W W W W W W W W
Panopea (Panopea) ramonensis
Clark __________________________ X __ __ W W W W W W
Oper'tochasma turnerae (Hickman) W X W W W W W W W W
Martesia Sp. ______________________ >< __ W W W __ W W W
Pandora (Pandora) laevis Hickman X W W W W W W W W W
Thracia condoniDall ____________ X X W X W X W W X W
Scaphopod
Dentalium (Fissidentalium?)
laneensis Hickman ____________ X X W W W W W W W W
Gastropods
Epitonium (Boreoscala) condoni
(Dall) ________________________ X X X X W W W W W W
E. (B.)condonioregonensis Durham W W W X W W W W W W
E. (B.)condonieugenense Durham W X X X W W W W W W
Acrilla (Ferminoscala) dickersoni
Durham ,,,,,,,,,,,,,,,,,,,,,, X X W W W W W W W X
A. (F.)becki Durham ____________ ? X __ W __ W W W W W
Calyptraea diegoana (Conrad) WW X X W W W W W W W W
Calyptraea sookensis Clark and
Arnold ________________________ W W W W W W W W __ ><
Crepidula ungana Dall ,,,,,,,,,, X X W W W W W W W W
Natica(Natica)n.sp.? ____________ W X W X W W X W W W
Neverita thomsonae Hickman WW X X W W W W X W X X
Polinices washingtonensis (Weaver) X X W W W W W W W W
Sinum obliauum (Gabb) __________ X X W W W W W W W W
Ficus modestaiConrad) __________ X X W W W W W W W W
Olequahia schencki Durham ________ X W W X X W W W W
Molopophorus dalli Anderson and
Martin ________________________________ W W W W W X
Molopophorus ﬁshii (Gabb) 11111111 X X X W W W W W W
Bruclarkia vokesi Hickman ______ X X X X X W W W W W
Bruclarkia columbiana (Anderson
and Martin) __________________ X X W W W W W W X X
Perse lincolnensis (Van Winkle) W W X W __ W __ __ W W W
Exilia lincolnensis (Weaver) ______ X X __ __ W W W __ W W
Gemmula bentsonae Durham ______ X X W W W W W W W W
Acteon parvuum Dickerson ,,,,,, x W W __ __ __ __ W W W
Cylichnina turneri Efﬁnger ________ X W W W W W W W W
Scaphander stewarti Durham ______ X W X X W X W W W

 
The presence of such typical Keasey species as Acila
(Truncacila) nehalemensis and Olequahia schencki high
in the Eugene Formation, combined with the absence of

SYSTEMATIC DESCRIPTIONS

any typical Keasey species in the Pittsburg Bluff

Formation, might permit considering the hypothesis
that all of the Eugene Formation is slightly older than
the Pittsburg Bluff Formation. Since the uppermost
part of the Eugene Formation and the lower part of the
Pittsburg Bluff Formation contain 19 species in
common, they are regarded as partly coeval.

SYSTEMATIC DESCRIPTIONS
Phylum MOLLUSCA
Class GASTROPODA
Family TROCHIDAE
Unidentiﬁed trochid?
Plate 1, ﬁgures 6, 7
This single specimen resembles the trochid
Bathybembix in overall outline (USNM 213948). Some
characteristics of the specimen recall “Turcicula”
columbiana Dall (1909, p. 100, pl. 3, ﬁgs. 2, 11) that
occurs in the Keasey Formation (late Eocene and early
Oligocene) in Oregon and has been assigned to
Bathybembix by Rehder (1955, p. 255). This specimen
does not have so high a spire as Bathybembix, is a much
smaller form, and measures 24 mm in maximum
diameter. Patches of the inner shell layers are pre—
served, as are fairly large nodes on the periphery of the
last whorl. The aperture and umbilicus are not pre-
served.
Locality.—USGS 15312.
Family ARCHITECTONICIDAE
Genus Architectonica Rbding'
Architectonica Roding, 1798, Museum boltenianum, pt. 2, p. 78.
Type species—By subsequent designation (Gray,
1847, Z001. Soc. London Proc., pt. 15, p. 151) Trochus
perspectivus Linné. Holocene, tropical western Paciﬁc
Ocean.
Architectonica blanda Dall
Plate 1, ﬁgures 1-4
Architectonica blanda Dall, 1909, US. Geol. Survey Prof. Paper 59, p.

80—81, pl. 3, ﬁgs. 4, 5. Weaver, 1942, Washington Univ. (Seattle)
Pubs. Geology, v. 5, p. 364, pl. 73, ﬁg. 7.

Two incomplete specimens of Architectonica blanda
are in the collections. They are distinguished by the
smoothness of the spire and by the paired spirals on the
periphery of the body whorl. These paired spirals are of
equal weight on one specimen and of unequal weight on
the other; the more posterior spiral is narrower. Ac-
cording to Dall (1909, p. 80), A. blanda has one strong
spiral and one much weaker one. Four somewhat
unequally spaced spiral grooves are visible on the base
of the shell. Because the umbilicus and umbilical mar-
gin are worn and corroded on the specimens at hand and
are covered by matrix on the type specimen of the
species, an assignment reﬁned to subgenus has not been
made.

 
29

Holotype.—USNM 107414. Figured specimens:
USNM 213945, 213946.

Type locality.—USGS 2697, north fork of Scappoose
Creek, at the mouth of Fall Creek, Columbia County,
Oreg. Scappoose Formation (late Oligocene and early
Miocene).

A. blanda is the only post-Eocene species of Ar-
chitectonica reported from Oregon and Washington.
Although the type locality has been cited as middle
Oligocene (Weaver, 1942, p. 364), it is actually in the
Scappoose Formation of late Oligocene and early
Miocene age.

Localities.—USGS 15588, M3858.

Occurrence elsewhere—Scappoose Formation (late
Oligocene and early Miocene), Oregon.

Family TURRITELLIDAE
Genus Turritella Lamarck
Turritella Lamarck, 1799, Soc. Hist. Nat. Paris Mem., ser. 1, p. 74.

Type species.—By monotypy Turbo terebra Linné.

Holocene, tropical western Paciﬁc Ocean.

Turritella pittsburg-ensis, n. sp.
Plate 3, ﬁgures 11—16; ﬁgure 8

Turritella pittsburgensis is a small species (largest
specimen, incomplete, 32 mm high and 10 mm wide)
with a shell of moderate thickness consisting of proba-
bly 12 whorls. On the whorls of the spire, the two an-
terior spiral ribs are the most prominent, and the an-
terior space between them and the suture is deeply
concave. These paired ribs are equal in weight on the
spire, but the anterior rib becomes more prominent on
the larger whorls nearest the body whorl. Above the
paired spirals are two spirals of equal weight, and above
them are two of lesser width just below the suture.
These two ﬁnest spirals are absent on the early whorls of
the spire. On the very earliest whorls, only the paired
primary spirals and one secondary spiral are present;
these spirals strongly suggest relationship to the
bicostate Turritella uvasana stock of Merriam (1941, p.
42— 44). On one specimen (pl. 3, ﬁg. 14), a ﬁne spiral is
present between the paired anterior spirals on the
largest preserved whorl. The body whorl is not pre-
served on the available specimens. The growth-line
sinus is shown in ﬁgure 8; this deep antispiral sinus has
the maximum swelling just above the whorl middle and
no apparent growth-line angle. In this regard it re-
sembles Turritella porterensis Weaver from the Lincoln
Creek Formation (Eocene to Miocene) of Washington
and Turritella oregonensis Conrad from the Astoria
Formation (Miocene) of Oregon. Both of these species
are assigned to the Turritella uvasana stock by Merriam
(1941, p. 43).

Holotype.—Herewith designated USNM 213991,
plate 3, ﬁgure 16.

30

 
FIGURE 8.—Growth-1ine sinus on Turritella pittsburgensis, n. sp.
Drawing by Anthony D’Attilio.

Type locality.—USGS 15588. Roadcut on logging road
along the headwaters of the second main tributary
entering Coal Creek from the northeast of its junction
with Pebble Creek. 3,900 feet west of grid 820 and 5,200
feet south of grid 2,650, Vernonia quadrangle, Pittsburg
Bluff Formation (middle Oligocene), Oregon.

Turritella wheatlandensis Clark and Anderson (1938,
p. 949, pl. 3, ﬁgs. 10, 18) from the Wheatland Formation
(late Eocene or early Oligocene), California, is a much
larger species (holotype 59 mm high, incomplete, and 24
mm wide) with a heavy shell. T. wheatlandensis has
four spiral ribs on the adult whorls whereas T.
pittsburgensis has six. Although both forms have paired
anterior ribs that are strongest, the paired spirals are
stronger on T. wheatlandensis in relation to the other
spirals than on T. pittsburgensis.

Turritella oregonensis Conrad from the Astoria
Formation (Miocene), Oreg. (Moore, 1963, p. 25, pl. 1
ﬁgs. 9—12), is similar in size and shell thickness to T.
pittsburgensis. It also has prominent paired spirals
anterior to the middle of the whorl. The paired spirals
are, however, more prominent and bolder than on T.
pittsburgensis and occupy a somewhat more posterior
position. T. oregonensis has a total of no more than four
spirals, whereas T. pittsburgensis has six on the later
whorls.

Turritella porterensis Weaver from the Lincoln Creek
Formation (late Eocene to early Miocene) of
Washington does not have the two strong paired an-
terior ribs, although it does have a pair of primaries

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

with a secondary between them. It has more spiral ribs,
and the whorls are gently and almost evenly rounded.

Perhaps Turritella wheatlandensis, T. pittsburgensis,
and T. oregonensis could appropriately be assigned to
one branch of the T. uvasana stock and T. porterensis
and T. diversilineata blakeleyensis Weaver (1912, p. 72,
pl. 11, ﬁg. 85; pl. 6, ﬁgs. 64, 67) from the Blakeley
Formation of Weaver (1912) (late Oligocene or early
Miocene) in Washington, could be assigned to another
separate branch (Merriam, 1941, p. 43, ﬁg. 6).

Localities—USGS 15278, 15457, 15499, 15519,
15530, 15537, 15588, M3873.

Occurrence elsewhere—One poorly preserved speci-
men from the top of the Keasey Formation (late Eocene
and early Oligocene), near Vernonia, Oreg., may be this

species (M3864).
Family EPITONIIDAE
Genus Opalia. Adams and Adams

Opalia Adams and Adams, 1853, The genera of Recent Mollusca, v. 1,
p. 223.
Type species.—By subsequent designation (Coss-
mann, 1912, Essais de paleoconchologie comparée, v. 9,
p. 78), Scalaria australis Lamarck. Holocene, Aus—

tralia.
Subgenus Dentiscala de Boury

Dentiscala de Boury, 1886, Monographie des Scalidae Vivante et
fossiles, 1, pt. 1, p. xxi.
Type species—By monotypy, Turbo crenata Linné,
1758, Syst. Nat., p. 765. Holocene, Mediterranean and
Atlantic.

Opalia (Dentiscala?) hertleini, n. sp.
Plate 3, ﬁgures 6, 8, 20

This species is of moderate size with a fairly thick
shell. It has 12 strong, slightly arcuate axial ribs on the
last preserved whorl and about 28 spiral threads. The
axial ribs may be offset at the suture or may be
conﬂuent. No callus is present. The interspaces are
wider than the axial ribs. The spiral threads are of
unequal weight, closely spaced, and cross the axial ribs.
The spiral threads are microscopically sculptured by
axial threads that produce a ﬁnely reticulate pattern on
well-preserved portions of shell. The suture is im-
pressed, somewhat overlapping, and sinuous. The
aperture is not preserved. It has not been possible to
determine the presence or character of a basal disk.

Holotype.——Herewith designated USNM 213983,
plate 3, ﬁgure 20.

Type locality.—USGS 15588. Cut in logging road
along the headwaters of the second main tributary
entering Coal Creek from the northeast of its junction
with Pebble Creek. 3,900 feet west of grid 820 and 5,200
feet south of grid 2,650, Vernonia quadrangle, Pittsburg
Bluff Formation (middle Oligocene), Oregon.

This species most closely resembles the subgenus
Dentisca‘la in conﬁguration and primary sculpture.
However, no punctations were seen on the shell, only

CLASS GASTROPODA

small preserved patches of microscopically reticulate
sculpture. Since the outermost shell layer is known to be
porous and to decorticate readily, it may be that the
punctations are absent owing to lack of preservation of
this layer.

The only west coast fossil epitonid which this form at
all resembles is Epitonium (Boreoscala) keaseyense
Durham (1937, p. 498, pl. 57, ﬁg. 17). It is distinguished
from E. (B.) keaseyense by its lack of a callus at the
suture where the axial ribs are joined and in having
more axial ribs and many more spiral threads than E.
(B. ) keaseyense. Opalia (Dentiscala?) hertleini resembles
the living form Opalia colimana (Hertlein and Strong)
which occurs from Santa Cruz, Nayarit, to Manzanillo,
Colima, Mexico (Keen, 1971, p. 438). It differs from it in
having two to four more ribs that are smaller than those
on 0. colimana.

Living species in tropical west America are found
from southern California and the Gulf of California to
Panama (Keen, 1971, p. 438—440).

Localities.——USGS 15588, 21612, M3857.

Family CALYPTRAEIDAE
Genus Crepidula. Lamarck
Crepidula Lamarck, 1799, Soc. Hist. Nat. Paris Mém., p. 78.

Type species—By monotypy, Patella fornicata Linné.

Holocene, Atlantic and Gulf coasts of the United States.

Crepidula pileum (Gabb)
Plate 1, ﬁgures 5, 8

Crypta (Spirocrypta) pileum Gabb, 1864, Geol. Survey California,
Paleontology, V. 1, p. 137, 228, pl. 29, ﬁgs. 2, 3.

Crepidula pileum (Gabb). Stewart, 1926, Acad. Nat. Sci. Philadelphia
Proc., v. 78, p. 341—342, pl. 29, ﬁgs. 2, 3. Turner, 1938, Geol. Soc.
America Spec. Paper 10, p. 90, pl. 20, ﬁg. 6. Efﬁinger, 1938, Jour.
Paleontology, v. 12, p. 378.

Crepidula (Spirocrypta) pileum (Gabb). Clark, 1938, Geol. Soc.
America Bull., v. 49, p. 701—702, pl. 4, ﬁg. 19.

Crepidula pileum is a small species. The apex is low
and does not rise above the shell. The shell is smooth
except for bunched concentric lines. The internal deck is
attached along the margins at about the middle of the
shell With a sinuous free margin. Because part of the
internal deck is missing on the ﬁgured specimen, the
S-shaped outline of the free deck edge does not show. I
am indebted to Bruce Welton, Portland State Uni-
versity, who collected and donated the ﬁgured speci-
men. It is the only well-preserved Crepidula in the
collections; the others are poorly preserved or broken.

Lectotype.—ANSP 4221 (Stewart, 1926, pl. 29, ﬁg. 3).

Type locality.—Tejon Pass, Kern County, Calif. (Te-
jon Formation, early, middle, and late Eocene.)

Crepidula pileum is distinguished from other species
of Crepidula by its small size, low apex, and sinuous
internal deck margin.

L0calities.—USGS 15264, 15310, 15310d; ﬁgured
specimen from road cut on the Vernonia-Scappoose

 
31

road, approximately 2 miles from the junction with
State Highway 47. Pittsburg Bluff Formation.

Occurrence elsewhere.—Cowlitz Formation (late
Eocene) and Gries Ranch Formation (early Oligocene),
Washington; Coaledo Formation (late Eocene), Oregon;
Tejon Formation (early, middle and late Eocene),
California. Family NATICIDAE

Subfamily NATICINAE
Genus Cryptonatica Dall

Cryptonatica Dall, 1892 (1890—1903), Wagner Free Inst. Sci. Trans., v.

3, pt. 2, p. 362.

Type species.—By subsequent designation (Dall,
1909, p. 85), Natica clausa Broderip and Sowerby.
Holocene, Arctic Ocean to Queen Charlotte Islands.

Dall proposed Cryptonatica for species with a smooth
calcareous operculum and an umbilicus entirely ﬁlled
with callus. Tectonatica is generally used for a small
tropical species (Type: Natica tectula Bonelli) and
Cryptonatica for a large boreal species. Another criter-
ion that has been used for distinguishing the shells of
the two forms is that the umbilical callus of the type
species of Tectonatica does not completely ﬁll the um-
bilicus (Woodring, 1957, p. 88), whereas in Cryptonatica
clausa it does. In the fossil species Cryptonatica
oregonensis (Conrad) from the Astoria Formation of
Oregon, specimens are found representing both types of
umbilical closure (Moore, 1963, pl. 2, ﬁgs. 2, 16).

Cryptonatica pittsburg'ensis n. sp.
Plate 1, ﬁgures 9, 12, 13, 15, 16, 18, 19, 23

Cryptonatica pittsburgensis is small to moderate in
size (largest specimen: 28 mm high, 23 mm wide); most
of the specimens are small. The umbilicus is usually
completely ﬁlled with callus (pl. 1, ﬁg. 13) but there are
rare specimens which have a slight groove behind the
callus. When the shell exfoliates, only a round umbilical
plug is left. The spire is small and low, and the whorls
are evenly rounded without a shoulder.

Holotype.—Herewith designated USNM 213951,
plate 1, ﬁgure 13.

Type l0cality.—USGS 15310h. First large roadcut on
west side of Scappoose-Vernonia Road, south of cutoff to
Wilark, Columbia County, Oreg. Pittsburg Bluff
Formation, middle Oligocene.

The body whorl of C. pittsburgensis is more inﬂated
and is not so high as on Cryptonatica oregonensis
(Conrad) (Moore, 1963, p. 27, pl. 2, ﬁgs. 2—4, 16, 17) from
the Astoria Formation (Miocene), Oregon. The body
whorl is less inﬂated than that of "Natica” weaveri
Tegland (1933, p. 138—139) from the Gries Ranch (lower
Oligocene) and Lincoln Creek (late Eocene to early
Miocene) Formations in Washington.

Localities—USGS 2714, 5394, 15264, 15264a,
15264b, 15264e, 15310, 15310a-j, 15586, 15588, 18638,
21612, M3857, M3871, M3872, M3877, M3878.

32

Subfamily POLINICINAE

Genus Polinices Montfort
Polinices Montfort, 1810, Conchyliologie systématique, V. 2, p. 223.
Type species.——By original designation, Polinices
albus Montfort (=Natica mamillaria Lamarck = N atica

brunnea Link). Holocene, West Indies.

Polinices washingtonensis (Weaver)
Plate 1, ﬁgures 14, 17, 20—22, 24

Natica washingtonensis Weaver, 1916a, Washington Univ. (Seattle)
Pubs. Geology, v. 1, p. 44, pl. 5, ﬁgs. 73—76.

Polinices washingtonensis (Weaver). Clark and Anderson, 1938, Geol.
Soc. American Bull., V. 49, p. 954, pl. 3 ﬁgs. 16, 17. Weaver, 1942,
Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 337, pl. 68, ﬁgs.
18, 23. Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p.
84—85, pl. 11, ﬁgs. 12—19.

N atica lincolnensis Weaver, 1916a, Washington Univ. (Seattle) Pubs.
Geology, v. 1, p. 44—45, pl. 5, ﬁgs. 71, 72.

Polinices (Polinices) washingtonensis (Weaver) var. lincolnensis
(Weaver). Weaver, 1942, Washington Univ. (Seattle) Pubs. Geolo-
gy, v. 5, p. 337—338, pl. 68, ﬁg. 22, pl. 69, ﬁgs. 4, 7.

Polinices washingtonensis is of moderate size with a
fairly thick shell, moderate spire, evenly rounded body
whorl, and spire without shoulders. The shell is smooth
except for bunched radial lines that increase in
prominence with erosion of the shell.

Holotype.—CAS 7516.

Type locality—Cut along Union Paciﬁc Railway 1
mile north of Galvin Station, Lewis County, Wash.
Lincoln Creek Formation, late Eocene to early Miocene.

Tegland (1933, p. 139), Clark and Anderson (1938, p.
954), and Hickman (1969, p. 85) thought that Polinices
washingtonensis and Polinices lincolnensis were
probably conspeciﬁc. Efﬁnger (1938, p. 377) thought
that the forms were probably distinct. Weaver (1942, p.
337—338) considered P. lincolnensis as a variety of P.
washingtonensis; he believed that P. lincolnensis dif-
fered from P. washingtonensis by having the umbilicus
wide open whereas the umbilicus of P. washingtonensis
was covered by a heavy callus. He also believed that the
two forms he described were of possible stratigraphic
signiﬁcance. On the basis of a comparison of type
specimens of "Natica” washingtonensis Weaver (CAS
7516) and "'Natica” lincolnensis Weaver (CAS 7515A)
and other available material, it is my belief that they
belong to one variable species. The specimens that were
removed from the same piece of rock represent the two
forms (pl. 1, ﬁgs. 17, 20). Therefore it is difﬁcult to
believe that they might be of stratigraphic signiﬁcance.
The degree of closure of the umbilicus is not related to
the size of the specimen.

The type specimen of Polinices washingtonensis is
smaller than that of Polinices washingtonensis lin—
colnensis. Because the inner edge of the callus lobe is
broken on the type specimen of P. washingtonensis
lincolnensis, an erroneous impression is given of the
extent of coverage of the umbilicus; the umbilical area is

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

larger than it is on P. washingtonensis. In the original
description, the umbilical opening was said to be en-
tirely absent on P. washingtonensis, but it is not en-
tirely absent; the callus does not completely cover the
umbilical area, there is a funnellike groove behind it. It
is well known that the variability within species of the
naticids can be great and that factors such as size, sex,
and preservation increase this variability. With no
evidence that the two forms P. washingtonensis and P.
washingtonensis lincolnensis have different strati-
graphic positions, it is illogical to separate them.

L0calities.——USGS 2714, 5394, 15264, 15310, 15310a,
c—e, g, h, 15588, M3871, M3878.

Occurrence elsewhere.—Gries Ranch Formation
(early Oligocene), Quimper Sandstone of Durham
(1942) (early and middle Oligocene), Lincoln Creek
Formation (late Eocene to early Miocene), Blakeley
Formation of Weaver (1912) (late Oligocene and early
Miocene), Washington; Alsea Formation (early, middle
and late Oligocene), Tunnel Point Sandstone (middle
Oligocene), Eugene Formation (early and middle
Oligocene), Oregon; Wheatland Formation of Clark and
Anderson (1938) (late Eocene or early Oligocene), upper
part of San Emigdio Formation (late Eocene to middle
Oligocene), California.

Genus Neverita Risso
Neverita Risso, 1826, Histoire naturelle des principales production de

l’Europe Méridionale, v. 4, p. 149.

Type species.—By monotypy, Neverita josephinia
Risso. Holocene, Mediterranean Sea.

Subgenus Glossaulax Pilsbry
Glossaulax Pilsbry, 1929, Nautilus, v. 42, p. 113.

Type species.—Holotype by original designation,
Neverita reclusiana (Deshayes). Holocene, southern
California, and throughout Gulf of California to Tres
Marias Islands, Mexico (Keen, 1971, p. 482).

Neverita (Glossaulax) thomsonae Hickman
Plate 2, ﬁgures 1—15

Neverita (Glossaulax) thomsonae Hickman, 1969, Oregon Univ. Mus.
Nat. Hist. Bull. 16, p. 84, pl. 11, ﬁgs. 20—23.

Neverita thomsonae is moderate to large in size
(largest specimen 47 mm wide and 39 mm high, in-
complete); it has a thick shell, large globose body whorl,
and a small, low spire. The suture is overlapping and no
tabulation is present. The shell is usually smooth, but
on some specimens (pl. 2, ﬁg. 15) spiral lines can be seen
near the base of the body whorl. The shape and size of
the umbilical callus is variable, depending largely on
the size of the entire shell. The largest shells have a very
thick callus Whereas the smallest shells have a callus of
moderate thickness. The callus completely ﬁlls the
umbilical area and is grooved. The posterior portion of
the biﬁd callus is the largest and is rounded and
pluglike; the anterior portion is small and triangular.

CLASS GASTROPODA

The outer lip protrudes a few millimetres beyond the
callus.

Holotype.—UO 27366. Paratypes: UO 27367—27372.

Type locality—U0 2567. In well indurated
brownish-gray tuffaceous sandstone and siltstone, east
side of Oregon State Highway 47, 2 miles north of
junction with Pittsburg-Scappoose Road. N1/2 sec. 23, T.
5 N., R. 4 W., Vernonia quadrangle. Type Pittsburg
Bluff Formation (middle Oligocene), Oregon.

N. thomsonae is a much larger and heavier shelled
form than any of the Eocene species of Neverita that I
have examined. It is larger than Neverita jamesae
Moore from the Astoria Formation (Miocene), Oregon
(Moore, 1963, p. 28) and has a much larger and heavier
umbilical callus.

N everita lives intertidally on sandbars where it preys
on clams (Keen, 1971, p. 482) and in lagoons and shal-
low bays (McLean, 1969, p. 37).

Localities.—USGS 2714, 5394, 15264, 15310, 15310a,
d—g, j, 15311, 15312, 15588, M3857, M3858, M3871,
M3878.

Occurrence elsewhere—Eugene Formation (early
and middle Oligocene), Oregon; Wygal Sandstone
Member of the Temblor Formation (late Oligocene),
California.

Subfamily SININAE
Genus Sinum Roding'
Sinum Roding, 1798, Museum boltenianum, pt. 2, p. 14.

Type species.—By subsequent designation (Dall,
1915, US. Natl. Mus. Bull. 90, p. 109),Helix haliotoidea
Linné. Holocene, western Paciﬁc Ocean(?). Subgeneric
assignments are discussed by Addicott (1970c, p. 70).

Sinum aff. S. obliquum (Gabb)
Plate 1, ﬁgures 10, 11

Two small specimens of Sinum (largest: 10 mm high,
9.3 mm wide) were collected from the Pittsburg Bluff
Formation. Sinum aff. S. obliquum (Gabb) is thin shel—
led and has a small low spire and spiral cords of equal
size with ﬁner cords present in some but not all of the
interspaces. The secondary cords are more numerous
near the round shoulder. Of the described west Ameri-
can species, it resembles Sinum obliquum (Gabb) (1864,
p. 109, 225, pl. 21, ﬁg. 112) from the Eocene and
Oligocene of the Paciﬁc coast, but it seems to have a
higher body whorl and a more ovate and perpendicular
aperture. It is much smaller than Sinum scopulosum
(Conrad) (1849, p. 727, pl. 19, ﬁgs. 6, 6a; Moore, 1963, p.
29, pl. 1, ﬁgs. 2, 3, pl. 2, ﬁgs. 20, 21) from the Miocene and
Pliocene of the Paciﬁc coast and seems to have a less
inﬂated body whorl. It has not. been possible to de-
termine, on the basis of the two specimens available, if
this is a new species.

Localities.—USGS 15264, 15264e.

Occurrence elsewhere—Of Sinum obliquum (Gabb):

 
33

Cowlitz (late Eocene) and Gries Ranch (early Oligocene)
Formations, Washington; Keasey (late Eocene and
early Oligocene) and Eugene (early and middle
Oligocene) Formations, Oregon; Tejon Formation (ear-
ly, middle and late Eocene), California.

Family NEPTUNEIDAE
Genus Eosiphonalia Ruth

Eosiphonalia Ruth, 1942, California Univ. Pubs, Dept. Geol. Sci.

Bull., v. 26, no. 3, p. 288.

Type species.—-—By original designation, Strepsidura
washingtonsis Weaver, Lincoln Creek Formation (late
Eocene to early Miocene), Washington.

As noted by Ruth (1942, p. 288), Eosiphonalia is
distinguished from Siphonalia by its lower spire, shor-
ter and less recurved canal, biangulate body whorl that
is more nodose, and lack of lirations on the inner lip.
Eosiphonalia is an Oligocene genus endemic to
California, Oregon, Washington, and Alaska.

Eosiphonalia oregonensis (Dall)
Plate 4, ﬁgures 1—9
Strepsidura oregonensis Dall, 1909, US. Geol. Survey Prof. Paper 59,
p. 51, pl. 3, ﬁg. 6.

Siphonalia (Easiphonalia) oregonensis Dall. Ruth, 1952, California
Unit. Pubs, Dept. Geol. Sci. Bull., v. 26, p. 290, pl. 47, ﬁg. 20.
Siphonalia oregonensis (Dall). Weaver, 1942, Washington Univ.

(Seattle) Pubs. Geology, v. 5, p. 439, pl. 86, ﬁg. 12.

Eosiphonalia oregonensis is of moderate size; the
largest s specimen is 39.2 mm high and 27.5 mm wide
(pl. 4, ﬁgs. 1, 3). The spire is low, making up a quarter of
the total shell height, is tabulate, and has nodes on the
shoulders. The body whorl is large, inﬂated, and
sculptured usually by three or four, but sometimes ﬁve,
prominent spirals that are separated by angulations.
The spiral on the shoulder has nodes, and usually the
next two anterior spirals are also noded. The entire shell
is sculptured by ﬁne spirals of approximately equal
strength. The siphonal canal is deeply notched and
slightly recurved. The area between the last strong
spiral on the body whorl and the canal is moderately to
deeply impressed.

Holotype.—USNM 107395, plate 4, ﬁgures 4, 6.

Type locality.—USGS 2714. In ﬁne-grained
brownish—gray sandstone in roadcut at Pittsburg Bluffs,
Columbia County, Oregon. Pittsburg Bluff Formation,
middle Oligocene.

Two described fossil species resemble E. oregonensis:
E. washingtonensis (Weaver) (1916a, p. 48—49, pl. 5,
ﬁgs. 81—83) from the Lincoln Creek Formation (late
Eocene to early Miocene), Washington, and E. califor—
nica (Arnold) (1908, p. 370—371, pl. 33, ﬁg. 12) from the
San Lorenzo Formation (late Eocene to middle
Oligocene), California. E. washingtonensis is a smaller
form with a higher spire and stronger nodes, some of
which are almost spinose. It has two or three raised

34

spirals with nodes on the body whorl; the ﬁner spirals
are more prominent than on E. oregonensis. Weaver
(1942, p. 439) said that E. washingtonensis has a
nonornamented band just posterior to the siphonal
fasciole at the end of the canal that distinguishes it from
E. oregonensis; such an area is not discernible on the two
specimens examined.

E. californica is a higher spired form, has stronger
nodes than E. oregonensis, and has two angulations on
the body whorl.

L0calities.—USGS 15264, 15310, 15310a, (1, 15532,
15537, 15588, M3857, M3871.

Occurrence elsewhere—Poul Creek Formation
(Oligocene and Miocene), Yakataga district, Gulf of
Alaska.

Genus Bruclarkia Trask
Bruclarkia Trask in Stewart, 1926, Acad. Nat. Sci. Philadelphia Proc.,

V. 78, p. 397, 399.

Type species.—By original designation, Clavella
gravida Gabb. Lower Miocene, Contra Costa County,
Calif.

Bruclarkia is an endemic Paciﬁc coast genus; it ﬁrst
appears in the early Oligocene and becomes extinct
before the end of the Miocene. Its known geographic
range is from California north to Alaska. Vokes (1939,
p. 138) suggests that Bruclarkia may have developed
from the Eocene genus U mpq uaia (Turner, 1938, p. 79).

The degree of development of nodes and spines is not
believed to be a speciﬁc character in Bruclarkia but
rather to usually be an expression of variability within
a species (Moore, 1963, p. 36). Exceptions may be found,
of course, where there is a relation between degree of
sculpture and stratigraphic occurrence. Characters that
have been found to be valid in separating species of
Bruclarkia are the conﬁguration and extent of de-
velopment of the shoulder on the body whorl, the
number and spacing of the strong spiral cords on the
body whorl, and the height of the spire in relation to the
size of the body whorl.

Bruclarkia columbiana (Anderson and Martin)
Plate 3, ﬁgures 1—5, 21—23
Agasoma columbianum Anderson and Martin, 1914, California Acad.

Sci. Proc., ser. 4, v. 4, p. 73, pl. 5, ﬁgs. 6a, 6b.

Bruclarkia columbiana (Andeeson and Martin). Weaver, 1942,

Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 443, pl. 87, ﬁgs. 7,

8. Durham, 1944, California Univ. Pubs, Dept. Geol. Sci. Bull., v.

27, p. 173. Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p.

94, pl. 13, ﬁgs. 12, 13.

Bruclarkia columbiana is the largest species in the
genus; individuals grow to a height of 60 mm and a
width of 48 mm. The spire is low, about one-fourth the
height of the body whorl, and the body whorl is greatly
inﬂated. The species has three prominent spiral cords on
the body whorl; the one on the shoulder and the one
below it are nodose to slightly spinose; the third and

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

most anterior spiral may be smooth or slightly noded.
One noded prominent spiral may be present on the
whorls of the spire at or just above the suture, which is
strongly overlapping. On well-preserved specimens, a
collar, sculptured by prominent spirals, is present at the
suture (pl. 3, ﬁg. 5), but this collar apparently exfoliates
readily, as it is rarely preserved, even on specimens
with the remainder of the shell intact. The entire sur-
face of the shell is sculptured by subrounded spiral cords
of varying strength that may be separated by ﬁner
secondary cords. The siphonal canal is long and re-
curved.

Holotype.—CAS 155. Paratype CAS 156.

Type locality.—At Pittsburg Bluffs, Columbia Coun-
ty, Oreg. Pittsburg Bluff Formation (middle Oligocene),
Oregon.

The holotype of B. columbiana is 56 mm high and 40
mm wide, bears three nodose spirals on the body whorl,
and has an overlapping, sinuous, swollen and collared
suture. There are no nodes on the spire. The paratype of
B. columbiana bears three spirals on the body whorl.
These spirals are slightly spinose over two-thirds of the
body whorl, but smooth on one-third of the body whorl
near the aperture. The suture on the body whorl of the
paratype is sinuous, overlaps the spire, and is strongly
collared near the aperture. The whorls of the spire bear
nodes on the spiral just above the suture on the
paratype; they are smooth on the holotype.

Specimens of B. columbiana from USGS locality
15310 have much stronger nodes and are generally
larger than specimens from other localities within the
Pittsburg Bluff Formation.

B. columbiana is distinguished from other described
species of Bruclarkia by the constant 40° slope from the
suture to the shoulder margin of the body whorl, the low
spire, the strongly inﬂated body whorl, and the two
prominent, noded spiral cords on the body whorl, one on
the edge of the shoulder and the other below it.

Durham (1944, p. 173) reportsB. col umbiana from the
Molopophorus gabbi, Turritella olympicensis, and T.
porterensis Zones of northwestern Washington.

L0calities.—USGS 2415, 2714, 2715, 2721, 5394,
15264, 15264a, 15310, 15310a—c, e, f, j, 15312, 15316,
15499, 15532, 15586, 15588, 18638, M3858, M3871,
M3872, M3877, M3878.

Occurrence elsewhere.——Quimper Sandstone of Dur-
ham (1942) (early and middle Oligocene), Marrowstone
Shale (early Oligocene), and Lincoln Creek Formation
(late Eocene to early Miocene), Washington; Alsea
Formation (early to late Oligocene), upper part of the
Eugene Formation (middle Oligocene), and Tunnel
Point Sandstone (middle Oligocene), Oregon; Cymric
Shale Member of the Temblor Formation (middle
Oligocene), California.

CLASS GASTROPODA 35

Family BUCCINIDAE‘?
Genus Molopophorus Gabb

Molopophorus Gabb, 1869, California Geol. Survey, Paleontology, v.
2, p. 156—157, 219, pl. 26, ﬁg. 36.

Type species.—By monotypy, Bullia (Molopophorus)
striata Gabb. Tejon Formation, upper Eocene,
California.

Molopophorus is an endemic Paciﬁc coast genus
appearing in the Eocene and becoming extinct by the
end of the Miocene. It is found in Alaska, Washington,
Oregon, and California, and is particularly common in
the Pittsburg Bluff Formation.

Molopophorus gabbi Dall
Plate 5, ﬁgures 1—22

Molopophorus gabbi Dall, 1909, U.S. Geol. Survey Prof. Paper 59, p.
45, pl. 3, ﬁg. 8. Anderson and Martin, 1914, California Acad. Sci.
Proc., ser. 4, v. 4, p. 78, pl. 6, ﬁgs. 5a, 5b. Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 466—467, pl. 90, ﬁgs. 4, 6.

Molopophorus biplicatus quadranodosum Weaver, 1912, Washington
Geol. Survey Bull. 15, p. 75—76, pl. 11, ﬁgs. 91—93; pl. 14, ﬁg. 122.

Molopophorus gabbi is moderate in size (largest
specimen 30 mm high and 20 mm wide); it has a rather
thin shell, inﬂated body whorl, and short, deeply
notched, siphonal canal. The most distinctive character
of the species is its marked variation in body whorl
sculpture. Usually the sculpture consists of four
prominent spiral cords. Starting at the posterior end,
the ﬁrst three are equally spaced and the fourth has only
half as much space separating it from the third spiral
(pl. 5, ﬁgs. 10, 11, 16). On some specimens (pl. 5, ﬁgs. 8,
9), the four prominent spiral cords are equally spaced,
and on the other specimens only three spiral cords are
present (pl. 5, ﬁg. 15). The spirals may be crossed by
axial lines that form nodes (pl. 5, ﬁg. 20) or spines (pl. 5,
ﬁg. 8) at the juncture or that may form axial ribs (pl. 5,
ﬁg. 12). The suture is sinuous and the collar overlaps the
spire; more than one-third of the body whorl im-
mediately below the suture is unsculptured. Immature
forms lack the large unsculptured area on the body
whorl and are usually more strongly sculptured over the
rest of the shell.

Type—USNM 107377 (pl. 5, ﬁgs. 19, 22) is herewith
designated the lectotype. This is the specimen origi-
nally ﬁgured by Dall (1909, pl. 3, ﬁg. 8) and represents
the smooth form. A strongly sculptured specimen in
Dall’s type lot is assigned USNM 214016 (pl. 5, ﬁg. 21).
The remaining specimen in the type lot has been as-
signed USNM 214015.

Type locality.—USGS 2714. Pittsburg, Columbia
County, Oreg. Pittsburg Bluff Formation, middle
Oligocene.

The lectotype (ANSP 4340) of Molopophorus bipli-
catus (Gabb) 1866, p. 9, pl. 2, ﬁg. 14), from the San
Ramon Sandstone (early Miocene?) in California, has a
less inﬂated body whorl and a higher spire than M.

 
gabbi. Its collar is not so strongly overlapping and
prominent, nor does it have as large a concavity below
the collar on the body whorl as M. gabbi. The three
specimens in the type lot are not too well preserved, but
they do show axial ribs on the body whorl that may
become obsolete toward the aperture. Clark (1918, p.
174) considered M. gabbi and M. biplicatus to be so
closely related that he considered M. gabbi to be a
subspecies of M. biplicatus. The two specimens ﬁgured
by Clark (1918, pl. 6, ﬁgs. 7a, 7b) were collected from the
San Ramon Sandstone and compare well with M.
biplicatus.

Weaver (1912, p. 75—76, pl. 11, ﬁgs. 91—93, pl. 14, ﬁg.
122) described Molopophorus biplicatus quad-
ranodosum from the middle Oligocene of Washington.
Weaver (1942, p. 469) thought that the four promi—
nently noded spiral ribs on the middle of the body whorl
distinguished this subspecies. The large number of
specimens of M. gabbi now available show that this
ornamentation is common on M. gabbi. The holotype of
M. biplicatus quadranodosum has been lost.

Molopophorus dalli Anderson and Martin (1914, p.
78, pl. 6, ﬁgs. 7a, 7b) lacks the strong sculpture of M.
gabbi and never has nodes or spines, although it may be
cancellate or beaded (Hickman, 1969, p. 91, pl. 13, ﬁg.
1). M. dalli was originally collected near Clatskanie,
Greg, in rocks that are now assigned to the Gries Ranch
Formation (early Oligocene) (Warren and others, 1945).
Durham (1944, p. 170) reports M. dalli from his
Molopophorus gabbi Zone, speciﬁcally from a locality in
the Quimper Sandstone of Durham (1942) (middle and
late Oligocene), Washington. Hickman (1969, p. 91)
reports the rare occurrence of M. dalli in the lower and
middle Eugene Formation, which she assigns to the
early Oligocene. She also collected some specimens of M .
dalli from the Salem area, in beds questionably referred
to the upper (middle Oligocene) part of the Eugene
Formation. M. dalli has not been found in any of the
collections from the Pittsburg Bluff Formation at hand,
and it seems probable that M. dalli may be restricted to
the early Oligocene.

Molopophorus lincolnensis Weaver (1916a, p. 50, pl.
4, ﬁgs. 60, 61), a common species in the Lincoln For-
mation (late Eocene to early Miocene) in Washington, is
distinguished from M. gabbi by its smaller size and lack
of spiral sculpture. The sculpture consists only of axial
ribs.

Localities.—USGS 2415, 2714, 5394, 15264, 15264a,
e, d, 15278, 15310, 15310a—j, 15311, 15312, 15532,
15544, 15586, 15588, 18638, 18779, M3858, M3860,
M3871, M3877, M3878.

Occurrence elsewhere.—Quimper Sandstone of
Durham (1942) (early and middle Oligocene), reported
by Weaver (1916d, p. 39) from the Lincoln Creek

36 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Formation (late Eocene to early Miocene), Washington;
Gries Ranch Formation (early Oligocene), USGS 5210,
Tunnel Point Sandstone (middle Oligocene), Oregon;
San Lorenzo Formation (late Eocene to middle
Oligocene), California (Clark, 1915, p. 18).
Family FUSINIDAE
Genus Priscofusus Conrad

Priscofusus Conrad, 1865, Am. Jour. Conchology, v. 1, p. 150.

Type species.—By subsequent designation (Cossman,
1901, Essais de paleoconchologie comparée, p. 8), Fusus
geniculus Conrad. Astoria Formation, Miocene, Ore-
gon.

Priscofusus is an endemic Paciﬁc coast genus ap-
pearing in the Paleocene and becoming extinct in the
Pliocene. Its geographic range is Alaska to California.

Priscofusus stewarti (Tegland)
Plate 3, ﬁgures 17—19
F usinus (Priscofusus) stewarti Tegland, 1933, California Univ. Pubs,

Dept. Geol. Sci. Bull, v.23, p. 129—30, pl. 12, ﬁgs. 4—8. Weaver, 1942,

Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 486—487, pl. 93,

ﬁgs. 3, 4, 10, 14.

Two small specimens of Priscofusus stewarti are in
the collections; one is almost complete; the other has
only the spire preserved. P. stewarti is slender in out-
line with small somewhat elongate nodes one-third the
whorl height above the suture. The surface is sculptured
with closely spaced subrounded spiral ribs of slightly
different widths; between the ribs there may be a spiral
thread.

Holotype.—UCMP 32238.

Type locality—Restoration Point, opposite Seattle,
Wash. Blakeley Formation of Weaver (1912) (late
Oligocene and early Miocene).

Priscofusus chehalisensis (Weaver) (1912, p. 78—79,
pl. 6, ﬁgs. 65, 66) is larger and has a much higher and
slimmer spire than P. stewarti.

Localities.———USGS 15264, 15588, M3871.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Yakataga district, Gulf
of Alaska; Blakeley Formation (late Oligocene and
early Miocene), Washington; Alsea Formation [early to
late Oligocene].

Family FASCIOLARIIDAE
Genus Perse Clark
Perse Clark, 1918, California Univ. Dept. Geology Bull., v. 11, p. 179.

Type—By original designation, Perse corrugatum
Clark. San Ramon Sandstone (early Miocene?), Cali-
fornia.

Perse is an endemic west coast genus found in Eocene
to Miocene rocks in California, Oregon, and
Washington. It ﬁrst appears in the late Eocene and
becomes extinct at the end of the early Miocene, or the
end of the Oligocene, depending upon the age as-
signment given to the Blakeley and San Ramon

 
Formations of Washington and California, respectively.

Stewart (1926, p. 401—402) proposed a new genus,
Whitneyella and designated Hemifus us washingtoniana
Weaver (1912, p. 46—47, pl. 2, ﬁg. 11, not ﬁg. 12) as the
type species. Stewart considered the type specimen of
Perse corrugatum to be generically distinct from the
group represented by Hemifusus washingtoniana,
although Clark had placed H. washingtoniana in his
genus Perse. In 1938, Clark (p. 718—719) placed
Whitneyella in synonymy with Perse, saying that the
anterior end of the canal of the poorly preserved type
specimen of P. corrugatum was broken off and that the
original illustration was therefore misleading.
Examination of the type specimen of P. corrugatum
shows it to be congeneric with Hemifusus washing-
toniana, and this group is therefore assigned the older
name Perse.

Perse is usually of small to moderate size, it has a thin
shell that has a long, slightly recurved canal. The an-
terior end of the canal is very narrow, and specimens are
rarely collected with the canal intact. On broken
specimens, the narrowness of the canal may lead one to
suppose erroneously that it would have been about half
of its actual length. Slightly rounded to ﬂat-topped spi-
ral cords form the predominant sculpture. These cords
may have weak nodes or axial swellings. The suture is
collared and overlaps the spire; the collar varies in
strength and may be smooth or sculptured by spiral
cords. The spire is usually low and less sculptured than
the body whorl. A pronounced concavity occurs between
the suture and the maximum inﬂation of the whorls;
this concavity is particularly well developed on the body
whorl.

Perse pittsburg‘ensis Durham
Plate 6, ﬁgures 1, 4, 6, 7, 9, 12—14, 18—20
Perse pittsburgensis Durham, 1944, California Univ. Pubs, Dept.
Geol. Sci. Bull., v. 27, p. 175, pl. 16, ﬁgs. 2, 4.

Perse pittsburgensis is a small- to moderate-sized
species (largest specimen: 27 mm high, 15 mm wide)
with a thin shell. The suture is collared and overlaps the
spire; the collar usually bears two closely spaced, ﬂat
spirals. The spire and body whorl are sculptured by
slightly rounded, straplike spiral cords that are gen-
erally smooth but may be slightly noded. The spirals are
most strongly developed on the maximum swelling of
the whorls, and all are separated by interspaces that
may be equal to one and one-half times the width of the
spirals. The Wider interspaces may bear a secondary
spiral thread. A concavity is present on the body whorl
between the suture and the ﬁrst strong spiral just above
the maximum point of inﬂation; it generally bears
spirals of somewhat smaller size than on the rest of the
body whorl. The whorls of the spire are roundly
tabulate. The siphonal canal is long, very narrow, and
slightly recurved (pl. 6, ﬁgs. 1, 4).

CLASS GASTROPODA

Holotype.—-UCMP 35409.

Type locality. ——In bluffs along road along the east side
of the highway along the Nehalem River, about 21 miles
south of Mist and 0.2 mile north of junction with road to
St. Helens, and 0.25 mile north of bridge. Pittsburg
Bluff Formation (middle Oligocene), Oregon.

P. pittsburgensis varies considerably in degree of
sculpture, but it always bears straplike spiral cords and
has a characteristic outline with a low spire and an
inﬂated body whorl bearing a deep but relatively short
sinus. P. pittsburgensis vernoniensis has a longer
concavity between the suture and the periphery, and
bears, if any, only one strong straplike spiral on this
concavity. The sculpture usually consists of ﬁne spiral
threads. The entire shell is slimmer and the spire is
higher than that of P. pittsburgensis.

Perse olympicensis Durham (1944, p. 174—175, pl. 16,
ﬁg. 1), from the early Oligocene Molopophorus
stephensoni Zone, does not bear the straplike spirals of
P. pittsburgensis. P. Olympicensis quimpersensis
Durham (1944, p. 175, pl. 16, ﬁgs. 5, 6), from the middle
Oligocene Molopophorus gabbi Zone, is distinguished
by having longitudinal ribs.

Localities.—USGS 2714, 2722, 5394, 15264,
15264b,c,e,15278,15310,15310b, c,e—j, 15311,15312,
15519, 15537, 15545, 15586, 15588, 18638, 18779,
M3856, M3857, M3858, M3866, M3868, M3871, cf.
M3872, M3877, M3878.

Occurrence elsewhere.—Alsea Formation (early,
middle, and late Oligocene), Oregon.

Perse pittsburgensis vernoniensis, n. subsp.
Plate 6, ﬁgures 2, 3, 5, 8, 10, 11, 15—17

Perse pittsburgensis vernoniensis is fusiform in
outline, is of moderate size (largest specimen: 29 mm
high, 16 mm wide), and has a higher spire than is usual
for Perse. It is sculptured with rounded spiral cords
which may be noded with axial swellings (pl. 6, ﬁgs. 10,
17), noded without axial swellings (pl. 6, ﬁg. 16), or
fairly smooth (pl. 6, ﬁgs. 2, 3). Secondary cords of about
half the width of the primaries may be present in the
interspaces, but their occurrence and distribution is
random. The interspace may be two to three times as
wide as the spiral cord. Fine spiral threads are present
on the sinus of the body whorl and on the sinus of the
spire whorls, if such a sinus is present. The canal is very
long, slender, and slightly recurved; the entire canal is
not preserved on any specimen. The inner lip is lirate;
the suture is overlapping and collared and the collar
bears one or two spiral cords. Below the collar is a sinus;
it is strongly developed on the body whorl, occasionally
shows on the two preceding whorls, but is never present
on the ﬁrst three whorls. The sinus is always sculptured
by ﬁne spiral threads and may also bear one strong
spiral cord.

 
37

Holotype.—USNM 214017 is herewith designated the
holotype (pl. 6, ﬁgs. 5, 8).

Type locality.—USGS 15588. Cut in logging road
along the headwaters on the second main tributary
entering Coal Creek from the northeast of its junction
with Pebble Creek, 3,900 feet west of grid 820 and 5,200
feet south of grid 2,650, Vernonia quadrangle. Pittsburg
Bluff Formation (middle Oligocene), Oregon.

The shape and sculpture distinguish P. pittsburgensis
vernoniensis, although, as can be seen on plate 6, the
sculpture is variable. The spire is higher, the sinus is
less sculptured and more pronounced, and the spiral
cords are ﬁner and farther apart than on Perse pitts-
burgensis; P. pittsburgensis vernoniensis, has a longer
concavity between the suture and the maximum swell-
ing of the body whorl, and bears, if any, only one strong
straplike spiral on this concavity. The sculpture con-
sists usually of ﬁne spiral threads. The entire shell is
slimmer than that of P. pittsburgensis.

Perse lincolnensis (Van Winkle) (1918, p. 89—90, pl. 7,
ﬁg. 10) is higher spired than P. pittsburgensis ver-
noniensis with ﬁner spiral sculpture that bears nodes or
spines.

Perse Olympicensis Durham (1944, p. 174—175, pl. 16,
ﬁg. 1) does not bear straplike spirals like P.
pittsburgensis vernoniensis does, and P. Olympicensis
quimpersensis Durham (1944, p. 175, pl. 16, ﬁgs. 5, 6) is
distinguished by longitudinal ribs.

P. pittsburgensis vernoniensis occurs at only eight
localities in the Pittsburg Bluff Formation but is very
abundant at these localities and occurs with P.
pittsburgensis at many of them.

Localities.—USGS 2714, 15264, 15536, 15588, 18779,
21612, M3871, M3872, M3878.

Family TURRIDAE

Subfamily TURRICULINAE
Genus Aforia Dall

Aforia Dall, 1889, Mus. Comp. Zool. Bull. 18, p. 99.

Type species. —By original designation, Pleurotoma
circinata Dall. Holocene, North Paciﬁc.

The known fossil occurrences of Aforia are in the
Pliocene of Japan, the Oligocene to Pliocene of
Washington, the Oligocene and Miocene of Oregon, and
the Oligocene or Miocene of California (Powell, 1966, p.
44; Javidpour, 1973, p. 197).

Aforia campbelli Durham
Plate 7, ﬁgure 22

Aforia campbelli Durham, 1944, California Univ. Pubs, Dept. Geol.
Sci. Bull., v. 27, p. 183—184, pl. 14, ﬁg. 4. Javidpour, 1973, Veliger, v.
15, p. 199—200, ﬁgs. 1, 6, 10.

Aforia clallamensis (Weaver) subsp. wardi (Tegland). Weaver, 1942,
Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 516—517, in part,
pl. 97, ﬁg. 10, not pl. 96, ﬁg. 6.

Six whorls of the spire of one specimen are preserved

as an external cast of Aforia campbelli. A rubber im—

38 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

pression that was made from it is illustrated in plate 7,
ﬁgure 22. Aforia campbelli is a large species,
pagodiform in outline; it has a sharp carina just above
the suture. The whorl is concave above the carina and
deeply concave below it. The sinus is deep and broadly
U-shaped and is located in the middle of the shoulder
above the carina. The shell seems to have been spirally
sculptured below the carinae.

Holotype.—UCMP 14961.

Type locality—A1636. Type “Porter” Bluffs along
northeast side of highway beginning at a point 270
yards southeast of ﬁrst exposure southeast of Porter
Station and extending 180 yards. Grays Harbor County,
Wash. Middle Oligocene, Lincoln Creek Formation.

A. campbelli has a slimmer spire and higher shoulder
above the angulation than A. wardi (Tegland, 1933, p.
124, pl. 10, ﬁgs. 5—8), and the angulation is closer to the
suture than on A. wardi. A. addicotti J avidpour (1973,
p. 201, ﬁgs. 8, 12) has the angulation closer to the middle
of the whorl and does not have as deep a concavity below
the angulation as A. campbelli. A. clallamensis
(Weaver, 1916a, p. 52, pl. 4, ﬁg. 59) has the angulation
near the middle of the whorl; the shoulder above the
angulation is not so high nor so concave as on A.
campbelli and the spire is slimmer. A. clallamensis does
not have a deep concavity beneath the angulation.

Javidpour (1973, p. 196—199) has discussed the
phylogenetics of the six species ofAforia reported from
the west coast of North America. To her record should be
added the occurrence of A. campbelli in the Pittsburg
Bluff middle Oligocene of northwestern Oregon and of
A. clallamensis (Weaver) in the Astoria Formation,
Miocene, of the Newport area, Oregon (Moore, 1963, p.
47, pl. 10, ﬁgs. 16, 18).

Locality.—USGS 15519.

Occurrence elsewhere—Lincoln Formation (late
Eocene to early Miocene), Washington.

Subfamily TURRINAE?
Genus Taranis J effreys
Taranis Jeffreys, 1870, Ann. Mag. Nat. Hist, ser. 4 (5), p. 447.

Type species.—By monotypy, Trophon morchi Malm.
Holocene, North Atlantic.

Taranis has a very small, ovate-biconic, predomi-
nantly medially angulate and spirally keeled shell. The
protoconch is paucispiral, of barely two whorls, papil-
late to slightly globose, superﬁcially smooth, but it has a
microscopic sculpture of closely spaced stippled spiral
lirae. The sinus is shallow; its apex is at the peripheral
angle or major keel; and its angles of approach are
unequal—steep and straight above, protractively
arcuate below. The pillar is abruptly twisted at the
beginning of a short shallowly notched anterior canal.
The subfamily position of Taranis is problematic, but
based on the type of sinus, the apex of which is

 
peripheral, the genus is provisionally placed in the
Turrinae (Powell, 1966, p. 55).

The known fossil occurrences of Taranis are in the
Pleistocene of England, Sicily, California, and New
Zealand; the Pliocene of Italy; the Oligocene and
Miocene of Oregon; and the Miocene of California.

Taranis columbiana (Anderson and Martin)
Plate 7, ﬁgures 2, 3, 5—8, 16, 37
Drillia col umbiana Anderson and Martin, 1914, California Acad. Sci.

Proc., ser. 4, v. 4, p. 94, pl. 7, ﬁgs. 4a, 4b. Not Drillia columbiana

Anderson and Martin of Adegoke, 1969, California Univ. Pubs.

Geol. Sci., V. 80, p. 192, pl. 13, ﬁg. 10.

Thesbia columbiana (Anderson and Martin). Weaver, 1942,

Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 537, pl. 99, ﬁg. 13.

Taranis columbiana has a rather thick shell and a
moderately high spire. The sinus is shallow, U-shaped,
and conﬁned to the keel with almost equal angles of
approach. The angles are perhaps a bit steeper above
than below the sinus. The protoconch consists of a little
more than one and one-half rounded, smooth whorls (pl.
7, ﬁg. 8). At the apex is a twisted, recurved, hooklike
process that is centrally located. This process forms a
spur off the protoconch, rather than from the tip of the
last whorl, and looks as if it were the columella pro-
truded from the center. The body whorl is small and
canal is short, recurved, and slightly notched.

Holotype.—CAS 231; paratype CAS 232.

Type locality. —Northwest Oregon. This is the locality
cited by Anderson and Martin (1914, p. 94) and agrees
with the label on the type specimens. The locality cited
by Weaver (1942, p. 537), “(CAS 65) West bank of small
canyon one and one-fourth miles northeast of Barker’s
Ranch house in Kern County, California” is in error. In
addition to checking the label with the holotype of
“Drillia” columbiana, the late Leo G. Hertlein, Califor-
nia Academy of Sciences, kindly checked the collection
from locality CAS 65 and found no specimen labelled
"D” columbiana. Presumably the type specimens of
"Drillia” columbiana were collected from the Pittsburg

Bluff Formation near Vernonia, Oreg.

Twenty specimens that are well enough preserved to
show shell sculpture are in the collections. These
specimens show three different forms of sculpture, and
specimens of each type are present at a single locality
(M3871). On the smooth-keeled form (pl. 7, ﬁgs. 6, 16)
the keel is smooth, straplike, slightly rounded, and not
sculptured. There are no spirals above or below the keel
on the spire. There is no spiral sculpture above the keel
on the body whorl. Below the keel a strong spiral forms
an angulation on the body whorl and above the
angulation are one or two ﬁne spirals. Below the second
strong spiral is a weaker but still strong spiral and
beneath this weaker one are eight ﬁne spirals of equal
strength. On the intermediate form (pl. 7, ﬁg. 37) the
keel on the early whorls is thin and smooth; the keel on

CLASS GASTROPODA 39

the later whorls is again straplike but bears three to
four spiral cords. The whorls have a ridgelike collar
bearing one or two spiral threads. Between the collar
and the keel may be an additional spiral thread. Below
the keel on the whorls of the spire is a fairly prominent
spiral cord. Below the keel on the body whorl are three
equally spaced smooth spiral cords followed by about
seven or eight ﬁner, equally spaced spirals. On the
sculptured-keeled form (pl. 7, ﬁg. 5), the keel spiral is
thin and rather pointed; above the keel are three ﬁne
spirals and on the collar one stronger spiral and one ﬁne
spiral. Above the keel, half way between the keel and
the suture, is a strong, sharply pointed spiral and below
it, right at the suture, is a smaller, more rounded spiral.
The keel of the body whorl is formed by one sharply
pointed spiral above which are three closely spaced ﬁner
spirals and one spiral on the collar. Below the keel are
three strong equally spaced spirals followed by eight
closely spaced ﬁner spirals. Given only the smooth-
keeled and sculptured-keeled forms, it would probably
seem as if two species were present, but the inter-
mediate form points to the fact that T. columbiana
varies markedly in its spiral sculpture.

Hickman (written commun., 1975) assigns Taranis
columbiana t0 Ptychosyrinx.

The specimen ﬁgured by Adegoke (1969, pl. 13, ﬁg. 10)
as Drillia columbiana Anderson and Martin, from the
Temblor Formation (Oligocene and Miocene), Coalinga
region, California, is much larger and different in
outline than Taranis columbiana. It lacks the deep
concavity below the whorl sutures of T. columbiana.

Localities.—USGS 15264, 15264a, b, 15310, 15310d,
M3871, M3872, cf. 15278.

Subfamily CLAVINAE
Genus Spirotropis Sars

Spirotropis Sars, 1878, Mollusca regionis Arcticae Norvegicae, p. 242,
pl. 17, ﬁgs. 5a, 5b.

Type species.-—By monotypy, Spirotropis carinata
Philippi. Holocene, Norway to Azores.

Spirotropis is thin shelled and has a moderately high
spire and has roundly keeled whorls. The sinus, which is
rather deep and U—shaped, is conﬁned to the shoulder
above the keel. Powell (1966, p. 74) says that the typical
adult has medially carinate whorls but is otherwise
smooth except for some weak, oblique, peripheral nodes
on the early postnuclear whorls.

The known fossil occurrences of Spirotropis are in the
Miocene to Pleistocene of Europe and the Oligocene to
Pleistocene of northwestern America (Powell, 1966,
p. 75).

Spirotropis kincaidi (Weaver)
Plate 7, ﬁgures 1, 9, 10, 13
Turris kincaidi Weaver, 1916a, Washington Univ. (Seattle) Pubs.
Geology, v. 1, p. 53, pl. 5, ﬁg. 67.

 
Turricula kincaidi (Weaver). Tegland, 1933, California Univ. Pubs.
Dept. Geology, v. 23, p. 126—127, pl. 10, ﬁgs. 12, 13.

Spirotropis kincaidi (Weaver). Grant and Gale, 1931, San Diego Soc.
Nat. Hist. Mem., v. 1, p. 548. Weaver, 1942, Washington Univ.
(Seattle) Pubs. Geology, v. 5, p. 522, pl. 97, ﬁgs. 18, 19, 25.

Spirotropis kincaidi is small to moderate in size and
bears a sharply rounded keel or shoulder just above the
suture. The whorls of the spire are smooth above the
keel except for the U-shaped sinus and three ﬂat-topped
spiral cords below the keel. The body whorl is sculptured
with similar ﬁat spiral cords below the keel which are
closely spaced. No nodes are discernible on any of the
specimens examined, nor are they present on the
holotype. The protoconch consists of two smooth whorls
with the apex slightly arcuate and recurved.

Holotype.—CAS 470.

Type locality.—UW 256. In Union Paciﬁc Railway cut
1 mile north of Galvin Station, Lewis County, Wash.
Lincoln Creek Formation (late Eocene to early
Miocene).

Hickman (written commun., 1975) assigns Spirot-
ropis kincaidi to the genus Parasyrinx.

Spirotropis kincaidi has a shorter, wider spire and a
more sharply rounded keel than S. washingtonensis
Etherington (1931, p. 113, pl. 14, ﬁgs. 8, 22, 34).

Localities.—USGS 15264, 15310, 15310d, 15588,
M3856, M3857, M3871, M3872, M3878.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene) and Blakeley(?) Forma-
tion (late Oligocene and early Miocene), Washington;
Tunnel Point Sandstone (middle Oligocene), Oregon.

Genus Suavodrillia. Dall

Suavodrillia Dall, 1918, US. Natl. Mus. Proc., v. 54, no. 2238, p. 331.

Type species.—By original designation, Drillia
kennicotti Dall, Holocene, Alaska. Bering Strait south
to the Aleutian Islands.

The known fossil occurrences of Suavodrillia are in
the Miocene and Pliocene of Japan and the Oligocene of
Washington and Oregon.

Some of the diagnostic features of Suavodrillia, as
given by Powell (1966, p. 82), are

Shell moderately large, up to 37 mm, rather thin, claviform, with a
tall pagodiform spire and a narrow body-whorl, quickly contracted to a
moderately long, decidedly twisted, and rather deeply notched an-
terior canal. Protoconch small, turbinate of 21/2 smooth whorls, the tip
almost central and slightly inrolled. Spire-whorls dominated by a
strong but narrowly rounded keel, which is situated at about a third
whorl height. Body-whorl and a second keel, emergent at the lower
suture, and seven more below to the anterior end, but becoming
progressively weaker. There is also a broad but weak subsutural fold
which bears two closely spaced ﬁne threads at its lower margin. The
shoulder slope is wide, ﬂat and steep, which with the carina, impart
the pagodalike proﬁle to the spire. Aperture ovate-pyriform. Outer lip
thin edged, with a moderately deep U-shaped sinus, at the apex of a
wide, chevron-shaped entrance; the apex is on the lower part of the
shoulder slope, immediately above the carina. The inner lip is a
slightly excavated smooth callus with processes.

40 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Power cites Suavodrillia hertleini Durham (1944, p. I

182—183, pl. 14, ﬁg. 1) from the Oligocene of Washington
as a characteristic species.
Suavodrillia winlockensis (Efﬁnger)

Plate 7, ﬁgures 4, 11, 12, 15, 33—36, 38
Surcula dickersoni (Weaver). Dickerson, 1917, California Acad. Sci.
Proc., ser. 4, V. 7, p. 161, pl. 31, ﬁgs. 3a, 3b.
Spirotropis (Spirotropis) winlockensis Efﬁnger, 1938, Jour. Paleon-
tology, v. 12, p. 386, pl. 46, ﬁgs. 12, 16. Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 520-521, pl. 97, ﬁgs. 5, 8, 9.

S uavodrillia winlockensis is a small thin-shelled
species with a high, slim, turreted spire. The aperture is
ovate, and the siphonal canal is moderately long, re-
curved, and notched. The primary sculpture consists of
one strong narrow keel at the shoulder, a strong con—
cavity just below the shoulder, and two strong rounded
spirals on this concavity. The posterior spiral is one half
as wide as the anterior one. The surface above the
shoulder has ﬁne slightly rounded spirals of unequal
width that are closely spaced. Below the shoulder on the
body whorl are three slightly rounded strong spirals
alternating with weaker spirals of half the width. The
remainder of the shell to the tip of the canal bears
ﬂat—topped spiral cords of lesser strength; these cords
alternate with incised lines. The sinus occupies most of
the shoulder and is shaped like a rounded, very open V.
The early whorls of some immature shells show a second
strong spiral just above the suture, and instead of being
concave are straight sided. Well-preserved juvenile
specimens may bear a ﬁne reticulate sculpture on the
shoulder; the sculpture is formed by ﬁne spiral threads
crossing the lines of the suture. The size and ar-
rangement of secondary spiral cords varies considerably
on different specimens. On a few specimens the keel is
grooved. The protoconch is small and smooth with the
tip almost central.

Holotype.—UCMP 33607.

Type locality—UW 239. South bank of the Cowlitz
River at old Gries Ranch, Lower Cowlitz Valley, Wash.
Gries Ranch Formation (early Oligocene).

Suavodrillia dickersoni (Weaver) (1916a, p. 54, pl. 5,
ﬁg. 66), from the Lincoln Creek Formation (late Eocene
to early Miocene), Washington, is not so strongly keeled
and seems to have a much shorter siphonal canal.

Localities.—USGS 15264, 15264b, e, 15310, 15310a,
c, e, f, h,j, 15499, 15530, 18638, 21612, M3871, M3878.

Occurrence elsewhere—Gries Ranch Formation
(early Oligocene), Washington.

Family PYRAMIDELLIDAE
Genus Odostomia Fleming
Odostomia Fleming, 1813, Brewster’s Edinburgh Encyclopedia, v. 7,

pt. 1, p. 76.

Type species.—By subsequent designation (Gray,
1847, Zool. Soc. London Proc., pt. 15, p. 159), Turbo

plicatus Montagu. Holocene, Europe.

 
Odostomia winlockiana Efﬁnger

Plate 3, ﬁgures 7, 9, 10
Odostomia (Odostomia) winlockiana Efﬁnger, 1938, Jour. Paleon-
tology, v. 12, p. 375, pl. 46, ﬁgs. 13, 17, 20. Weaver, 1942,
Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 306—307, pl. 64,
ﬁgs. 23, 24, 30.

Shell very small (2.5—4.5 mm high and 1.0—2.2 mm
wide), adult specimens probably have ﬁve whorls. The
surface is white and polished, and the protoconch
heterostrophic. A single fold can be seen on the col-
umella. The sutures are linear and impressed. The body
whorl is moderately large, and the aperture probably
subovate.

Holotype.—UCMP 33564.

Type locality—In south bank of Cowlitz River at old
Gries Ranch, N14 sec. 25, T. 11 N., R. 2 W., Cowlitz
County, Wash. Gries Ranch Formation, early
Oligocene.

The species is distinguished by the moderately
rounded whorls and impressed sutures. Odostomia may
be parasitic upon the mollusks Ostrea, Pecten, and C rep-
idula and on polychaete worms (Keen, 1971, p. 770).

Localities.——USGS 5329, 15310.

Occurrence elsewhere—Gries Ranch Formation
(early Oligocene), Washington.

Family ACTEONIDAE
GenusrAgteron Montfort
Acteon Montfort, 1810, Conchyliologie systématique, v. 2, p. 315.

Type species.—By original designation, Voluta
tornatilis Gmelin = Voluta tornatilis Linné. Holocene
seas of Europe.

Acteon chehalisensis (Weaver)
Plate 7, ﬁgures 20, 21

Acteocina chehalisensis Weaver, 1916a, Washington Univ. (Seattle)
Pubs. Geology, v. 1, p. 55, pl. 4, ﬁgs. 55, 56.

Acteon chehalisensis (Weaver). Weaver, 1942, Washington Univ.
(Seattle) Pubs. Geology, v. 5, p. 543, pl. 99, ﬁgs. 38—40.

Three incomplete specimens are in the collections
examined. The body whorl is large and somewhat
elongate, and the spire is moderately high and consists
of four whorls. The body whorl of the middle-sized
specimen bears about 30 spiral ribs. The body whorl of
the largest specimen has twice as many ribs; they each
seem to have split in two. The smallest specimen does
not have the outer shell layer preserved. Fine axial
threads occur in the spaces between spiral ribs. The
spirals are offset at irregular intervals on the largest
specimen.

Holotype.—CAS 474.

Type locality.—UW 352. In Union Paciﬁc Railway cut
1 mile north of Galvin Station, Lewis County, Wash.
Lincoln Creek Formation (late Eocene to early
Miocene).

Acteon parvuum Dickerson (1917, p. 172, pl. 29, ﬁgs.
12a, 12b) from the Gries Ranch Formation (early

CLASS SCAPHOPODA 41

Oligocene), Washington, has a more inﬂated body
whorl, lower spire, and only about 20 spiral ribs. Al-
though A. parvuum has been recorded from the
Pittsburg Bluff Formation (Warren and others, 1945), it
is not present in the collections studied.

Localities.—USGS 15264, 15537, 15588, M3871.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene), Washington.

Acteon? n. sp.?
Plate 7, ﬁgure 19

A small (4 mm high, incomplete; 2.7 mm wide) in-
complete, poorly preserved specimen of Acteon? is in the
collections. It is unique in that the shell is not com-
pletely sculptured by spiral ribs or incised lines. The
smallest whorl on the shell has widely spaced spiral
lines. The next largest whorl is smooth except for one
incised line seen where the next whorl has broken away
at the suture. The upper third of the body whorl is
smooth; the lower two-thirds is sculptured with incised
lines except at the base where the sculpture is of ﬂat-
topped spiral ribs. The aperture is almost completely
missing, but the inner lip seems to be thickened, and the
general outline of the aperture is similar to that of
Acteon. As all the fossil species of Acteon seen have had
all the whorls spirally sculptured, it seems improbable
that this specimen is simply an immature form of Ac-
teon chehalisensis (Weaver) or of some other described
fossil species.

Locality.—USGS 15588.

Family SCAPHANDRIDAE
Genus Scaphander Montfort

Scaphander Montfort, 1810, Conchyliologie systématique, v. 2, p. 335.

Type species.—By original designation, Bulla lig-
naria Linné. Holocene, eastern North Atlantic to
Mediterranean Sea.

Scaphander stewarti Durham
Plate 7, ﬁgures 18, 23—32

Scaphander stewarti Durham, 1944, California Univ. Pubs, Dept.
Geol. Sci. Bull., v. 27, p. 189, pl. 14, ﬁg. 15. Hickman, 1969, Oregon
Univ. Mus. Nat. Hist. Bull. 16, p. 100—101, pl. 14, ﬁgs. 1—3.

Scaphander stewarti is of moderate size, thin shelled,
and subovate in outline. The spire is sunken and cov-
ered with callus that continues as a ridge on the pos-
terior edge of the aperture to the outer lip edge. The
outer lip leaves the spire at an angle and ﬂares out
beyond the body whorl. The shell is so thin that the
outer lip is usually broken off; it is not completely
preserved on any of the specimens in the collections
examined. The shell is sculptured with ﬂat spiral ribs
that are grooved medially on the posterior portion of the
shell and are split into two ribs on the anterior portion.
The ribs are of unequal width and are serrated along the
edges.

Holotype.—UCMP 35483.

 
Type locality—In seacliff SWIANElA sec. 19, T. 29 N.,
R. 1 E., Nordland quadrangle, Jefferson County,
Wash.Quimper Sandstone of Durham (1942) (early and
middle Oligocene).

Scaphander stewarti differs from Scaphander
washingtonensis Weaver (1916a, p. 56, pl. 5, ﬁg. 68) by
having the lip more roundly truncated at the anterior
end. The aperture is more inﬂated anteriorly, and the
outer lip leaves the spire at an upward angle.

Localities.—USGS 2714, 5407, 15264, 15264b, e,
15310, 15310a, b, d, j, 15312, 15537, 15545, 15583,
15586, 15588, 18638, 21612, M3858, M3868, M3871,
M3872, M3878.

Occurrence elsewhere.—Quimper Sandstone of
Durham (1942) (early and middle Oligocene),
Washington; Gries Ranch Formation (early Oligocene),
Keasey Formation (late Eocene and early Oligocene),
and Eugene Formation (early and middle Oligocene),
Oregon.

Class SCAPHOPODA
Family DEN TALIIDAE
Genus Dentalium Linné
Dentalium Linné, 1758, Systema naturae, ed. 10, p. 785.

Type species.——By subsequent designation (Montfort,
1810), Dentalium elephantinum Linné. Holocene,
Amboynaland, Philippine Islands.

Subg‘enus Fissidentalium Fischer

Type species.~—By monotypy (Fischer, 1885, Manuel
de Conchyliologie, p. 894), Dentalium ergasticum
Fischer. Living in Gulf of Gascony and the Atlantic
Ocean ranging in water depth from 400 to 1,900 m.

Dentalium (Fissidentalium?) laneensis Hickman
Plate 7, ﬁgures 14, 17

Dentalium (F issidentalium? ) laneensis Hickman, 1969, Oregon Univ.
Mus. Nat. Hist. Bull. 16, p. 74, pl. 9, ﬁgs. 1—6.

About 30 specimens of Dentalium are in the Pittsburg
Bluff collections; of these about 10 have some of the
original shell preserved, although none of them are
complete specimens. The longitudinal ribs are narrow,
strong, and rounded near the apex. Secondary ribs may
appear between 8 and 10 mm from the apex where the
primary ribs become less pronounced. The primary ribs
become broader and ﬂatter nearer the middle of the
shell, and may be completely absent near the aperture
so that the shell is smooth. Wear and exfoliation make
speciﬁc identiﬁcation of most of the specimens impos-
sible, but I think that all the specimens represent one
species. The shell is moderately curved near the apex;
the remainder of it is straight or nearly so.

Holotype.—UO 27332.

Type locality.—UO 2538. In roadcut, 30th Ave. and
Agate St., Eugene, Oreg. NWM; sec. 8, T. 18 S., R. 3 W.
Eugene quadrangle, Eugene Formation (early and
middle Oligocene).

42 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

The longitudinal sculpture distinguishes Dentalium
laneensis from other described species of the west coast
Tertiary.

Localities.—USGS 2723, 15264, 15278, 15310,
15310g, 15530, 15588, M3856, M3858, M3871, M3872.

Occurrence elsewhere—Eugene Formation (early
and middle Oligocene), Oregon; Wygal Sandstone
Member of the Temblor Formation (late Oligocene),
California.

Class PELECYPODA
Family NUCULEDAE
Genus Nucula. Lamarck
Nucula Lamarck. 1799, Soc. Hist. Nat. Paris Mem., ser. 1, p. 87.

Type species.—By monotypy, Arca nuculeus Linné.
Holocene, France.

Subgenus Leionucula Quenstedt

Leionucula Quenstedt, 1930, Geol. und Paléiont. Abhand., Bd. 22, Heft
1, p. 112.

Type species.—By original designation, Nucula al-

bensis d’ Orbigny. Cretaceous, England and France.
Nucula. (Leionucula) vokesi, n. sp.
Plate 8, ﬁgures 10, 13, 16, 17

N ucula vokesi is a small species (5.2 to 7.3 mm long
and 3.7 to 6.3 mm high) with a smooth shell sculptured
only with concentric grooves. The shell is longer than
high and moderately inﬂated, and it has a well-deﬁned,
elongate, heart-shaped escutcheon. The shell is pro-
duced along the posterior margin and bears a faint sul—
cus parallel to the anterior dorsal margin; the sulcus is
about 1 mm from the margin. The poorly preserved
hinge of one right valve (pl. 8, ﬁg. 17) shows 8 or 9 teeth
preserved in the posterior series (the teeth stop at the
edge of the resilifer); and 9 teeth or more preserved in
the anterior series (the teeth continue above the re-
silifer to the beak). A left valve, also poorly preserved,
shows 5 or 6 teeth in the anterior series and perhaps
about 15 teeth in the posterior series that continue
above the resilifer to the beak (pl. 8, ﬁg. 16). The inner
ventral margin has not been exposed.

Holotype.—Herewith designated USNM 214074 (pl.
8, ﬁg. 10).

Type locality.—USGS 18638. Type area of the
Pittsburg Bluff Formation (middle Oligocene), Oregon.

The holotype is a small right valve 6.5 mm long and
4.7 mm high; the hinge is not exposed.

The resilifer is longer, and the shell is less inﬂated
and lacks the bunched concentric threads that
characterize Nucula (Leionucula) nuculana (Dall)
(Dall, 1909, p. 125—126, pl. 18, ﬁg. 2; Moore, 1963, p.
52-53, pl. 11, ﬁgs. 2, 5, 10; pl. 12, ﬁg. 1). Nucula han—
niballi Clark (1925, p. 73—74, pl. 8, ﬁg. 2), a species that
occurs in the Blakeley Formation of Weaver (1912) (late
Oligocene and early Miocene), has radial sculpture. N.

 
(Leionucula) vokesi is rare in the Pittsburg Bluff
Formation.

Localities.—USGS 2714,15264,15310, 15536, 15586,
15588, 18638.

Genus Acila. Adams and Adams

Acila Adams and Adams, 1858, Genera of Recent Mollusca, v. 2, p.
545.

Type species.—By subsequent designation (Stoliczka,
1871, India Geol. Survey Mem. Palaeontologia Indica,
V. 3, p. 325),Nuc ula divaricata Hinds. Holocene, Korea.

Subgenus Truncacila. Schenck

Truncacila Schenck, 1931, in Grant and Gale, San Diego Soc. Nat.
Hist. Mem., v. 1, p. 115.

Type species.—By original designation, Nucula
castrensis Hinds, Holocene, Sitka, Alaska, to San Diego,
Calif.

Truncacila originated in the Cretaceous. It prefers a
cool temperate habitat and depths of 5—500 fathoms
(10—914 In) (Schenck, 1936, p. 33—35). Truncacila had its
greatest development in the Oligocene (Schenck, 1936,
p. 38). It is one of the most common fossils in the
Pittsburg Bluff Formation.

Slodkewitsch (1967, p. 64) proposed Lacia, a new
subgenus of Acila, with N ucula (Acila) shumardi Dall
as the type species. No diagnostic features were given
that validly separate the subgenus Lacia from Trun-
cacila and the subgenus Truncacila is here retained.

Acila (Truncacila) shumardi (Dall)
Plate 8, ﬁgures 1—9, 11, 12, 14, 15, 18

Nucula (Acila) decisa Conrad. Dall, 1898, Wagner Free Inst. Sci.
Trans, v. 3, pt. 4, p. 573. Dall, 1900, Wagner Free Inst. Sci. Trans, v.
3, pt. 5, pl. 40, ﬁgs. 1, 3. Not Nucula decisa Conrad in Blake, 1855,
Paciﬁc R.R. Survey, v. 5, p. 322, pl. 3, ﬁg. 19.

Nucula (Acila) shumardi Ball, 1909, U.E. Geol. Survey Prof. Paper 59,
p. 103. Clark, 1925, California Univ. Pubs., Dept. Geol. Sci. Bull., v.
15, no. 4, p. 75, pl. 8, ﬁg. 11. Tegland, 1933, California Univ. Pubs.,
Dept. Geol. Sci. Bull., V. 23, no. 3, p. 107, pl. 5, ﬁg. 10.

Acila shumardi Dall. Weaver, 1916a, Washington Univ. (Seattle)
Pubs. Geology, v. 1, no. 1, pl. 3, ﬁg. 43. Clark, 1918, California Univ.
Dept. Geology Bull., v. 11, no. 2, p. 95, 121—122, pl. 13, ﬁgs. 7, 8, 17.
Schenck and Keen, 1940, California fossils, pl. 28, ﬁg. 2.

Acila (Truncacila) shumardi (Dall). Schenck, 1936, Geol. Soc.
America Spec. Paper 4, p. 64—67, pl. 4, ﬁgs. 5—7, 9; pl. 6, ﬁgs. 1—11,
text ﬁg. 7 (18). Weaver, 1942, Washington Univ. (Seattle) Pubs.
Geology, v. 5, p. 25—26, pl. 7, ﬁgs. 5—7, 11; pl. 8, ﬁgs. 2, 5 [1943].
Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 26—27, pl.
1, ﬁgs. 6, 7, 10.

Acila shumardi is large to moderate in size (largest
specimen: 30 mm long, 22 mm high, and 16 mm thick),
and is sculptured with many narrow ribs separated by
small spaces which on some specimens are barely
discernible and could be described as incised lines.
Secondary bifurcation of the ribs may be present at the
ventral margin either in the midportion of the anterior
half of the shell or along the anterior side of the primary
bifurcation. On one specimen (USGS 18681) the ribs

CLASS PELECYPODA 43

split near the dorsal margin on the anterior portions of
both valves of an articulated specimen. Although areas
of secondary bifurcation, if present, usually occur on the
largest specimens, such bifurcation has also been seen
on specimens of only small to moderate size. The beaks
are located at the sharply truncated posterior margin.
The hinges exposed on two left valves (pl. 8, ﬁgs. 4, 8)
show 7—10 posterior teeth and 16—22 anterior teeth. The
hinges exposed on six right valves (pl. 8, ﬁgs. 6, 9, 11, 12,
15, 18) show 7—11 posterior teeth and 17—20 anterior
teeth. One specimen (pl. 8, ﬁg. 18), at the anterior end of
the posterior series of teeth, shows a deep irregular
socket with an irregular toothlike projection at the
ventral anterior edge. The number of teeth varies with
the size of the individual shell, and the larger specimens
have more teeth than the smaller ones.

Holotype.—USNM 406405 (pl. 8, ﬁgs. 5, 6), ﬁgured by
Ball (1900, pl. 40, ﬁgs. 1, 3). This specimen was
erroneously cited as USNM 406505 by Weaver (1942, p.
26) and Schenck (1936, p. 64).

Paratypes.—USNM 107402, four specimens.

Type locality—USGS 2714, sec. 23, T. 5 N., R. 4 W.,
Vernonia quadrangle, Pittsburg, Columbia County,
Oreg. Pittsburg Bluff Formation, middle Oligocene.

The holotype is a right valve with the hinge exposed;
the paratypes are articulated double valves and one
specimen is an internal mold. A topotype from Dall’s
original collection is ﬁgured on plate 8, ﬁgures 2, 3, 7.

The sculpture of closely spaced ribs with narrow
interstices, the size of average specimens, and the
posterior truncation distinguish A. shumardi from
other species of Acila (Truncacila).

The Acila zones of Schenck (1936, p. 41—44), like
many biozones deﬁned by single species, are not so
restricted in time as some scientists supposed. Acila
(Truncacila) nehalemensis (G. D. Hanna) has been
collected from the Eugene Formation (early and middle
Oligocene) by Hickman (1969, p. 24—25), whereas it was
considered a guide fossil to beds of Keasey age (late
Eocene and early Oligocene) by Schenck (1936, p. 42—44,
60—63).Acila (Acila) gettysburgensis (Reagan) occurs in
beds of Blakeley age (late Oligocene and early Miocene)
as well as in the Astoria Formation (Miocene), as noted
by Howe (1922, p. 58), Schenck (1936, p. 80), and Moore
(1963, p. 54). Acila shumardi is found in the Gries
Ranch Formation of early Oligocene age, and in the
Oligocene portion of the Poul Creek Formation of
middle Oligocene to early Miocene age in Alaska. Acila
shumardi therefore ranges from early through middle
Oligocene. The genus Acila is very useful for dating
because of its abundance, good preservation, distin-
guishing characters, and ease of collection. If its
presence is used with descretion along with the presence

 
of other species in a fauna, it is a valuable tool.

Localities.—USGS 2415, 2707, 2714, 2715, 2721,
5394, 15264, 15264a, b, e, 15310, 15310a—c, e—h, 15311,
15312, 15530, 15586, 115588, 18638, 18779, M3856,
M3857, M3860, M3871, M3872, M3877, M3878.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Yakataga and Katalla
Districts, Gulf of Alaska, and Stepovak Formation of
Burk (1965) (early and middle Oligocene), Alaska
Peninsula; Lincoln Creek Formation (late Eocene to
early Miocene), Washington; Gries Ranch Formation
(early Oligocene), USGS 5210, 15298, 15585, Eugene
Formation (early and middle Oligocene), upper part
only, Alsea Formation (early, middle, and late
Oligocene), Tunnel Point Sandstone (middle
Oligocene), Oregon; Tumey (early and middle
Oligocene), Alegria (middle Oligocene), Kirker (middle
Oligocene), and upper San Emigdio (late Eocene to
middle Oligocene), Formations, California.

Family NU CULANDDAE
Genus Litorhaxlia Stewart

Litorhadia Stewart, 1930, Acad. Nat. Sci. Philadelphia Spec. Pub. 3, p.
52—53.

Type species.—By original designation, Leda acala
Dall (1898, Wagner Free Inst. Sci. Trans., pt. 4, p. 586,
pl. 32, ﬁg. 3). Eocene, Wood’s Bluff, Ala.

Litorhadia washing’tonensis (Weaver)
Plate 9, ﬁgures 1—10, 12

Leda washingtonensis Weaver, 1916a, Washington Univ. (Seattle)
Pubs. Geology, v. 1, p. 34—35, pl. 3, ﬁgs. 25, 26.

Nuculana washingtonensis (Weaver). Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 38-39, pl. 8, ﬁgs. 18, 20, 26.
Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p.27, 30, pl.
1, ﬁgs. 8, 11.

Leda Zincolnensis Weaver, 1916a, Washington Univ. (Seattle) Pubs.
Geology, v. 1, p. 35, pl. 3, ﬁgs. 23, 24.

Litorhadia washingtonensis in the collections
examined attains a maximum length of 29 mm,
although it is usually a small form. It is sculptured with
concentric ridges. The posterior dorsal margin is
markedly concave, and the shell is produced, turning
outward, along the margin of the escutcheon. The
posterior end is truncated and pointed, and the anterior
margin is evenly rounded. The beaks are slightly
anterior to the midpoint of the shell. The right valve has
20 posterior and 26 anterior teeth; the left valve has 24
anterior and 18 posterior teeth, as counted on the two
available exposed hinges. The chondrophore is long,
shallow, moderately impressed, and symmetrical.

Lectotype.—CAS 451 is herewith selected as the
lectotype. It is one of the two specimens cited by Weaver
(1942, p. 39) as syntypes.

Type locality.—In Union Paciﬁc Railway cut, 1%; mile
northwest of Galvin Station, in sec. 27, T. 15 N., R. 3 W.,

44 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Malone quadrangle, Washington. Lincoln Creek For—
mation (late Eocene to early Miocene).

The lectotype (Weaver, 1942, pl. 8, ﬁgs. 18, 20) is a left
valve with the hinge exposed and the exterior of the
shell showing the concentric ridges. The shell is worn at
the posterior extremity and seems to be square, whereas
it was originally pointed.

Closely related forms are found in the Poul Creek
(middle Oligocene to early Miocene) Formation,
Yakataga District, Gulf of Alaska, and possibly in the
upper Kreyenhagen Shale or Tumey Formation,
California.

Localities.—USGS 2714, 5394, 15264, 15264a—c, e,
15278,15310,15310a,g,j,15312,15519,15530,15532,
15537, 15545, 15548, 15583, 15586, 15588, 18638, cf.
M3857, M3867, M3868, cf. M3869, M3871, M3872,
M3878.

Occurrence elsewhere.—Gries Ranch Formation
(early Oligocene), Lincoln Creek Formation (late
Eocene to early Miocene), Quimper Sandstone of
Durham (1942) (early and middle Oligocene), and
Blakeley Formation of Weaver (1912) (late Oligocene
and early Miocene), Washington; Eugene Formation
(early and middle Oligocene), Alsea Formation (early to
late Oligocene), and Tunnel Point Sandstone (middle
Oligocene); upper part of Brabb’s (1960) Rices Mudstone
Member of the San Lorenzo Formation (early Oligocene
to early Miocene), California.

Genus Yoldia Méller
Yoldia Méller, 1842, Index molluscorum Groenlandiae, p. 18.

Type species.——By subsequent designation (Verrill
and Bush, 1898, U.S. Natl. Mus. Proc., V. 20, no. 1139, p.
858), Yoldia arctica (Gray) = Y.hyperborea (Gould).
Holocene, northern seas of Europe.

Subgenus Kalayoldia Grant and Gale
Kalayoldia Grant and Gale, 1931, San Diego Soc. Nat. Hist. Mem., V.

1, p. 128.

Type species.—By original designation, Yoldia
cooperii Gabb. Miocene to Holocene, Paciﬁc coast of the
United States. Living from central California to
northern Lower California, Mexico (Hertlein and
Grant, 1972, p. 51).

Yoldia (Kalayoldia) oregona (Shumard)
Plate 9, ﬁgures 14, 16—18
Leda oregona Shumard, 1858, Acad. Sci. St. Louis Trans, v. 1, p.
121—122 (Reprinted in Dall, 1909, U.S. Geol. Survey Prof. Paper 59,
p. 187). Gabb, 1869, California Geol.Survey, Paleontology, V. 2, p.
121.
N uculana oregano (Shumard). Meek, 1864, Smithsonian Misc. Colln.
183, p. 5, 27. Conrad, 1866, Smithsonian Misc. Colln. 200, p. 3.
Neilo oregano (Shumard). Conrad, 1865, Am. Jour. Conchology, V. 1, p.
153.

Yoldia (Cnestrium) oregona (Shumard). Dall, 1909, U.S. Geol. Survey
Prof. Paper 59, p. 105, pl. 19, ﬁg. 4. Not Yoldia (Cnestrium) oregona
(Shumard) of Dall, 1922, Am. Jour. Sci., ser. 5, V. 4, p. 310, nor

 
Yoldia oregona (Shumard) of Etherington, 1931, California Univ.
Pubs, Dept. Geol. Sci. Bull., V. 20, p. 67, pl. 1, ﬁg. 8.

Yoldia (Portlandia) oregona (Shumard). Weaver, 1942, (in part),
Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 49, pl. 9, ﬁg. 16;
not pl. 9, ﬁg. 8.

Yoldia (Kalayoldia) oregona (Shumard). Grant and Gale, 1931, San
Diego Soc. Nat. Hist. Mem., V. 1, p. 130. Trumbull, 1958, Jour.
Paleontology, v.32, no. 5, p. 900—901, pl. 115, ﬁgs. 2, 3. Moore, 1963,
U.S. Geol. Survey Prof. Paper 419, p. 58, pl. 12, ﬁg. 20. Hickman,
1969, Oregon Mus. Nat. Hist. Bull. 16, p. 31—32, pl. 1, ﬁgs. 14, 15.

?Yoldia tenuissima Clark, 1918, California Univ. Pubs. Dept. Geol.
Sci. Bull., V. 11, p. 125—126, pl. 11, ﬁg. 10; pl. 12, ﬁgs. 8, 14.

Yoldia oregona is moderate to large in size and is
sculptured with concentric lines. The umbos are located
medially or slightly anterior to the midline. The
anterior end is evenly rounded, and the posterior end is
recurved and sharply attenuated. The lectotype has
about 20 teeth on the concave hinge line and about 25
teeth on the convex hinge line.

Lectotype.—USNM 562470 (designated by Trumbull,
1958, p. 900).

Type locality—A few miles south of Oregon City,
Oreg. (Oligocene).

Yoldia tenuissima Clark (1918, p. 125—126, pl. 11, ﬁg.
10; pl. 12, ﬁgs. 8, 14) is perhaps conspeciﬁc with Y.
oregona. The poorly preserved holotype of Y. tenuissima
seems to have a sloping anterior dorsal margin, rather
than the almost straight margin of Y. oregona, but this
is not true of a specimen subsequently ﬁgured by
Clark(1925, pl. 8, ﬁg. 5) as Y. tenuissima. Clark (1918, p.
126) differentiates the two species on the basis that Y.
tenuissima has more posterior beaks, a somewhat more
attenuate posterior end, and fewer teeth on the
posterior margin.

Localities.—USGS 2714, 2722, 15264, 15264e, 15310,
15310b, f, 15312, 15499, 15516, 15586.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene), Washington; Eugene
Formation (early and middle Oligocene), Oregon.

Family MYTILIDAE
Genus Mytilus Linné

Mytilus Linné, 1758, Systema naturae, ed. 10, p. 704.

Type species.—By subsequent designation (Anton,
1839, Verzeichniss der conchylien welche sich in der
Sammlung von H. E. Anton beﬁnden, p. 17), Mytilus
edulis Linné. Miocene to Holocene; living, cosmopolitan
except in extreme tropical water (Hertlein and Grant,
1972, p. 163).

Mytilus cf. Mi. snohomishensis Weaver

Two small, incomplete, and poorly preserved
specimens of Mytilus are in the collections. Owing to
the state of their preservation, they cannot be posi-
tively identiﬁed. They are compared to Mytilus
snohomishensis Weaver (1912, p. 59, pl. 13, ﬁg. 110), a
species that is found in the middle and upperOligocene

CLASS PELECYPODA 45

of Oregon and Washington and possibly also in the
lower Miocene. The two specimens have terminal beaks,
and the dorsal margin has a pronounced angle, possibly
atabout one-fourth to one-third the distance from the
beak. Only the internal shell layer is preserved; it is
smooth except at the ventral margin, where weak
longitudinal folds can be seen.

Localities.—USGS 2714, 15586.

Occurrence elsewhere—Of Mytilus snohomishensis:
Lincoln Creek Formation (late Eocene to early
Miocene), Blakeley (late Oligocene and early Miocene)
and Twin River Formations (late Eocene to late
Oligocene), Washington; Eugene Formation (early and
middle Oligocene), Oregon.

Subfamily CRENELLINAE
Genus Crenella Brown

Crenella Brown, 1827, Illus. Conchology, Great Britain, v. 1, pl. 31,
ﬁgs. 12—14; 1844, ed. 2, p. 75, pl. 23, ﬁgs. 12—14.

Type species.—By monotypy, Mytilus decussatus
Montagu. Holocene, northern Norway.

Crenella porterensis Weaver
Plate 12, ﬁgure 12

Crenellaporterensis Weaver, 1912, Washington Geol. Survey Bull. 15,
pl. 14, ﬁg. 116, Weaver, 1916a, Washington Univ. (Seattle) Pubs.
Geology, v. 1, p. 36—37, pl. 3, ﬁgs. 41, 42. Tegland, 1933, California
Univ. Pubs, Dept. Geol. Sci. Bull., v. 23, p. 112, pl. 6, ﬁg. 2.

This one specimen of Crenella porterensis is incom-
pletely exposed in rock. The preserved inner shell layers
show that some of the ribs bifurcate near the ventral
margin. The margin of the valves is crenulate. The shell
is moderately inﬂated, the inner shell layers are pearly,
and faint concentric lines are visible on one small por-
tion of the shell.

Holotype.—CAS 454A.

Type locality—In railroad cut on Union Paciﬁc
Railway 1 mile north of Galvin Station, Lewis County,
Wash., sec. 27, T. 15 N., R. 3 W., Centralia quadrangle.
Lincoln Creek Formation (late Eocene to early
Miocene).

C. porterensis is distinguished from Crenella
washingtonensis Weaver (1916a, p. 37, pl. 3, ﬁg. 40)
from the Lincoln Creek Formation by its larger size and
its strong radial sculpture.

Locality.—USGS 15583.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Katalla District, Gulf
of Alaska; Lincoln Creek Formation (late Eocene to
early Miocene) and Blakeley Formation of Weaver
(1912) (late Oligocene and early Miocene), Washington;
Keasey Formation (late Eocene and early Oligocene),
Alsea Formation (early to late Oligocene), and possibly
in the Astoria Formation (Miocene), Oregon.

Family CARDITIDAE

 
Subfamily CARDITAMERINAE
Genus Cyclocardia. Conrad

Cyclocardia Conrad, 1867, Am. Jour. Conchology, v. 3, p. 191.

Type species.—By subsequent designation (Stoliczka,
1871, India Geol. Survey Mem. Palaeontologia Indica,
v. 3, XX, p. 281), Cardita borealis Conrad, Holocene,
eastern United States, Labrador to Cape Hatteras.

Cyclocardia (Cyclocardia) of. C (C.) hannibali (Clark)

Plate 9, ﬁgures 11, 13, 15

Cyclocardia cf. C. hannibali is a rather small carditid,
subcircular in outline. It has approximately 16 to 21
rounded, slightly nodose ribs. The nodes seem to be
formed by the bunching of the concentric threads that
sculpture the entire shell. A rubber impression of the
hinge of a left valve (pl. 9, ﬁg. 15) shows the anterior
cardinal tooth to be rather small, somewhat trigonal,
and blunt. The socket posterior to this tooth shows that
the opposing cardinal tooth in the right valve was
straight on the anterior edge.

All the specimens of C. cf. C. hannibali are preserved
as molds from one locality. The rubber impressions of
these specimens show this species to be most closely
related to C. hannibali (Clark) (1925, p. 88, pl. 19, ﬁgs. 6,
7). If well preserved specimens were available, they
would probably prove to be conspeciﬁc.

Cyclocardia hannibali differs from C. hannai
(Tegland), from the Blakeley Formation of Weaver
(1912) (late Oligocene and early Miocene) of
Washington, by having many more ribs; the ribs are a
little thinner with wider interspaces but have similar
sculpture. C. hannabali is distinguished from C. sub-
tenta (Conrad), by narrower, higher, and more nodose
ribs. The beaks seem to be higher and the anterior end
more produced. C. hannibali occurs in the Astoria
Formation (Miocene) of Washington and Oregon.

Locality.—USGS 15537.

Occurrence elsewhere—Of C. hannibali: Ushikubi-
toga Formation (Oliogocene), Japan (Kanno, 1960);
Poul Creek Formation (middle Oligocene to early
Miocene), Alaska; Blakeley Formation (late Oligocene
and early Miocene), Washington.

Family LUCINIDAE
Subfamily MYRTEINAE
Genus Lucinoma Dall
Lucinoma Dall, 1901, US. Natl. Mus. Proc, v. 23, p. 806.

Type species.—By original designation, Lucina ﬁlosa
Stimpson, Holocene, Grand Banks, off southeastern
Canada, and northwestern United States, to Gulf of
Mexico.

Lucinoma columbiana. (Clark and Arnold)
Plate 10, ﬁgures 1—8

Phacoides columbianum Clark and Arnold, 1923, California Univ.
Pubs, Dept. Geol. Sci. Bull., v. 14, p. 144—145, pl. 25, ﬁgs. 2a, 2b.

46 OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Clark, 1925, California Univ. Pubs, Dept. Geol. Sci. Bull., V. 15, p.
89, pl. 22, ﬁg. 9.

Lucina columbiana (Clark and Arnold). Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 145—146, pl. 34, ﬁgs. 13—15, 17.

Lucinoma columbiana is small to moderate in size.
Both valves of the largest ﬁgured specimen are 21.2 mm
long, 20.0 mm high, and 11.6 mm thick, but one poorly
preserved specimen was at least 32 mm long. L. col-
umbiana is inﬂated, subquadrate in outline with the
beaks rather high, and situated anterior to the middle of
the shell. L. columbiana bears closely spaced, raised
concentric lamellae, and on one specimen (pl. 10, ﬁgs. 3,
7) the lamellae are more closely spaced toward the
ventral margin. The anterior dorsal margin is concave,
joining smoothly the rounded anterior end; the posterior
dorsal margin is slightly convex, and it abruptly joins
the somewhat truncated posterior end. The hinges il-
lustrated (pl. 10, ﬁgs. 2, 6) are of a specimen that was
articulated but the cardinal teeth were apparently
destroyed when the valves were opened. The two valves
are illustrated to show the muscle scars and the outline
of the hinge. Of note are the large, heavy, seemingly ﬂat
areas posterior to the beaks on both valves, and the
small node on both valves at the anterior end of the
hinge. The ligament is mineralized at the dorsal edge of
the posterior part of the hinges. The escutcheon is long
and narrow. The lunule is moderate sized, impressed,
and inequilateral, and the portion on the right valve is
larger than that on the left.

Holotype.—CAS 593.

Type locality—From sandstone and conglomerate of
the Sooke Formation (early Miocene?) in the sea cliffs
between the mouths of Muir and Kirby Creeks, west of
Otter Point, Sooke Bay, Vancouver Island, BC.

The Holocene species Lucinoma annulata (Reeve) is
less inﬂated thanL. columbiana in proportion to its size,
it does not have the heavy posterior hinge plate, and it
has a smaller equilateral lunule. Lucinoma acutilineata
(Conrad) (1849, p. 725, pl. 18, ﬁgs. 2, 2a, 2b; Moore, 1963,
p. 70-71, pl. 15, ﬁgs. 7—10, 12), an early to middle
Miocene species, is thinner than L. columbiana in
proportion to its size; it has a much wider escutcheon,
and it lacks the heavy ﬂat posterior hinge plate.
Lucinoma hannibali (Clark) (1925, p. 89, pl. 22, ﬁgs. 2,
4) from Weaver’s (1912) Blakeley Formation (late
Oligocene and early Miocene) in Washington has a
wider escutcheon and less concave dorsal margin than
L. columbiana.

Clark (1932) reportsLucinoma cf.L. columbiana from
the Poul Creek Formation (middle Oligocene to early
Miocene), Alaska.

Localities.—USGS 15264, 15588, M3858.

Occurrence elsewhere.—Ushikubitoga Formation
(Oligocene), Japan (Kanno, 1960); Sooke Formation
(early Miocene?), Vancouver Island, BC; Blakeley

 
Formation (late Oligocene and early Miocene),
Washington. Possibly in the Eugene Formation (early
and middle Oligocene), the Alsea Formation (early to
late Oligocene), and the Tunnel Point Sandstone (mid-
dle Oligocene), Oregon.

Family UNGULINIDAE
Genus Felaniella. Dall
Felaniella Dall, 1899, Jour. Conchology, v. 9, no. 8, p. 244.

Type species—By original designation, Mysia
(Felania) usta Gould, Holocene, Japan.

Felaniella can be distinguished externally from
Diplodonta by its less prominent, centrally positioned
beaks, its subquadrate outline, and its lesser inﬂation.
Taras goodspeedi Durham and Diplodonta parilis
(Conrad) probably belong in the genus Felaniella.
Durham (1944, p. 145) pointed out the resemblance of T.
goodspeedi to the Holocene species T. sericata, which is
now assigned to Felaniella (Keen, 1958, p. 103).

Felaniella. (Felaniella) snavelyi, n. sp.
Plate 10, ﬁgures 9—11

Felaniella snavelyi is subquadrangular, inequilater-
al, and thin-shelled; it bears the ligament in a marginal
groove. The beaks are small and situated about one-
third the distance from the anterior margin. The
posterior dorsal margin slopes away from the beaks in a
straight line at an angle of about 20°, and joins the
rounded posterior margin abruptly; the anterior dorsal
margin is shorter and a bit more rounded. One right
valve has the hinge exposed (pl. 10, ﬁg. 10) showing two
cardinal teeth. The anterior tooth is moderately thick
and subvertical; the posterior tooth is thick, biﬁd, and
oblique. The pallial line seems to be doubled.

Holotype.——Herewith designated as USNM 214099,
plate 10, ﬁg. 10.

Type locality.—USGS 15264. On east side of Oregon
State Highway 47, approximately 600 feet north of
junction of Highway 47 and Scappoose-Vernonia Road
(3,500 ft south of grid 2,660 and 5,000 ft west of grid 820,
Army Engineers Vernonia quadrangle), Columbia
County, Oreg. Pittsburg Bluff Formation (middle
Oligocene).

In external characters F elaniella snavelyi is identical
to the living species F. serricata (Reeve). The shell of
F. snavelyi is thicker, however, and the conﬁguration of
the nymph plate and ligament groove are different. The
nymph plate of F. snavelyi is larger, heavier, and
ﬂanged along the dorsal margin, and it lacks the
ﬂattened, shallow trigonal pit that holds the resilium on
F. serricata. The ligament groove and ligament are
larger on F. snavelyi than on F. serricata.

F elaniella goodspeedi Durham (1944, p. 145) is more
rounded at the anterior and posterior margins, has a
higher angle between the beak and the posterior and

CLASS PELECYPODA 47

anterior dorsal margins, and has more prominent beaks
than F. snavelyi. Felaniella parilis (Conrad) (1848, p.
432; Moore, 1963, p. 71, pl. 23, ﬁg. 9) has a more rounded
anterior and posterior margin and a higher angle
between the beak and the posterior and anterior dorsal
margins like Felaniella griesensis (Efﬁnger) (1938, p.
369).

F. snavelyi is rare in the Pittsburg Bluff Formation.
Most of the complete specimens preserved have the
mineralized ligament intact.

Localities.—USGS 2714, 15264, 15310, 15312, 15516,
15537, 15544, 15586, M3858, M3871.

Family CARDIIDAE
Subfamily PROTOCARDIINAE
Genus Nemocardium Meek
Nemocardium Meek, 1876, U.S. Geol. Survey Territories, v. 9, p.

167—168.

Type species.—By subsequent designation (Sacco,
1899, I. Moll. Liguria, pt. 27, p. 56), Cardium
semiasperum Deshayes. Eocene, France.

Subgenus Keenaea Habe

Keenaea Habe, 1951, Genera of Japanese Shells: Pelecypoda, no. 2, p.
152.
Type species—By original designation, Nemocar-
dium samarangae Makiyama. Holocene, Japan.
Nemocardium (Keenaea) lorenzanum (Arnold)
Plate 10, ﬁgures 12—14

Cardium cooperii Gabb var. lorenzanum Arnold, 1908, U.S. Natl.
Mus. Proc., v. 34, p. 366, pl. 33, ﬁg. 6; 1909, U.S. Geol. Survey Geol.
Atlas, Santa Cruz Folio, p. 4, ﬁg. 17.

Cardium lorenzanum Arnold. Tegland, 1933, California Univ. Pubs.,
Dept. Geol. Sci. Bull., v. 23, p. 116—117, pl. 7, ﬁgs. 16, 17.

Nemocardium lorenzanum (Arnold). Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 160, pl. 35, ﬁg. 22, pl. 36, ﬁgs.
3, 5.

Nemocardium (Keenaea) lorenzanum (Arnold). Keen, 1954, Am.
Paleontology Bu11., v. 35, no. 153, p. 11. Hickman, 1969, Oregon
Univ. Mus. Nat. Hist. Bull. 16, p. 38, pl. 2, ﬁg. 7.

Nemocardium lorenzanum is a small form in the
Pittsburg Bluff Formation; the length of the largest
specimen in the collections is 18. 3 mm, but most of the
specimens are about 10 mmm long. N. lorenzanum is
subquadrate in outline, is moderately inﬂated, and has
prominent beaks. The hinge is not exposed. The shell is
very thin. The well-developed posterior ridge demar-
cates the change in ribbing: the anterior portion bears
ﬂat small radial ribs separated by ﬁnely incised lines;
the posterior portion bears narrow high ribs that are
separated by interspaces almost as wide that bear a
secondary concentric sculpture. This concentric
sculpture is between the ribs and at right angles to
them, and it consists of raised, thin, ridgelike inter-
calations that are evenly spaced but commonly not
alined.

Holotype.—USNM 165444.

 
Type locality—In cliff in north bank of Chehalis
River, at the town of Porter, Grays Harbor County,
Wash. In sec. 22, T. 17 N., R. 4 W., Malone quadrangle.
Lincoln Creek Formation (late Eocene to early
Miocene).

This species is distinguished by its \subquadrate
outline and by its sculpture of more than 60 ﬂat-topped
ribs anterior to the posterior ridge and a few more than
25 narrow high ribs posterior to the posterior ridge.

Closely related forms occur in the Poul Creek For-
mation (middle Oligocene to early Miocene), Yakataga
District, Gulf of Alaska, and in Burk’s (1965) Stepovak
Formation (early and middle Oligocene), McGinty Point
section, Alaska.

Localities.—USGS 15264, 15278, 15310, 15530,
15537, 15548, 18638, M3873.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene) and Weaver’s (1912)
Blakeley Formation (upper Oligocene and lower
Miocene), Washington; Eugene Formation (lower and
middle Oligocene), Alsea Formation (early, middle, and
late Oligocene), Keasey Formation (late Eocene and
early Oligocene), Oregon; upper part of Brabb’s (1960)
Rices Mudstone Member of San Lorenzo Formation
(late Eocene to middle Oligocene), California.

Family VENERIDAE
Subfamily PITARINAE
Genus Pitar Romer
Pitar Romer, 1857, Krit. Unters. Art. Moll., Venus, p. 15.
Type species.—By monotypy, Venus tumens Gmelin.
Holocene, West Africa.

Pitar (Pitar) dalli (Weaver)
Plate 12, ﬁgures 1, 2, 4

Pitaria dalli Weaver, 1916a, Washington Univ. (Seattle) Pubs.
Geology, v. 1, p. 41, pl. 1, ﬁgs. 1—4. Tegland, 1929, California Univ.
Pubs, Dept. Geol. Sci. Bull, v. 18, p. 278, pl. 21, ﬁgs. 4—9.

Pitar dalli (Weaver). Weaver, 1942, Washington Univ. (Seattle) Pubs.
Geology, v. 5, p. 181—182, pl. 43, ﬁgs. 1—5, 8, 11. Hickman, 1969,
Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 46—47, pl. 3, ﬁgs. 16—19, pl.
5, ﬁgs. 2, 5.

An internal mold of one almost complete large
specimen is subovate in outline and moderately
inﬂated. The few small internal molds are also subovate
in outline but are less inﬂated. On one of these molds,
the beaks are very close to the anterior margin; on all
the others, they are about a third of the distance from
the anterior end. One incomplete left hinge is ﬁgured
(pl. 12, ﬁg. 2).

Syntypes.—CAS 460A, 460C, 460D.

Type locality—In railroad cut on Union Paciﬁc
Railway 1 mile north of Galvin Station, Lewis County,
Wash. Sec. 27, T. 15 N., R. 3 W., Centralia quadrangle.
Lincoln Creek Formation (late Eocene to early
Miocene).

48

Localities.—USGS 15278, 15310, 15310a, 15499,
15516, 15532, 15537, 15548, M3873; cf. 15519.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Yakataga and Katalla
Districts, Gulf of Alaska; Lincoln Creek Formation (late
Eocene to early Miocene) and the Marrowstone Shale of
Durham (1944), Washington; Eugene Formation (early
and middle Oligocene), Alsea Formation (early to late
Oligocene), Tunnel Point Sandstone (middle Oligo—
cene), Oregon; Tumey Formation of Atwill (1935) (early
and middle Oligocene), California.

Genus Callista Poli

Callista Poli, 1791, Testacea utriusque Siciliae, eorumque historia et
anatomia, tome 1, p. 30.

Type species—By subsequent designation, Venus

chione Linné (Meek, 1876). Holocene Mediterranean.
Subgenus .Macrocallista Meek
Macrocallista Meek, 1876, US. Geol. Survey Territories, v. 9, p. 179.

Type species—By monotypy, Venus gigantea Gmelin
= Venus nimbosa Lightfoot. Holocene, Caribbean.

The mature specimens of Callista have much more
massive hinge plates and all the teeth are larger than on
specimens of Macrocallista of similar size; this is not
true of juvenile specimens of Callisto. Macrocallista is
much more produced anteriorly, is less inﬂated, and has
a thinner shell than Callista. The conﬁguration and
arrangement of teeth on both valves of Macrocallista so
closely resembles that of Callista that it does not seem
proper to separate M acrocallista except subgenerically.
Placing Macrocallista as a subgenus of Callista helps to
show the close relation within this difﬁcult and variable
group.

The hinge of Callista (Macrocallista) pittsburgensis
differs from that of the type species of Macrocallista,
Venus nimbosa Lightfoot. The hinge of C. (M .) nimbosa
is here described in order that the differences can be
noted and the reasons for retaining C. (M.)
pittsburgensis in Macrocallista understood.

In the following description, the right valve is consid-
ered to have two anterior laterals, three cardinals, and a
posterior lateral; the left valve is considered to have one
anterior lateral and three cardinals.

The right valve of Callista (Macrocallista) nimbosa
has the two anterior laterals bordering a socket that
receives the left anterior lateral. The right anterior
laterals are smooth and rounded, the dorsal one is
clearly deﬁned with a slight pointed prominence at the
anterior end. The ventral lateral is a thick, rather even
swelling projecting a bit over the socket and perhaps, if
strictly deﬁned, is not a lateral tooth. The right anterior
cardinal, the most prominent tooth, projects beyond all
the others. It is thickest at the ventral end, and it thins
and curves towards the anterior at the dorsal margin.
The posterior edge of the tooth nearly parallels the

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

anterior side of the middle cardinal. The right middle
cardinals form a very deep socket between their nearly
parallel surfaces. The right posterior cardinal is thinner
than the other two cardinals and is pointed at about
midpoint. It parallels the posterior lateral tooth. The
right posterior cardinal is not grooved in the strict sense
of the word, but has a ﬂange that looks like a deformity.
However, examination of 11 right valves of C. (M .)
nimbosa has shown that the posterior cardinal on all
right valves has an anterior ﬂange. The right posterior
cardinal consistantly shows a slight groove along the
anterior side at the highest part of the tooth, with the
part of tooth anterior to the groove lower than the
posterior part. The right posterior lateral is thin and
bladelike.

The anterior lateral of the left valve of C. (M .) nim-
bosa is a prominent, somewhat triangular, pointed
projection. The anterior cardinal is very thin except at
the ventral margin where it thickens; its anterior edge
is ﬂat and almost perpendicular to the beak. The middle
cardinal is thick and curved with the thickest portion at
the ventral end. The posterior cardinal, which resem-
bles a lateral tooth, is thin, bladelike, and long. It
extends along the dorsal margin to a point just above the
middle cardinal tooth where it forms a socket to receive
the right posterior cardinal.

Callista (Macrocallista) pittsburgensis Dall
Plate 12, ﬁgures 3, 5—11, 13

Callista pittsburgensis Dall, 1900, Wagner Free Inst. Sci. Trans, V. 3,
pt. 5, pl. 36, ﬁg. 22.

Meretrix (Callista) pittsburgensis Dall, 1900, Wagner Free Inst. Sci.
Trans, V. 3, pt. 5, pl. 43, ﬁg. 15.

Macrocallista pittsburgensis (Dall). Dall, 1903, Wagner Free Inst. Sci.
Trans, V. 3, pt. 6, p. 1253. Clark, 1918, California Univ. Dept.
Geology Bull., V. 11, p. 146. Clark, 1925, California Univ. Pubs,
Dept. Geol. Sci. Bull., V. 15, p. 92, pl. 18, ﬁg. 9; pl. 19, ﬁgs. 4, 5. Clark,
1932, Geol. Soc. America Bull., v. 43, p. 816, pl. 19, ﬁgs. 1, 2. Weaver,
1942, Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 175-176,
pl. 32, ﬁg. 7; pl. 41, ﬁgs. 4, 7, 10, 14. Hickman, 1969, Oregon Univ.
Mus. Nat. Hist. Bull. 16, p. 43, pl. 3, ﬁgs. 8—14.

Callista pittsburgensis is of moderate size, subovate in
outline, and sculptured with bunched concentric lines.
It is elongate posteriorly with a subdued angulation; the
anterior end is evenly rounded. The beaks are situated
one-fourth to one-ﬁfth the distance from the anterior
end. The shell is usually brown; Dall (1903, p. 1253)
attributed this to the preservation of the periostracum,
which seems reasonable considering the tight adher-
ence of the periostracum on Holocene species. A few
specimens lack the subdued posterior angulation and
are higher in proportion to length than the average
specimen (pl. 12, ﬁg. 8). These specimens are considered
to represent normal variation within the species. The
external ligament platform is commonly preserved. The
elongate lunule is demarcated by an incised line; it is
smooth because the concentric lines sculpturing the rest

CLASS PELECYPODA

of the shell do not cross it. The hinge of C. pittsburgensis
differs from the type species of Macrocallista, C.
nimbosa. The posterior cardinal tooth of the right valve
of C. pittsburgensis is deeply grooved, whereas this
tooth of C . nimbosa is not grooved; instead it has a small
ﬂange on the anterior side. The middle and anterior
right cardinals slant toward the anterior end rather
than being perpendicular to the beak; the socket
bordered by the two anterior laterals is not parallel to
the dorsal hinge margin, and both the anterior laterals
are more prominent on C. pittsburgensis than on C.
nimbosa. The left valve of C. pittsburgensis has an
anterior lateral that is smaller, thinner, and less
prominent than on C. nimbosa; the anterior cardinal is
not perpendicular to the beak but slants toward the
anterior margin; the middle cardinal projects over the
ventral edge of the hinge plate and seems to be very
slightly grooved; the anterior cardinal is essentially
similar to that of C. nimbosa. In both valves of C.
pittsburgensis, the hinge plate and attendant dentition
in specimens of similar size are more restricted to the
area below the beak. The anterior end of the shell of C.
nimbosa is much more produced. Perhaps the most
striking difference between the hinges of the two species
is the grooved right posterior cardinal of C.
pittsburgensis. C. hornii (Gabb) from the Eocene of
California (Stewart, 1930, pl. 17, ﬁg. 7) and C.
cathcartensis (Weaver) from the late Oligocene and
early Miocene of Washington have a grooved right
posterior cardinal. C. densa Moody ( 1916, p. 58) from the
Pliocene of California is said to have biﬁd posterior
cardinals in both valves. Although the differences
between C. pittsburgensis and C. nimbosa are consi-
dered signiﬁcant, it is my opinion that they could be the
result of the evolution of the genus, and that the
Pitarinae need much more study before it would be
practical to propose, if necessary, a new subgeneric
name.

Lectotype.—USNM 107396 is herewith designated
the lectotype (pl. 12, ﬁg. 13). The lectotype is one of the
two specimens originally ﬁgured by Dall (1900, pl. 36,
ﬁg. 22). The ﬁgured paratype (pl. 12, ﬁg. 11) has been
assigned catalogue number USNM 107399.

Type locality—Pittsburg, Columbia County, Oreg.
Sec. 23, T. 5 N., R. 4 W., Vernonia quadrangle. Pittsburg
Bluff Formation (middle Oligocene).

The posterior elongation and anterior location of the
beaks of C. pittsburgensis separate it from other species.
Locally very abundant, it occurs in great numbers in
some rocks with only a few other forms intermingled but
with no apparent life orientation. The mineralized
ligament is preserved on some specimens (M3858).

Localities.—USGS 2714, 5394, 15264, 15264a, b, e,
15310, 15310a, c, f, g,j, i, 15311, 15519, 15530, 15537,

 
49

15545, 15583, 15586, 15588, 18638, 21612, M3856,
M3857, M3858, M3867, M3868, cf. M3869, M3871,
M3872, M3878.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Alaska; Lincoln Creek
Formation (late Eocene to early Miocene), Washington;
Alsea Formation (early to late Oligocene), Eugene
Formation (early and middle Oligocene), and Tunnel
Point Sandstone (middle Oligocene), Oregon;
Kreyenhagen Shale (Eocene and early Oligocene),
Kirker Tuff (middle and late Oligocene), California.
Possibly in Alegria Formation (middle Oligocene),
California.

Family MACTRIDAE
Genus Spisula Gray
Spisula Gray, 1837, Mag. Nat. Hist., new ser., v. 1, p. 372.

Type species—By subsequent designation (Gray,
1847, Zool. Soc. London Proc., no. 179, p. 185), Mactra
solida Montagu = Cardium solidum Linné. Holocene,
Atlantic.

Subgenus Mactromeris Conrad

Mactromeris Conrad, 1868, Am. Jour. Conchology, v. 3, app., pt. 3, p.
45.

Type species.—-By subsequent designation (Stoliczka,
1871, Geol. Survey India, Palaeontologia Indica, ser. 6,
v. 3, p. 16), Mactra ovalis Gould, Holocene, North At-
lantic.

Spisula (Mactromeris) pittsburgensis Clark
Plate 14, ﬁgures 3—8, 10, 11

Spisula pittsburgensis Clark, 1925, California Univ. Pubs, Dept.
Geol. Sci. Bull., v. 15, p. 101—102, pl. 17, ﬁgs. 2, 4. Tegland, 1933,
California Univ. Pubs., Dept. Geol. Sci. Bull., v. 23, p. 120—121.
Weaver, 1942, Washington Univ. (Seattle) Pubs. Geology, v. 5, p.
235, pl. 54, ﬁg. 9; p]. 61, ﬁgs. 1, 4. Hickman, 1969, Oregon Univ. Mus.
Nat. Hist. Bull. 16, p. 51, pl. 5, ﬁg. 1.

Spisula pittsburgensis is subovate in outline, small to
moderate sized, and thin shelled. The posterior dorsal
margin is straight except for a slightly inﬂated es-
cutcheon. The posterior end is evenly rounded. A ridge
extends from the umbo to the posterior ventral margin.
The anterior dorsal margin is inﬂated in the lunule
area; the anterior end is slightly pointed. There is little
variation in size, outline, and degree of inﬂation in this
species.

The right anterior cardinal is thin, bladelike, and
protrudes well beyond the hinge plate; it is fused to the
dorsal margin of the shell. The right posterior cardinal
is thin, does not protrude as far as the anterior cardinal,
and borders the anterior end of the resilifer, which is
moderately deep and oblique. The anterior and pos-
terior paired laterals are thin; each are bordered with a
moderately shallow dorsal pit and separated from one
another by a very deep pit. The left cardinal has the
shape of an inverted V, is small, and projects far beyond
the hinge plate. The single anterior and posterior

50

laterals are thin, the posterior one bladelike, the an-
terior one rounded and more produced.

Holotype.—SU 5205.

Type locality.—UW 476. From bluffs along highway
near old mill at Pittsburg, Columbia County, Oreg.
Pittsburg Bluff Formation (middle Oligocene).

Spisula eugenensis differs from S. pittsburgensis by
having an anterior umbonal ridge (Hickman, 1969, p.
50—51).

Localities.——USGS 2714, 5394, 15264, 15264a—e,
15310, 15310a—f, i, 15311, 15312, 15499, 15532, 15545,
15586, 15588, 18638, M3856, M3858, M3860, M3869,
M3871, M3872, M3877, M3878.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Yakataga District,
Gulf of Alaska; Quimper Sandstone of Durham (1942)
(early and middle Oligocene) and Blakeley Formation of
Weaver (1912) (late Oligocene and early Miocene),
Washington; Alsea Formation (early to late Oligocene),
Eugene Formation (early and middle Oligocene), Tun-
nel Point Sandstone (middle Oligocene), Oregon.

Spisula. (Mactromeris?) veneriformis Clark
Plate 14, ﬁgures 1, 2, 9
Spisula veneriformis Clark, 1925, California Univ. Pubs., Dept. Geol.

Sci. Bull., v. 15, p. 103, pl. 16, ﬁgs. 1—3. Weaver, 1942, Washington

Univ. (Seattle) Pubs. Geology, v.5, p. 235, pl. 54, ﬁg. 9; pl. 61, ﬁgs. 1,

4.

Clark describes the hinge of this species as follows:

Hinge plate rather heavy; resilifer pit deep, the two cardinals in the
right valve well developed, both reaching nearly across hinge plate;
anterior cardinal close to and connected with anterior dorsal margin.
Cardinal in right valve apparently not deltoid. The deltoid tooth is a
character common to almost all genera of the Mactridae; but in this
species the cardinal consists of one heavy process extending from a
beak to anterior edge of hinge plate.

Keen (1969, p. N595) describes the hinge of the
Mactracea as having one inverted V-shaped cardinal
tooth in the left valve and two cardinals in the right
valve.

The right valve is here considered to have two cardi-
nal teeth, rather than one deltoid tooth. The few
specimens of Spis ula veneriformis in the collections are
internal molds with no shell remaining. Rubber im-
pressions were made of all specimens retaining a mold
of the hinge. An impression of a right valve was ob-
tained (pl. 15, ﬁg. 2), and although the impression is not
perfect, the right valve may have had two cardinal teeth
originally. In examining Holocene specimens of Spisula
(Mactromeris) in the collections, I found that in at least
half the specimens of right valves the posterior cardinal
was either completely destroyed or broken. Perhaps
when the valves of this form are disarticulated, the
fragile right posterior cardinal is destroyed. This may
be the explanation for Clark (1925, p. 103) saying that
the right valve had but one tooth.

Holotype.—UCMP 54.

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

Type locality.——SU NR 42. In shale and sandstone in
sea cliff at Tunnel Point, west of Coos Bay, Oreg. Tunnel
Point Sandstone (middle Oligocene).

This species is very large and shaped more like a
venerid than a mactrid. The beaks are high and about a
third the distance from the anterior margin. The ven-
erid outline distinguishes S. veneriformis from other
species of Spisula.

Localities.—USGS 15516, 15532, 15537, 15544,
15588.

Occurrence elsewhere—Tunnel Point Sandstone
(middle Oligocene), Oregon.

Family MESODESMATIDAE
Subfamily DAVILINAE
Genus Ervilia. Turton
Ervilia Turton, 1822, British Bivalves, p. 56.

Type species.—Mya nitens Montagu. Holocene,
Florida.

?Ervilia oregonensis Dall
Plate 16, ﬁgures 2, 5

E rvilia oregonensis Dall, 1898, Wagner Free Inst. Sci. Trans, v. 3, pt.
4, p. 916, pl. 33, ﬁg. 16. Weaver, 1942, Washington Univ. (Seattle)
Pubs. Geology, v. 5, p. 243, pl. 56, ﬁg. 4.

The single specimen is presumably conspeciﬁc with
Ervilia oregonensis Dall. The hinge, though exposed, is
not sufﬁciently well preserved for generic identiﬁcation.
The specimen is more quadrate in outline than the
Holocene specimens of Ervilia. The shell is very thin
and concentrically sculptured, and the ligament is
presumably obsolete.

Holotype.——USNM 107406.

Type locality.—Nehalem River, Columbia County,
Oreg. Presumably from the Pittsburg Bluff Formation,
middle Oligocene.

Locality.—USGS 18638.

Family TELLINIDAE
Subfamily TELLININAE
Genus Tellina Linné
Tellina Linné, 1758, Systema naturae, ed. 10, p. 674.

Type species.—By subsequent designation (Schmidt,
1818, Versuch Conchylien-Sammlung, p. 51, 177),
Tellina radiata Linné, Holocene, West Indies.

Subgenus Eurytellina. Fischer

Eurytellina Fischer, 1887, Man. de Conchyliologie et de Paleont.
Conch., p. 1147.

Type species—By monotypy, Tellina punicea Born.
Holocene, West Indies.
Tellina (Eurytellina) aduncanasa Hickman
Plate 11, ﬁgures 7—12

Tellina aduncanasa Hickman, 1969, Oregon Univ. Mus. Nat. Hist.
Bull. 16, p. 55—56, pl. 6, ﬁgs. 7—12.

Tellina aduncanasa is of moderate size and elongate;
the length about twice the height. The anterior end is
evenly rounded, the posterior end sharply attenuated.
The posterior end is strongly beveled and set off by a

CLASS PELECYPODA 51

ridge at the anterior side. The entire surface bears ﬁne
incised lines that change direction at the anterior edge
of the beveled part, making an angle of about 90°.
Hickman (1969, p. 56) describes the hinge of both
valves.

Holotype.—UO 27262.

Type locality.—UO 2567. In well-indurated
brownish-gray tuffaceous sandstone and siltstone on
east side of Oregon State Highway 47, 0.2 mile north of
junction with Pittsburg-Scappoose Road, N1/2 sec. 23, T.
5 N., R. 4 W., Vernonia quadrangle, Columbia County,
Oreg. Pittsburg Bluff Formation, (middle Oligocene).

Localities.—USGS 2714, 2722, 15264, 15264b, c, e,
15310, 15310b, 15312, 15544, 15586, 15588, M3858; cf.
15311.

Occurrence elsewhere—Eugene Formation (early
and middle Oligocene), Oregon.

Tellina? pittsburg'ensis Clark
Plate 11, ﬁgures 1—6
Tellina pittsburgensis Clark, 1925, California Univ. Pubs, Dept.

Geol. Sci. Bull., v. 15, p. 95, pl. 12, ﬁgs. 8, 9. Weaver, 1942,

Washington Univ. (Seattle) Pubs. Geology, v. 5, p. 200—201, pl. 48,

ﬁg. 4. Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 55,

pl. 6, ﬁgs. 3—6.

Tellina? pittsburgensis is of small size, subovate in
outline, and very thin shelled. The anterior end is
evenly rounded and the posterior end is slightly pro—
duced. The shell bears ﬁne, bunched concentric lines
that are deﬂected near the posterior end. Just anterior
to this deﬂection is a slight sulcus. The shell is mod-
erately inﬂated. The left valve is slightly larger than
the right, and both valves are deﬂected to the right at
the posterior end.

Holotype.—SU Paleo. Type C011. 46.

Type locality.—SU 10c. NP 5. In sandstone cliff along
Nehalem River near old Pittsburg lumber mill, just past
bridge below Vernonia, Oreg. Pittsburg Bluff Forma-
tion (middle Oligocene).

Because of the state of preservation of the specimens,
the small size of the species, and the very thin shell, it
has not been possible to prepare a perfect hinge. Several
hinges were exposed and two are ﬁgured (pl. 11, ﬁgs. 1,
2) but still some details are not clear. No lateral teeth
could be identiﬁed without qualiﬁcation, although there
is a suggestion of a lateral tooth on one of the valves.
Hickman (1969, p. 55) found well-developed lateral
teeth on specimens identiﬁed as T. pittsburgensis from
the Eugene Formation. Her ﬁndings suggest that the
specimens from the Eugene Formation may not be
conspeciﬁc with the Pittsburg Bluff specimens. The
following characters were noted on the hinges exposed:
On the right valve there are two cardinal teeth, the
posterior one thick and biﬁd, the anterior one very small
and thin. A possible lateral tooth is posterior to the

 
cardinals but near them; no lateral tooth was found
anterior to the cardinals. On the left valve are two
cardinal teeth, the posterior thick and biﬁed and the
anterior one very small and thin. A possible lateral
tooth is anterior to the cardinal teeth.

A closely related form occurs in the Poul Creek
Formation (middle Oligocene to early Miocene),
Yakataga and Katella Districts, Gulf of Alaska.

Localities.—USGS 2714, 15264, 15264b, c, 15310,
15310d, 15519, 15530, 15586, 15588, 18638, M3871,
M3877, cf. M3878.

Occurrence elsewhere—Gries Ranch Formation
(early Oligocene), Quimper Sandstone of Durham
(1942) (early and middle Oligocene), Washington;
Eugene Formation (early and middle Oligocene) and
Tunnel Point Sandstone (middle Oligocene), Oregon;
Tumey Formation of Atwill (1935) (Oligocene),
California.

Family SOLENIDAE
Genus Solen Linné
Solen Linné, 1758, System naturae, ed. 10, p. 672.

Type species.—By subsequent designation
(Schumacher, 1817, Essai d’un nouveau systeme des
habitations des vers testaces, p. 124, pl. 6, ﬁg. 3), Solen
vagina Linné. Holocene, Europe.

Solen townsendensis Clark
Plate 13, ﬁgures 3—5

Solen (Plectosolen) townsendensis Clark, 1925, California Univ.
Pubs, Dept. Geol. Sci. Bull., v. 15, p. 97—98, pl. 22, ﬁgs. 7, 10.
Solen townsendensis Clark. Efﬁnger, 1938, Jour. Paleontology, v. 12,
p. 372—373. Weaver, 1942, Washington Univ. (Seattle) Pubs.
Geology, v. 5, p. 225, pl. 53, ﬁgs. 1, 9.

?Solen sicarius Gould. Hickman, 1969, Oregon Univ. Mus. Nat. Hist.
Bull. 16, p. 63—64, pl. 8, ﬁgs. 5, 7, 9.

Solen townsendensis is thin shelled. The few
specimens in the collections are small. The anterior end
is truncated at the dorsal margin and evenly rounded at
the ventral margin. It lacks a sulcus but it has a slight
broad depression. The posterior end is almost evenly
rounded with a slight ﬂattening in the midregion of the
shell.

Holotype.—SU 51.

Type locality.—SU Loc. NP 272. In bluffs along
Skamokawa River above big bend 1 mile east of junction
of main and middle forks, Skamokawa, Wash. Gries
Ranch Formation (early Oligocene).

Hickman (1969, p. 63—64) assigned an Oligocene
Solen from the Eugene Formation (early and middle
Oligocene), Oregon, to the Miocene to Holocene species
Solen sicarius Gould, because she felt it impossible to
determine the afﬁnities of the fossil species without
intensive study. One well-preserved specimen in the
Pittsburg Bluff collections (pl. 8, ﬁgs. 10, 11) makes
some comparison with S. sicarius possible. In the ratio
of height to length, the fossil form is identical to S.

52

sicarius. However, both the anterior and posterior ends
of S. townsendensis are rounded as in Solen rosaceus
Carpenter, a Holocene species, rather than truncated as
in S. sicarius. S. rosaceus is much more elongate in
proportion to height than the Oligocene species. It
seems probable that the Oligocene species is not con-
speciﬁc with the Holocene forms examined, and the
name Solen townsendensis is retained for the fossil
form.

Solen conradi Dall (1900, p. 953), a Miocene species,
has a concave dorsal margin and is more sharply
truncated at the posterior end than S. townsendensis.

Localities.——USGS 2714, 5394, 15264, 15310, 15537,
15586, M3858, M3860, M3871, M3872.

Occurrence elsewhere.—Gries Ranch Formation
(early Oligocene), Quimper Sandstone of Durham
(1942) (early and middle Oligocene), Washington; Alsea
Formation (early to late Oligocene) and possibly in the
Eugene Formation (early and middle Oligocene) and
the Tunnel Point Sandstone (middle Oligocene), Ore-
gon.

Genus Solena Mérch
Solena Mbrch, 1853, Cat. Conch. Yoldi, pt. 2, p. 7.

Type species.—By subsequent designation (Stoliczka,
1871, Geol. Survey India, Palaeontologia Indica, ser. 6,
p. xvi), Solen obliquus Spengler. Holocene, Caribbean.

Subgenus Eosolen Stewart

Eosolen Stewart, 1930, Acad. Nat. Sci. Philadelphia Spec. Pub. 3, p.
290—291.

Type species—By original designation, Solen
plagiaulax (Cossmann). Middle Eocene, France.

On the basis of a distinct umbonal furrow, Solena
(Eosolen) columbiana (Weaver and Palmer) (1922, p. 24,
pl. 10, ﬁg. 3) was placed in Eosolen by Stewart (1930, p.
292). The following species should also be assigned to
this subgenus:

Solena lincolnensis (Weaver), 1916a, p. 43, pl. 2, ﬁgs.
9—12, Oligocene, Washington.

Solena clarki (Weaver and Palmer), 1922, p. 23-24, pl.
9, ﬁg. 16, Eocene, Washington.

Solena eugenensis (Clark), 1925, p. 98, pl. 22, ﬁg. 1,
Oligocene, Oregon.

Solena. (Eosolen) eugenensis (Clark)
Plate 13, ﬁgures 1, 2, 6

Solen eugenensis Clark, 1925, California Univ. Pubs, Dept. Geol. Sci.
Bull., v. 15, p. 98, pl. 22, ﬁg. 1.

Solena eugenensis (Clark). Weaver, 1942, Washington Univ. (Seattle)
Pubs. Geology, v. 5, p. 230, pl. 53, ﬁgs. 14, 15.

Solena (Eosolen) eugenensis (Clark). Hickman, 1969, Oregon Univ.
Mus. Nat. Hist. Bull. 16, p. 63, pl. 7, ﬁgs. 11, 12.

Solena eugenensis is a large moderately thick—shelled
form with a strong anterior sulcation. The shell ﬂares
outward at the anterior gape. The anterior margin is
truncated at an angle of about 30° from the perpen-
dicular; the posterior angulation is nearly perpen-

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

dicular. The shell is smooth except for bunched con-
centric lines. Parts of the mineralized ligament are
preserved on some specimens.

Holotype.—UCMP 30338.

Type locality.———UC 4182. New City Reservoir,
Eugene, Oreg. Eugene Formation (early and middle
Oligocene).

Solena eugenensis is higher in proportion to length
and has a lower anterior angulation than S. lorenzana
Wagner and Schilling (1923, p. 256, pl. 47, ﬁg. 1) from
the Oligocene of California.

A closely related form occurs in the Poul Creek
Formation (middle Oligocene to early Miocene), Alaska.

Localities.—USGS 2714, 5394, 15264b, 15278,
15310a, 15312, 15499, 15519, 15529, 15537, 15544,
15586, 15588, M3858, M3867, M3868, M3872; cf.
M3871, cf. M3878.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene), Washington; Eugene
Formation (early and middle Oligocene), and possibly in
the Alsea Formation (early to late Oligocene) and in the
Tunnel Point Sandstone (middle Oligocene), Oregon.

Family HIATELLIDAE
Genus Panopea Menard de la Groye

Panopea Ménard de la Groye, 1807 , Mémoire sur un nouveau genre de
coquille bivalve-équivalve de la famille des Solenoides, p. 16, 31
(Dall, 1912, Malacological Soc. Proc., V. 10, p. 34—35). Vokes (1967,
p. 326) cites Panopea Ménard de la Groye (April?, 1807) as the
nomenclatorially valid name predating Panope Menard de la Groye
(August, 1807). A decision of the I.C.Z.N. for the emended spelling,
Panope, is pending.

Type species.—By subsequent designation (Schmidt,
1818, Versuch Conchylien-Sammlung, p. 47, 177), Mya
glycimeris Born (cited by Ménard de la Groye, 1807, p.
32, in synonymy of Panope aldrovandi). Holocene,
Mediterranean Sea.

Panopea snohomishensis Clark
Plate 15, ﬁgure 5

Panope snohomishensis Clark, 1925, California Univ. Pubs, Dept.
Geol. Sci. Bull., v. 15, p. 105, pl. 10, ﬁg. 2. Weaver, 1942, Washington
Univ. (Seattle) Pubs. Geology, v. 5, p. 261—263, pl. 59, ﬁgs. 3, 10.
Panopea snohomishensis is moderate sized, subovate,

and high in proportion to length. The anterior end is
evenly rounded and the posterior end is attenuated and
evenly rounded to moderately truncated (pl. 15, ﬁg. 5).
The posterior end is smaller than the anterior end. The
beaks are slightly anterior of the midportion of the
shell. The hinge line is not straight; instead it slopes
from the beaks to the anterior and posterior ends of the
shell and thus is not parallel to the ventral margin. The
beaks are prominent and small. The hinge is not ex—
posed.

Holotype.—SU 59. Paratype SU 60.

Type locality.—SU loc. N.P. 146. In Northern Paciﬁc
Railway cut one-half mile north of Cathcart Station,

CLASS PELECYPODA

Snohomish County, Wash. sec. 6, T. 27 N., R. 6 E.,
Maltby quadrangle, Lincoln Creek Formation (late
Eocene to early Miocene).

This species is distinguished by its subovate outline,
the slope of the dorsal margin, and the large anterior
end.

Panopea cf. P. snohomishensis is reported from the
Poul Creek Formation (middle Oligocene to early
Miocene), Alaska.

Localities.—USGS 15264, 15516.

Occurrence elsewhere—Lincoln Creek Formation
(late Eocene to early Miocene), Washington; Alsea
Formation (early to late Oligocene) Oregon.

Panopea ramonensis Clark
Plate 15, ﬁgures 1—3
Panope ramonensis Clark, 1925, California Univ. Pubs, Dept. Geol.

Sci. Bull., v. 15, p. 106, pl. 10, ﬁgs. 2, 3. Weaver, 1942, Washington

Univ. (Seattle) Pubs. Geology, v. 5, p. 263—264, pl. 59, ﬁg. 11.

Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 65, 68, pl.

8, ﬁgs. 8, 12.

Panopea ramonensis is elongate and subquadrate in
outline. The hinge line is straight and parallels the
ventral margin. The posterior and anterior ends are of
equal size; the posterior end is broadly truncated and
gaping and the anterior end is evenly rounded. The
beaks are small but prominent, inturned, and anterior
of the midpoint of the shell. In his original description,
Clark (1925, p. 106) says, “A fairly broad, shallow
depression or sinus between beak and lower angle of
truncated posterior end; this zone of depression more
noticeable on some specimens than on others.” In the
Pittsburg Bluff collections, the specimens with the shell
intact do not show this sinus, whereas those from which
the shell has exfoliated do. It seems possible that this
sinus is simply the impression left at the boundary
where thickened shell which forms the hinge line meets
the thinner shell. Modeling clay was pressed into the
shell of a Holocene specimen of Panopea abrupta and a
“sinus” was produced on the clay similar to that seen on
internal molds of P. ramonensis. P. ramonensis is more
elongate in proportion to height and is much smaller
than P. abrupta. It differs from P. snohomishensis by
having a straight hinge line and a medially located
beak.

Holotype.—UCMP 30330. Paratype: UCMP 30331.

Type locality.—UC loc. 1131. One-half mile southwest
of town of Walnut Creek, on east side of Oakland-
Antioch Railway bridge, elevation 150 feet, Contra
Costa County, Calif. San Ramon Sandstone (early
Miocene?)

Localities.—-USGS 2714, 15310, 15310e, 15312,
15499, 15519, 15586, 15588, M3871, M3872.

Occurrence elsewhere—Blakeley Formation of
Weaver (1912) (late Oligocene and early Miocene),

 
53

Eugene Formation (early and middle Oligocene),
Oregon; San Ramon Sandstone(early Miocene?), Wygal
Sandstone Member (late Oligocene) of the Temblor
Formation, California.

Family PERIPLOMATIDAE
Genus Cochlodesma. Couthouy

Cochlodesma Couthouy, 1839, Boston Jour. Nat. Hist., v. 2, p. 170.
Type species—By monotypy, Anatina leana Conrad,
Holocene, Nova Scotia to North Carolina, United
States.
Cochlodesma. bainbridgensis Clark
Plate 16, ﬁgures 4, 6—11

Cochlodesma bainbridgensis Clark, 1925, California Univ. Pubs,
Dept. Geol. Sci. Bull., v. 15, p. 86, pl. 13, ﬁgs. 3, 4. Tegland, 1933,
California Univ. Pubs, Dept. Geol. Sci. Bull., v.23, p. 112, pl. 6, ﬁgs.
3, 4. Weaver, 1942, Washington Univ. (Seattle) Pubs. Geology, v. 5,
p. 117, pl. 25, ﬁg. 1, pl. 29, ﬁg. 2. Durham, 1944, California Univ.
Pubs, Dept. Geol. Sci. Bull., v. 27, p. 141.

Cochlodesma bainbridgensis is small to moderate in
size; it has a very thin fragile shell that is internally
nacreous. The shell is sculptured with faint, concentric,
slightly irregularly spaced undulations that do not
resemble those present on Cyathodonta, a generic
assignment considered for this species (Grant and Gale,
1931, p. 255, footnote). On the hinge of a right valve, the
condrophore is small, deep, subtriangular and directed
posteriorly (pl. 16, ﬁg. 9), closely matching that illus-
trated by Tegland (1933, pl. 6, ﬁg. 3). The variation in
outline of the four specimens ﬁgured (pl. 16, ﬁgs. 6, 8, 10,
11) is so great that it seems useless to try to use this as a
speciﬁc criterion. Some of the variation is undoubtedly
caused by deformation but some of it may be inherent. It
has not been possible to separate the Cochlodesma in
the Pittsburg Bluff Formation from C. bainbridgensis;
possibly C. bainbridgensis is a species with a long time
range. The preservation of the specimens in the
collections is such that is has not been possible to
determine if C. bainbridgensis is inequivalve with the
right valve more convex.

Holotype.——-SU 27.

Type locality.—SU loc. NR 103. In outcrops of shaly
sandstones along beach between south side of entrance
to Port Blakeley and Restoration Point, Wash. Blakeley
Formation of Weaver (1912) (late Oligocene and early
Miocene).

Paratype.—SU 28. Same locality as holotype.

A closely related form occurs in the Alsea Formation
(early to late Oligocene), Oregon.

Localities.—USGS cf. 5392, 15278, 15519, 15583,
15588, M3872.

Occurrence elsewhere—Poul Creek Formation (mid-
dle Oligocene to early Miocene), Yakataga District,
Gulf of Alaska; Stepovak Formation of Burk (1965)
(early and middle Oligocene), Coal Bay section, Alaska;

54

Blakeley Formation of Weaver (1912) (late Oligocene
and early Miocene), Washington.

Family THRACIIDAE
Genus Thracia Blainville

Thracia Blainville, 1824, Dictionnaire des sciences naturelles, V. 32,

p. 347.

Type species.—By subsequent monotypy (Blainville,
1825, Manuel de malacologie et de conchyliologie, p.
660, removes his division B from Thracia, leaving but
one species in the genus), Thracia corbuloides Blain-
ville. Holocene, Mediterranean.

Sowerby (1823, The Mineral Conchology of Great
Britain, v. 5, pt. 1, p. 20) under the discussion of Mya
mentions Thracia of Leach as a possible name to be
applied to some forms he assigns to Mya. No particular
species or ﬁgure is cited, and this reference to Thracia is
considered a nomen nudum as listed by Vokes (1967, p.
339).

Thracia (Thracia) condoni Dall

Plate 16, ﬁgures 1, 3

Thracia condoni Dall, 1909, U.S. Geol. Survey Prof. Paper 59, p.
135—136, pl. 19, ﬁg. 5. Clark, 1918, California Univ., Dept. Geology
Bull., v. 11, no. 2, p. 137, pl. 11, ﬁg. 12; pl. 12, ﬁg. 2. Tegland, 1933,
California Univ. Pubs, Dept. Geol. Sci. Bull., v.23, no. 3, p. 113, pl.
6, ﬁg. 5. Weaver, 1942, Washington Univ. (Seattle) Pubs. Geology,
v. 5, p. 119, pl. 25, ﬁg. 10; pl. 29, ﬁg. 15. Durham, 1944, California
Univ. Pubs, Dept. Geol. Sci. Bull., V. 27, n0. 5, p. 141, pl. 13, ﬁg. 6.
Hickman, 1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 72—73, pl.
9, ﬁgs. 10—14.

Thracia condoni is usually of small to moderate size.
It is not common in the Pittsburg Bluff Formation. The
specimen illustrated is the largest in the collections; it
measures 46.7 mm long (broken) and 34.7 mm high. The
shell is smooth except for bunched concentric lines. The
beaks are centrally located. The posterior end is elon-
gate and the dorsal margin is almost straight. The
ligament nymph and groove can be seen on the pre-
served part of the hinge illustrated on plate 16, ﬁgure 3.
Parts of mineralized ligament are preserved on some
specimens. Because of the thin shell, most of the
specimens of T. condoni are crushed and distorted, and
many are molds from which the shell has exfoliated. On
the best preserved specimens, the right valve, notice-
ably larger than the left valve, overlaps the ventral
edge. On a specimen with a left valve about 19.4 mm
high, the right valve extends 1.7 mm beyond the ventral
margin at the anterior end. On all specimens the beak
on the right valve and the area along the dorsal edge of
the anterior hinge have been abraded by the left valve.

Holotype.——USNM 110460.

Type locality.—Smith’s quarry, Eugene, Oreg.
Eugene Formation (early and middle Oligocene).

T. condoni has a straighter posterior dorsal margin
and is more elongate posteriorly than Thracia schencki
Tegland (1933, p. 112—113, pl. 6, ﬁgs. 6—11). The umbos
are lower on T. condoni, the shell less inﬂated, and the

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

posterior end more elongate than on Thracia
trapezoides Conrad (1849, p. 723, pl. 17, ﬁg. 6a; Moore,
1963, p. 84—85, pl. 26, ﬁg. 3; pl. 31, ﬁg. 6).

Localities.—USGS 15264, 15278, 15310, 15519,
15548, 15583, 15586, 15588.

Occurrences elsewhere—Poul Creek Formation
(Oligocene and Miocene), Yakataga District, Gulf of
Alaska; Stepovak Formation of Burk (1965)(early and
middle Oligocene), Alaska; Quimper Sandstone of
Durham (1942) (early and middle Oligocene),
Washington; Eugene Formation (early and middle
Oligocene), Alsea Formation (early to late Oligocene),
Oregon; San Lorenzo Formation (Eocene and
Oligocene), California.

Class CEPHALOPODA
Family NAUTILIDAE
Aturia. angustata (Conrad)
Plate 15, ﬁgure 4

Nautilus angustatus Conrad, 1849, U.S. Explor. Exped. Geology, v. 10,
app. p. 728, atlas, pl. 20, ﬁgs. 5, 6.

Nautilites angustatus (Conrad). Conrad, 1858, Acad. Nat. Sci.
Philadelphia Jour., v. 3 (new ser.), p. 335.

Aturia angustata (Conrad). Dall, in Diller, 1896, U.S. Geol. Survey
17th Ann. Rept., pt. 1, p. 459, 465, 467, 468. Dall, 1909, U.S. Geol.
Survey Prof. Paper 59, p. 21. Schenck, 1931, California Univ. Pubs.,
Dept. Geol. Sci. Bull., v. 19, p. 457—462, pl. 69, ﬁgs. 1—3, pl. 70, ﬁgs.
1—5, pl. 71, ﬁgs. 1, 3—8, pl. 72, ﬁgs. 1, 2, 5, 6, text ﬁgs. 4, 5, 7—9, 20—23,
30, 33. Weaver, 1942, Washington Univ. (Seattle) Pubs. Geology, v.
5, p. 551—552, pl. 102, ﬁgs. 1—7, 10. Miller, 1947, Geol. Soc. America
Mem. 23, p. 85—88, pl. 48, ﬁgs. 5, 6, pl. 88, ﬁg. 1, pl. 90, ﬁgs. 1—3, pl.
91, ﬁgs. 12 pl. 92, ﬁgs. 1, 2, 8, 9, pl. 93, ﬁgs. 3. 4. Moore, 1963, U.S.
Geol. Survey Prof. Paper 419, p. 85—86, pl. 31, ﬁgs. 1, 5. Hickman,
1969, Oregon Univ. Mus. Nat. Hist. Bull. 16, p. 101—102, pl. 14, ﬁg.
10.

Aturia ziczac (Sowerby). Conrad, 1865, Am. Jour. Conchology, v. 1, p.
150. Gabb, 1869, Paleontology of California, v. 2, p. 69. Ball and
Harris, 1892, U.S. Geol. Survey Bull. 84, p. 22$224 (NotNautilus
ziczac Sowerby, 1812, Mineral Conch. Great Britain, v. 1, pl. 12,
lowest ﬁg.).

Aturia cf. ziczac (Sowerby). Reagan, 1908, Kansas Acad. Sci. Trans., V.
22, p. 171.

Aturia angustata has been described in detail by
Schenck (1931, p. 457—462) and by Miller (1947, p. 85—
88).

Type species.—Larger ﬁgured syntype, USNM 3610
(Moore, 1963, pl. 31, ﬁg. 1). This is the only specimen
originally ﬁgured by Conrad (1849, pl. 20, ﬁg. 5) that
remains in the U.S. National Museum type collection.

Type locality—Astoria, Oreg. Astoria Formation
(Miocene).

The only specimen of A. angustata known from the
Pittsburg Bluff Formation is the one ﬁgured on plate 15,
ﬁg. 4. It was collected and donated by Bruce Welton,
from Portland State University, to whom I am indebted.

Locality—Type locality for the Pittsburg Bluff
Formation, near Pittsburg, Oregon. (Bruce Welton,
written commun., Feb. 16, 1973).

CLASS CEPHALOPODA

Occurrence elsewhere—Early Oligocene to middle
Miocene in the Coast Ranges of Washington, Oregon,
and California. Lincoln Creek Formation (late Eocene
to early Miocene) and Weaver’s (1912) Blakeley
Formation (late Oligocene and early Miocene),
Washington; Eugene Formation (early and middle
Oligocene) and possibly the Keasey Formation (late
Eocene and early Oligocene), Oregon.

U.S. GEOLOGICAL SURVEY FOSSIL LOCALITIES
IN THE PITTSBURG BLUFF FORMATION,
MIDDLE OLIGOCENE, NORTHWESTERN
OREGON

 
USGS Cenozoic Description Collector Date
locality collected
No,

Washington,

DC, Register

2415 ______ Westport on Columbia River, Will Brown __________ ?1891
about 24 mi east of Astoria.

2707 ______ Sec. 4, T. 2 N., R, 4 W, J. S, Diller ____________ 1895
Washington County.

2714 ,,,,,, Pittsburg, Columbia County, sec. 23, ,,,,,,,,,, do ,,,,,,,,,, 1895
T. 5 N., R. 4 W.

2715 ,,,,,, Rock Creek, sec. 31, T. 5 N., R. 4 W., __________ do __________ 1895
Columbia County.

2721 ,,,,,, SW‘A sec. 27, T. 5 N., R. 3 W., .......... do ,,,,,,,,,, 1895
Columbia County

2722 ______ Nehalem River, 4 mi above Mist, __________ do ,,,,,,,,,, 1895
sec. 29, T. 6 N., R. 4 W.,
Columbia County.

2723 ,,,,,, Nehalem River near Mist, sec. 14, ,,,,,,,,,, do ,,,,,,,,,, 1895
T. 6 N., R. 5 W,, Columbia County.

5394 ,,,,,, Pittsburg road cut, Columbia County, G. A Macready ,,,,,, 1910
NWV4 sec. 23, T, 5 N,, R. 4 W,

15264 ,,,,,, East side of Oregon State Highway 47, W. C. Warren ,,,,,,,, 1944
approximately 600 ft north of
junction of Oregon State Highway 47
and Scappoose-Vernonia Road,
Columbia County, 3,500 ft south of
grid 2,660 and 5,000 ft west of grid
820, U.S. Army Corps Engineers
Vernonia quadrangle.

15278 ______ Wolf Creek Highway (Oregon 2), W. C. Warren 1944
third cut on north side of northwest and H. E. Vokes,
and H. E. Vokes.
junction of Buxton-Vernonia Road
(Oregon State Highway 47). Locality
is approximately 3/4 mi from junction.
5,500 ft south of grid 2,635, 5,500 ft
east of grid 910, U.S. Army Corp,
Engineers Gales Creek quadrangle.

15310 ,,,,,, First large roadcut on west side of H. Norbisrath 1944
Scappoose-Vernonia Road, south of and H. E. Vokes.
cutoff to Wilark, Columbia County.

15311 ,,,,,, Same locality as 15310, but 20 ft __________ do .......... 1944
stratigraphically lower.

15312 ,,,,,, Cuts on east side of Wilson Lumber __________ do __________ 1944
Company road, 0.4 mi south of
Kenusky Creek, on east branch of
Nehalem River. 6,200 ft south of
grid 2,655; 2,600 ft east of grid 820,
US. Army Corps Engineers
Vernonia quadrangle,

15457 ______ Cut on east side of abandoned road Wi C, Warren ,,,,,,,, 1944
grade paralleling Oregon Highway
202; 0.2 mi north of south edge of
Svenson quadrangle,

15499 111111 Under United Railroad trestle, about R. M. Grivetti, 1944
1 mi north of Buxton, Washington W. C. Warren,
County. Trestle bears notation "U.R. and H. Norbisrath.
Tr 399 & 35." At south end of Gales
Creek quadrangle.

 
55

 
USGS Cenozoic Description
locality
No,

Collector

Date
collected

 
15516 ,,,,,, Road cut on Vernonia-Scappoose Road
near divide. This is the ﬁrst cut
south of point Where the road passes
over the railroad tunnel. Vernonia
quadrangle.

15519 ,,,,,, Cut on line of United Railroad 2.0 mi
(airline) north of Buxton, Washing-
ton County. Cut is at north end of
arcuate railroad trestle. Gales Creek
quadrangle.

15529 ,,,,,, Cut on south side of Vernonia-
Scappoose Road, 3.5 mi by road
southeast ofjunction at Wilark,
Columbia County. Vernonia
quadrangle.

15530 ______ Cut on north side of Vernonia-
Scappoose Road, 5.0 mi by road
southeast of junction at Wilark,
Columbia County. Vernonia
quadrangle

15532 ,,,,,, Cut on north side of Vernonia-
Scappoose Road, 1.7 mi west of
Chapman School, Columbia County.
St. Helens quadrangle.

15536 111111 North side of Scoggin Creek Road, 1.3
1.3 mi west ofjunction with Oregon
and W. C. Warren,

State Highway 47.

15537 ______ Cut on north side of Vernonia-
Scappoose Road, 0.6 mi west of
Chapman School, Columbia County.
St, Helens quadrangle.

15544 ,,,,,, Cut on curve of United Railroad. This
is ﬁrst curve northeast of Buxton,
Washington County. 3,050 ft west of
grid 815,000 and 5,500 ft south of
grid 263,500. U.S. Army Corps
Engineers Vernonia quadrangle.

15545 ,,,,,, North end of trestle over ravine,
Fossils from north bank below
trestle, 5th railroad trestle north of
Buxton, Washington County.

15548 ,,,,,, Approximately 34 mi up Flora Road
from Nehalem River Highway,
along poorly exposed bank and in
roadbed Where road ascends hillside.
Cathlamet quadrangle.

15583 ,,,,,, Prominent bluff of east side of Oregon
State Highway 47, 1.6 mi north of
the junction with the St. Helens
highway, Columbia County, Oreg.
4,200 ft west of grid 820, 4,000 ft
north of grid 2,260, Cathlamet
quadrangle,

15586 ,,,,,, North end of short, abandoned tunnel
about 1/2 mi east of Westport, Clatsop
County, Greg, on south side of U.S.
Highway 30. 700 ft west of grid 800,
5,000 ft north of grid 2,865,
Cathlamet quadrangle,

15588 ,,,,,, Cut in logging road along the head-
waters of the second main tributary
entering Coal Creek from the north-
east of its junction with Pebble
Creek. 3,900 ft west of grid 820,
5,200 ft south of grid 2,650.
Vernonia quadrangle.

18638 ,,,,,, Type area of Pittsburg Bluff
Formation.

18779 ,,,,,, Type area of Pittsburg Bluff Formation,

Wolf Creek Highway, north of
Vernonia.

21612 ______ Pittsburg Bluff Formation. Oyster lens
with Acila about 30 ft above
Molopophurus.

W. C. Warren ,,,,,,,,

W. C. Warren
and Hi Norbisrath.

W. C, Warren ________

,,,,,,,,,, do,,,,,,,,,,

__________ do_-___._-u

R. M. Grivetti

W. C. Warren ,,,,,,,,

R. M. Grivetti,
H. Norbisrath,
and W. C. Warren.

,,,,,,,,,, do,,,,,,,.,,

H. Norbisrath
and W, C, Warren.

H. Norbisrath ,,,,,,,,

W. C. Warren,
D, Duncan,
and H. E. Vokes,

H. Norbisrath ,,,,,,,,

Ralph Stewart ........

E, James,
P. D. Snavely,
and W. W. Rau,
R. E, Stewart ,,,,,,,,

1944

1944

1944

1944

1944

1944

1944

1944

1944‘

1945

1945

1945

1952

56

 
USGS Cenozoic
locality
No.

Description Collector

Date
collected

 
Menlo Park,

Calif. Register

M3856 ______ Lat 45°51.7’ N., long 123°13.4’., along
private forest read 300 in northeast
ofjunction of Kenusky Creek and
East Fork of Nehalem River,
Columbia County. Middle of Pitts-
burg Bluff Formation.

M3857 ,,,,,,
private forest road 900 m southeast
ofjunction of Kenusky Creek and
East Fork of Nehalem River.
Columbia County. Middle of
Pittsburg Bluff Formation.

M3858 ,,,,,,
private forest road near divide
between East Fork Nehalem River
and North Scappoose Creek, 200 in
north of bench mark 1232. Columbia
County. Near top of Pittsburg Bluff
Formation,

Lat 45°55.0’ N., long 123°08.0’ W.,
along private forest road 750 in
northeast of bench mark 580, which
is about 1 km north of Pittsburg on
Oregon State Highway 47. Columbia
County. Base of Pittsburg Bluff
Formation.

Lat 45°43.6’ N., long 123°11.1'W.,
along Spokane, Portland, and Seattle
Railroad, 200 111 north of Hares
Canyon. Washington County. Near
top of Pittsburg Bluff Formation.

Lat 45°43.4' N., long 123°11.1’ W.,
along Spokane, Portland, and Seattle
Railroad, 200 m south of Hares
Canyon. Washington County. Near
top of Pittsburg Bluff Formation

Lat 45°43.3’ N., long 123°11.1’ W.,
along Spokane, Portland, and Seattle
Railroad, 400 m south of Hares
Canyon. Washington County. Near
top of Pittsburg Bluff Formation.

Lat 45°48.6’ N., long 123°08.4’ W.,
along logging road on south side of
Coal Creek, 350 m east of ﬁrst tribu—
tary to south. Columbia County.
Upper middle of Pittsburg Bluff
Formation.

Lat 45°48.9' N., long 123°08.0' W.,
along logging road 50 m east of ﬁrst
tributary to Coal Creek to north and
1,000 m northeast ofjunction of the
tributary with Coal Creek. Columbia
County. Upper middle of Pittsburg
Bluff Formation.

Lat 45°51.5’ N., long 123°09.0’ W.,
along logging road on south side of
second valley north of Coon Creek,
16 km east of Oregon State High-
way 47 where it turns west to become
the main street of Vernonia.
Columbia County. Middle part of
Pittsburg Bluff Formation.

Lat 45°51.0’N., long 123°06.6’ W.,
from roadcut along East Fork of
Nehalem River, 650 in northwest of
conﬂuence of Jim George Creek, and
100 in south of main road. Columbia
County. Middle of Pittsburg Bluff
Formation.

Lat 45°52.4’ N., long 123°07.5’ W.,
from roadcut along main road that
follows East Fork of Nehalem River
directly west of conﬂuence of Dog
Creek. Columbia County. Middle of
Pittsburg Bluff Formation.

M3 860 ,,,,,,

M3866 ,,,,,,

M3868 ,,,,,,

M3869 ______

M3871 ______

M3872 ,,,,,,

M3874 ,,,,,,

M3877 ,,,,,,

M3878 ,,,,,,

Lat 45°51.2’ N., long 123°13.7’ W., along ,,,,,,,,,, do ,,,,,,,,,,

Lat 45°50.2’ N., long 123°02.7’ W., along ,,,,,,,,,, do ,,,,,,,,,,

E. J. Moore

1968

iiiiiiiiii doﬂuuuu 1968

,,,,,,,,,, do,,,,,,,,,, 1968

,,,,,,,,,, do,,,,,,,,,,

1968

.......... do_.,,,,,,,,

1968

,,,,,,,,,, do,,,,,,,,,, 1968

 
OLIGOCENE MARINE MOLLUSKS FROM THE PITTSBURG BLUFF FORMATION IN OREGON

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(London), V. 7, pt. 2, p. 331—349.

 
Page
A

Abbreviations ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3
abrupta, Panopea ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 53
acala, Leda ,,,,,,,,,,,,,,,,,,,,,,,,,,, HH H 43
(Acharax) willapaensis, Solemya ,,,,,,,,,,,,,, 20
Acila ,,,,,,,,,,,,,,,,,,,,,, 14, 18, 20, 21,42, pl. 17
decisa ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3, 22
gettysburgensis zone ,,,,,,,,,,,,,,,,,,,,,,, 3, 4
nehalemensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 24
shumardi HH 1, 2, 3, 4, 5, 6, 8, 21, 24, 28,42, 43
biozone ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2, 9
Zone ,,,,,,,,,,,,,,,,,, 1, 2, 5, 6, 8, 9, 23,24
deﬁned ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2
(Acila) gettysburgensis ,,,,,,,,,,,,,,,,,,,,,, 43
(Truncacila) ,,,,,,,,,,,,,,,,,,,,,, 17, 18, 22, 43
nehalemensis ______________ 20, 21, 23, 28, 43
minima ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
shumardi ,,,,,,,,,,,,,,, 2, 14, 15, 16, 19; 21,
23,24, 26, 28, 42, pl. 8
type locality ,,,,,, 2

(Avila) decisa, Nucula ,,,,,,,, HH

getiysburgensis, Acila ,,,,,,,,,,,

 
shumardi, Nucula
Acrilla ,,,,,,,,,,,,,,,,,,
(Ferminoscala) becki

 
dickersoni ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Acteocina chehalisensis ,,,,,,,,,,,,,,,,,,,,,,,,,, 40
Acteon ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18, 20, 40

chehalisensis ,,,,,,,,,,,, 11, 15, 16, 26, 40, pl. 7
parvum ,,,,,,,,,,,,,,,,,,,,,,,,, 28, 40, 41
sp _____ H, 15,41,pl,7
Acteonidae H H
acutilineata, LacinomaH ,,,,,,,,,,,,,,, 28, 46
Addicott, W. 0,, cited ,,,,,,,,,,, 23, 24
addicolti, Aforia Hi ,,,,,,,, 38

 
aduncanasa, Tellina __
Tellina (Eurytellina)

H 8, 21, 28, 50
14,15, 16, 26,50, pl. 11

 
Aforia ,,,,,,,,,,,,,,, 17, 18, 19, 20, 37
addicolti ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
campbelli ____________________ 11, 15, 26, 37, pl. 7
clallamensis , H, 38

wardi H. . 16,37
wardi 11111111111111 L 38

Agasoma acuminatum beds ,,,,,,,,,,,,,,,,,,,,,,,, 4

columbiana ,,,,,,,,,,,,,,,,,,

columbianum H ,
Alaska Peninsula, Oligocene fossils ,H
albensis, Nucula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
albus, Polinices ,,,,,,,,,,,,,,,,,,,,,

 
aldrouandi, Panope ,,,,,,,,,,,,,,,,,

Alegria Formation ,,,,,,,,,,,,,,,,,,,,,, 8, 24, 25, 28
Calif ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 43, 49
fauna ,,,,,,,,,,,,,,,,,,,,,,,,,,, 8, 24

Algae, coralline ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20

Alsea Bay, Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 9, 10

Alsea Formation ,,,,,,,,,,,,,,,,,,,,,,,,,, 10, 36, 44
mollusks ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23, 25, 28
Newport area ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23, 28
Greg ______________ 10, 32, 34, 37, 43, 45, 46, 47,

48, 49, 50, 52, 53, 54

Alvania ________________________________________ 21

Analina leana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 53

Ancilla ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23

angustata, Ataria ________________ 15, 16, 54, pl. 15

anguslatus, Nautilites ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 54
Nautilus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 54

annalata, Lucinoma ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46

 
INDEX

[Italic page numbers indicate major references]

Apalymetis ,,,,,,,,,,,,,,,
Arca ,,,,,,,,,,,,,,,,,,,,,
montereyana Zone ,,,,,,,,,,,,,,,,,,,,,,,,,,

nuculeus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
Architectonica ,,,,,,,,,,,,,,,,,,,, 16, 17, 19, 20, 29
blanda ,,,,,,,,,,,,,,,,,, 11, 15, 16, 26, 29, pl. 1
Architectonicidae ,,,,,,,,,,,,,,,,
arctica, Yoldia HH
(Arenomya) kusiroensis, Mya HH
Arroyo Ciervo area, Calif ,,,,,,,,
Arthropoda ,,,,,,,,
Asteroidea ,,,,,,,
Astoria Formation ,,,,,,,,,,,,,,,,,, 4, 29, 30, 31, 43
Oreg ,,,,,,,,,,,,,,,,,, 30, 31,33, 36, 38,45, 54
Wash
Astraea
Astropecten sp ,,,,,,,,,,,,
Ataria ___________________
anguslata

 
,,,,,,,, 15, 16, 54, pl. 15
ziczac ,,,,,,,,,,,,,,,,,,,,, 54
australis, Scalaria ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 30

 
bainbridgensis, CochlodesmaH 14, 15, 16, 26,53, pl, 16

Barbatia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21
merriami Zone ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 4
Bastendorf [Bastendorff] Formation ,,,,,,,,,,,, 6, 24
[Bastendorff] Shale ,,,,,,,,,,,,,,,,,,,,,, 5, 6, 7
Bastendorff Shale ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 22, 23

foraminifera _ .
mollusks , , , ,
southwestern Oregon 1

 
Balhybembix ,,,,,,,,,,,,,, , 29
becki, Acrilla (Ferminoscala) ,,,,,,,,,,,,,,,,,, L 28
bentsonae, Gemmula ,,,,,,,,,,,,,,,,,,,,,,,, _ 28
bigelawii, Braarudosphaera ,,,,,,,,,,, _ 25
Biozone, deﬁnition ,,,,,,,,,,,,,,,,,,, L 2
biplicatus, Molopophorus ________ , 35
quadranodosum, Malopophorus _ 35
bisectus, Dictyococcites ,,,,,,,, , 25
Blakeley beds _________ _ 6
Blakeley Formation, Oreg .H.
Wash ,,,,,,,, 10, 30, 32, 36, 39,43, 44,45, 46, 47,
50, 54, 55
Blakeley horizon ,,,,,,,,,,,,, , 4, 5
Stage ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7, 9
blakeleyensis, Turritella diversillneata ,,,,,,,,,,,, 30
blanda, ArctheclonLca ,,,,,,,, 11, 15, 16, 26,29, pl, 1
borealis, Cardila ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45
(Boreascala) condoni, Epitonium ,,,,,,,,,,,,,,,,, 28
condoni eugenense, Epitonium H, __________ 28
oregunensis, EpitorLL'um ,,,,,,,,,,,,,,, 28
keaseyense, Epitonium ,,,,,,,,,,,,,,,,,,,,,,,, 31
Braarudosphaera bigelowii ,,,,,,,,,,,,,,,,,,,,,, 25
Brisasler ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
maximus LLLLLLLLLLLLLLLLLLLLLLLLLLLLLLLLLLLL 20
Brisingid sp ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
Bruclarkia ________________ _ 16, 19, 20, 22,34
columbiana ........ 1, 2, 5, 6, 9, 11, 14, 15,21, 23,
24, 26, 28, 34, pl. 3
columbianum ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8, 28
uokesi ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
brunnea, Natica ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 32
Buccinidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 35
Bukry, David, cited ,,,,,,,,,,,,,,,,,,,,,,,,,, 24, 25
Bulla lignaria ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 41
Bullia (Molopophorus) striata ,,,,,,,,,,,,,,,,,,,, 35

 
Page
C
California, Oligocene fossils ,,,,,,,,,,,,,,,,,,,,,, 19
californica, Easiphonalia ,,,,,,,,,,,,,,,,,,,,,, 33, 34
Callisla ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 18, 19, 20, 48
cathcarlensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 49
densa
harnii
nimbosa ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 49
pittsburgensis ______ 1, 4, 5, 6, 8, 21, 23, 28, 48, 49
sp ,,,,,,,,,,,,,,,,,,,,,,,,
(Macrocallista)
nimbosa ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 48
pittsburgensis HH 3, 15, 16, 19, 26,48, pl, 12
(Callista) pittsburgensis, Meretrix ,,,,,,,,,,,,,,,, 48
Calyplraea ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 22, 23
diegoana ,,,,,,,,,,,,,,,,,,,,,,,,,
sookensis ,,,,,,,,,,,,,,,,,,,,,,,,,
Calyptraeidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 31

campbelli, AforLa H, H, 11, 15, 26,37, pl. 7

 
Canada de Santa Anita, Calif ,,,,,,,,,,,,,,,,,,,, 23
Cancellaria ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22
sp LLLLLLLLLLLLLLL

 
Cardiidae

Cardiomya ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22

Cardita borealis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45

Carditamerinae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,

Carditidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,

Cardium coaperii lorenzanum ,,,,,,,,,,,,,,,,,,,, 47
lorenzanum ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 47
semiasperum H
solidum

carinala, Spirotropis

Caryophyllia sp ,,,,,,,,,,,,,,

castrensis, Nucula

cathcartensis, Callista ,,,,,,,,

Centrascymnus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17

Cephalopod ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 15, 16

Cephalopoda ,,,,,,,,,,,,,,,,

Chehalis River, Wash ........

chehalisensis, Acteocina ,,,,,,,,,,,,,,,,,,,,,,,,,, 40
Acteon ,,,,,,,,,,,,,,,,,, 11, 15, 16, 26, 40, pl. 7
Priscofusus ,,,,,,,,,,,,,,,,,,,

Yoldia (Portlandella) ,,,,,,,,,,,,,,,,,,,,,,, 20

Chiasmolilhus oamaruensis ,,,,,,,

chione, Venus

Cibicides hadgei ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8

Clallam Formation ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3

Clallam Stage ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 9

clallamensis, Aforia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
wardi, Aforia ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 16, 37

clarki, Pitar (Lamelliconcha) ,,,,,,,,,,,,,,,,,,,,,, 28
Selena ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52

Clatskanie, Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7, 35

clausa, Cryptonatica ,,,,,,,,,,,,,,,,,,,,,,,,,,,,
Natica H,

 
Clavella gravida ,

 
Clavinae ,,,,,,,,,,,,,,,,

(Cnestrium) oregona, YoldLa ,,,,,,,, 44

Coal ,,,,,,,,,,, . 7, 18, 19

Coal Creek, Oreg ,,,,,,,,

Coaledo Formation, Oreg _ 31

Coast Ranges, California H H H 8

Coccoliths ,,,,,,,,,,,,,,,,,,, , 9, 25
planktonic ,,,,,,,,,,, 25

Coccalithus eopelagicus H . 25
pelagicus LLLLL L 25

Cochladesma ,,,,,,,,,,,,,,,, 17 18, 20, 53

61

62

 
Page
Cochlodesma—Continued.
bainbridgensis ,,,,,,,,,, 14, 15, 16, 26,53, pl, 16
cacoaensis, Uvigeriria ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8
Coelenterata ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
colimana, Opalia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 31
Collections, preparation ,,,,,,,,,,,,,,,,,,,,,,,,,, 2
Columbia County, Oreg.,
stratigraphic section ,,,,,,,, . 2, 5
columbiana, Agasama ,,,,,,,,,,,,,,,,,,,,,,,,,,, 3
Bruclarkia ,,,,,,,,,,,, 1,2, 5,6,9, 11, 14, 15,21,

23, 24, 26, 28, 34, pl, 3
Drillia ....... . ...,............. 38,39

 
Lucina ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
Lucinomu ,,,,,,,,,,,, 8, 14, 15, 16, 26,45, pl. 10
Salem: (Eosolen) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52
Taranis ,,,,,,,,,,,,,,,,,, 11, 14, 15, 26,38, pl, 7
Thesbia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
Turcicula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29
columbianum, Agasoma ,,,,,,,,,,,,,,,,,,,,,,, _ 34
Bruclarkiu ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8, 28
Phacoides ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45

condoni, Epitonium (Boreoscala) .. .._ . 1.

 
eugenense, Epitonium (Bareoscalu) ... 28
oregonensis, Epitonium (Bareoscala) ,,,,,,,,,, 28
Thracia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21, 28, 54
(Thracia) ,,,,,,,,,, 14, 15, 16, 26, 54, pl. 16

Conger eels ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17

Congridae 1......1...

conradi, Solen ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52
consimilis, Quercus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21
Conus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22
cooperii larenzanum, Cardium ,,,,,,,,,,,,,,,,,,,, 47
Ynldia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44
(Kalayoldia) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
Coos Bay, Oreg ,,,,,,,,,,,,,,,,,,,,,,,, 22, 25, 28, 5O
Coral ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21
Corbis ,,,,,,,,,,

 
corbuloides, Thracia
corrugatum, Perse
Cowlitz Formation, Wash
Crabs

  
crenala, Turbo ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 30

Crenelia ,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18, 19, 22, 45
porterensis ,,,,,,,,,, 11, 15, 16, 19, 26, 45, pl. 12
washingtonensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45

Crenellinae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45

Crepidula .1... . .. ... ..,.....1... 16, 17, 20, 31, 40
pileum ,,,,,,,,,,,,,,,,,, 11, 15, 16, 26,31, pl. 1
ungana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
(Spirocrypta) pileum ,,,,,,,,,,,,,,,,,,,,,,,,, 3]

Crinoid Beds, Keasey Formation ,,,,,,,,,,,,,,,,,, 7

Crinoidea

Crinoids

Crustacea

 
Crypta (Spirocrypta) pileum ....
Cryptonatica ,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 19, 20, 31

 
clause ............... ,,,,,,,,,,,,,,,,,,,,, 31

oregonensis.. .. ... ., . 1 _ . ..-.......... 31

pittsburgensis .... ,,,,, 11, 14, 15, 26,31, pl. 1
Cyathodonta ............................... .- 53
Cyclicargolithus ﬂoridanus ...................... 25
Cyclncardia .......................... 17, 18, 20, 45

hannai..... ...1 ...................... 45

hannibali ............ ,

subtenta ..........

 
(Cyclocardia) hunnibali ..-. 8, 11, 15, 16,45, pl, 9
(Cyclocardia) hannibali,

Cyclocardia . ..... 8, 11, 15, 16, 45, pl, 9

Cylichnina . ................................... 22

turneri .................................. 22, 28

Cymric Shale Member ...................... 9, 25, 28
Calif ..................................

 
Cypraea ................... ... ....

    
D
Dall, W, H., cited . .. .... 23
dalli, Molopnphorus . 6, 8, 24, 28, 35
Pitar .......... -. ... 47
(Pitar) . 15, 16,26, 28,47, pl. 12
Pitaria ...................................... 47

 
INDEX
Page
Davilinae 1 ................................... 50
decisa, Acila .................................. 3, 22
Nucula..- ......................... 42

   
(Acila) _-
decussatus, Mytilus
Deer Island, Oreg -
Delectopecten --.

 
sp .....

densa, Callisto 111111

Dentaliidae .................................... 41

Dentalium .................................. 16, 41
elephantinum .........................
ergasticum ...........................
laneensis .................................. 9, 42
porterensis .................................. 22
(Fissidentalium) .......................... 17, 18

laneensis .-.. . 14, 15, 16, 26, 28, 41, pl. 7

 
Dentiscala ........ . 1 .................. 30
(Dentiscala), Opalia ............................ 18
hertleini, Opalia ...... -- 11, 15, 16, 26, 30, pl, 3
Diatoms ................................... 20
dickersoni, Acrilla (Ferminoscala) ................ 28
Suauodrillia ................................ 40
Surcula .................................... 40
Dictyococcites bisectus ............................ 25
scrippsae .................................... 25
diegoana, Calyptraea ____________________________ 28
Diller, J, S,, cited ................
Diplodonta ......................
parilis .................................. 28, 46
divaricata, Nucula ._ _ _________________________ 42
diversilineata blakeleyensis, Turritella ............ 30
Drillia columbiana .......................... 38, 39
kennicotti .................................. 39
duplicata, Neverita .............................. 19
Durham, J. W., cited ............................ 24
E
Echinoderms ........................... 17
Echinoidea .............................
Echinoids ................................ 8, 20, 21
Echinophoria ................................ 20, 22
rex Zone .................................... 9
Ecology ...................................... 16‘
edulis, Mytilus .................................. 44
Eelg‘rass ....................................... 21
elephantinum, Dentalium ........................ 41
Ennucula ...................................... 22
sp .......................................... 20
Eocene, provincial correlation ____________________ 25
Eocene-Oligocene boundary ...................... 24
eacernua, Ocotea ................................ 21
eopelagicus, Coccolithus .......................... 25
Eosiphonalia .......................... 16, 19, 20, 33
Californian 111 ........................ 33, 34
oregonensis .-. ...... 3, 11, 15, 16, 26,33, pl, 4
washingtonensis .......................... 33, 34
(Eosiphomzlia) oregonensis, Siphonalia ............ 33
Eosolen .................................. 16, 18, 52
(Eosolen) columbiana, Salem: .................... 52
eugenensis, Selena -- 14, 15, 16, 26, 28, 52, pl. 13
Epitoniidae ...................................... 30
Epitonium .................................. 20, 22
keaseyensis ............................. 20

 
(Boreoscala) condoni - . . -
condoni eugenense

 
oregonensis .......

keaseyense .........
ergasticum, Dentalium .......................... 41
Emilia ................................ 17, 18, 20, 50
oregonensis ............... 15, 16, 26,50, pl, 16
Eugene, Oreg .......................... 21, 25, 52
Eugene Formation .............. 1, 3, 5, 6, 7, 10, 23,
25, 28, 35, 43, 44
age ....................................... 29
fauna ............................ 8,21,22,28
lithology ................................ 21, 25
Oreg ........ 3, 10, 32, 33, 34, 41, 42, 43, 44, 45,

46, 47, 48, 49, 50, 51, 52, 53, 54, 55
eugenense, Epitonium (Boreoscala) condani ........ 28

 
Page
eugenense—Continued.
Paruicardium .........
eugenensis, Modiolus _________________________ 28
Solen ...................................... 52
Solena .................................. 21, 52
(Eosolen) ........ 14, 15, 16, 26, 28,52, pl, 13
Spisula .................................. 28, 50
eugenia, Tellina --
E urytellina ........
(Eurytellina), Tellina ........................ 17, 18
aduncanasa, Tellina ____ 14, 15, 16,26, 50, pl, 11
Exilia .................................... 20, 22, 23
lincolnensis .............................. 20, 28
F
Fasciolariidae .................................. 36
Fauna, Eugene Formation ...................... 23
Gries Ranch Formation ............... 6, 21, 23
Holocene .................................... 17
Keasey Formation ____________________ 19, 20, 23
Pittsburg Bluff Formation ________ 2, 3, 11, 16, 17,
19, 20, 22, 23
Stepof Bay, Alaska ____________________________ 7
Tunnel Point Sandstone ______________________ 22
Faunas, Oligocene ................................ 2
Paciﬁc coast... .......................... 2, 9
(Felania) usta, Mysia ............................ 46
Feloniella ............................ 17, 18, 20, 46
goodspeedi ______________________________
griesensis
parilis ...........................
serricata .........................
snavelyi ................................ 46, 47
(Feloniellu) snavelyi 1... 14, 15, 16, 26, 46, pl, 10
(Felaniella) snauelyi, Felaniella ........ 14, 15, 16, 26,
46, pl. 10
(Ferminoscala) becki, Acrilla ................... 28
dickersoni, Acrilla ........ 28
Ficus

modesta
ﬁlosa, Lucina 1 1 _ _
F imbria

 
Fish ............
Fish scales ......
Fisher Formation ................................ 7
ﬁshii, Molopophorus ............................ 28
Fissidentalium ................
(Fissidentalium), Dentalium ..--
laneensis, Dentalium .......... 14, 15, 16, 26, 28,
41, pl, 7
F issurella ...................................... 19
Fitch, John, cited ................................ 17
F labellum ...................................... 21
hertleini .. .. ........................ 20
ﬂoridanus, Cyclicargolithus -. .................. 25
Foraminifera ..................... 5, 7, 8, 9, 20, 22
Bastendorff Shale ............................ 22
planktonic ............................ 9, 17, 25
Refugian Stage .......
stages .................
upper Refugian Stage ........................ 6
zones
Formations, Oligocene, California ...........
fornicata, Patella ..........................
Fossil localities, US. Geological Survey,
Pittsburg Bluff Formation ............ 55
Fossils, collection .............................. 2, 14
Ball identiﬁcations .......................... 3
ﬁsh ........................................ 17
fragments .............................. 17, 18
locality numbers ........................... 2
Pittsburg Bluff Formation ................... 7
plant leaves .................................. 8
preparation ................................ 2, 3
San Lorenzo Formation ..................... 3
sea urchin ................................. 5
Fresno County, Calif .............................. 6
Fulgurofusus .................................... 22
sp ....................................... 20
Fusinidae ..... 36

 
Page

Fusinus (Priscofusus) stewarli ,,,,,,,,,,,,,,,,,,,, 36

Fusus geniculus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 36
G

gabbi, Molopophorus ____________ 1, 2, 3, 5, 11, 14, 15,

16,23, 24, 26,35, pl. 5
Galvin Station, Lewis County,

   
Wash ______________ 39, 40, 43, 44, 45, 47

Gastropoda ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29

Gastropods ,,,,,,,,,, 11, 14, 15, 16, 17, 18, 19, 20, 21,

22, 23, 26, 28

Gaviota Formation ______________________________ 24
fauna ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8, 24

Gemmula ___________________________ 20, 22
bentsanae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28

geniculus, Fusus ____________________________ 36

gettysburgensis, Acila (Acila) ____________________ 43

gigantea, Venus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 48

Globigerinids ,, W 17

Glossaulax ,,,,,,

(Glossaulax), Neueriia ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 18
reclusiana, Neuerita ,,,,,,,,,,,,,,,,,,,,,,,,,, 19
thomsonae, Neverita ______ 11, 14, 15, 26,32, pl, 2

Glycymeris ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21

glycimeris, Mya ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52

goodspeedi, Felaneilla ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
Taras ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46

Gorgonid coral ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20

gravida, Clauella ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 34

Grecco Ranch House ,,,,,,,,,,,,,,,,,,,,, ., _,, 4

Gries Ranch Formation ,, 4, 5, 6, 21, 23, 24, 25, 35, 43
deposition ,,,,,,,,,,,,,,,,,,
equivalent ,,,,,,,,,,,,,,,,
fauna
Oreg ,

Wash __________ 6, 31,32, 33,40, 41, 44, 51, 52

Gries Ranch horizon
griesensis, Felaniella , _
Gyrineum ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20,

H

Habitats, mollusks ,,,,,,,,,,,,,,,,,,,,,,,, 17, 18, 19
Haliotis
haliotoidea, Helix ,,,,,,,,,,,,,,,,
hannai, Cyclocardia ______________
hannibali, Cyclocardia
Cyclocardia (Cyclocardia) W 8, 11, 15, 16, 45, pl. 9
Lucinoma ,,,,,,,,,,,,,,,,
hanniballi, Nucula ,,,,,
haydani, Planulina A
Helix haliotoidea W,
Hemifusus washingtoniana ,,,,,,
(Here), Lucimz
hertleini, Flabellum ,,,,,,,,,,,,,,
Opalia (Dentiscala)
Suauodrillia ,,,,,,,,
(Heteromacoma) uancouverensis, Macoma
Hiatellidae ______
History of investigation ,
hodgei, Cibicides 1
hornii, Callista _.,,
hyperborea, Yoldia ,,,,,,,

 
I
inquinala, Macoma ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Introduction ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, I
Isocrinus _______________________________________ 20
nehalemensis _______________________________ 20
oregonensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
Isthmolithus recurvus ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 25

J

jamesae, Neuerita ,,,,,,,,,,,,,,,,
Japan 11111111111111111111111111
Jones Beach ,,,,,,,,,,,,,,,,,,,,
jasephinia, Neverita ,,,,,,,,,,,,,,

 
INDEX

Page
K

Kalayoldia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44
(Kalayoldia), Yoldia ,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
cooperi, Yoldia 111111111111111111111111111111 19
oregona, Yoldia ,,,,,,,, 14, 15, 16, 26, 28, 44, pl. 9
Keasey Formation ,,,,,,,,,,,, 3, 5, 6, 7, 8, 10, 11, 19,
21, 23, 24, 25

 
coccoliths
deposition ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7
fauna ,,,,,,,,,,,,,,,,,,,,,, 19, 20, 21, 22, 23,28
mollusks ,,,,,,,,,,,,,,,,,,,,,,, , "H 28, 29
northwestern Oregon ________________________ 23
Oreg ,,,,,,,,,,,,,,,,,,,,,, 10, 33, 41, 45, 47, 55
Vernonia area ,,,,,,,,,,,,,,,,,,,, 19, 20, 21, 30
volcanic ash ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21
Keasey Shale ________________________________ 1, 6
Keasey Stage ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7, 9
keaseyensis, Epitoniuml __________________________ 20
Epitonium (Boreascala) ,,,,,,,,,,,,,,,,,,,,,, 31
Keenaea ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 47
(Keenaea), Nemocardium ______________________ 17, 18
lorenzanum, Nemocardiumg14, 15, 16, 26,47, pl. 10
kennicotti, Drillia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 39
kincaidi, Spirotropis ,,,,,,,,, 11, 14, 15, 26,39, pl. 7
Turricula ,, 39
Turris ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 39
Kirker Formation, Calif ,,,,,,,,,,,,,,,,,,,,,,,,,, 43
Kirker Sandstone ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8
Kirker Tuff ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 4, 25, 28, 49
Kleinpell, R. M., cited ,,,,,,, H 24
quoted ,,,,,,,,,,,,,,,,, H 23
K nefastia _____________ ,_ 22
Kreyenhagen Formation 9
Kreyenhagen Shale ,,,,,,,,,, A 4, 6
Calif ,,,,,,,,,,,,,,,,,,,, 44, 49
kusiroensis, Mya (Arenomya) _ W 28
L
Lacia u , 42
laevis, Pandora (Pandora) _ , 28
(Lamelliconcha) clarki, Pitar, __ 28
laneensis, Dentalium ,,,,,,, __- 9, 42
Dentalium (Fissidentalium) ________ 14, 15, 16, 26,
28, 41, pl, 7
leana, Anatina _
Leda acala ,,,,,
lincolnensis
oregona
washingtonensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 43
Leionucula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
(Leionucula), Nucula ________________________ 17, 18
nuculana, Nucula ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
vokesi, Nucula ,,,,, ____ 14, 15, 16, 26, 42, pl. 8
lignaria, Bulla ,,,,,,,,,,,,,,,,,,,,,,,,,,, L-.. 41
Lima ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22
Lincoln Creek beds ,1" 4
Lincoln Creek Formation ,,,,,,,,,,,,,,,,,,,, 25, 45

Wash ,,,. 8, 10, 24, 28,29, 30, 31, 32, 33, 34, 35,
36, 38, 39, 40, 41, 43, 44, 45, 47,48, 49, 53, 55

Lincoln Formation ,,,,,,,,,,,,,,,,,,,,,,,, 4, 35, 38
Lincoln horizon ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 4, 5
Lincoln [Lincoln Creek] Formation -- 3, 5, 6, 8, 23, 24
Lincoln Stage ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7, 9

 
lincolnensis, Exilia
Leda ______________
Molopophorus , , ,,
Natica ,,,,,,,,,,,

  
Polinices ,,,,,,
washingtonensis ____________
(Polinices) washingtonensis H

Selena ___________________

Tellina (Moerella) _________

Liracassis _________________

Litorhadia ,,,,,,,,,,,,,,, 16, 19, 20, 43
washingtonensis W" 8, 14, 15, 16, 21, 26, 43, pl. 9

Long Island, NY ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19

 
lorenzana, Solena __________________
lorenzanum, Cardium ,,,,,,,,,,,,,,
Cardium cooperii ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 47
Nemocardium ,,,,,,,,,,,,,,,,,,,,,, 8,19,21,47
(Keenaea) __________ 14, 15, 16, 26, 47, pl. 10
Lorenzian Stage ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 9
Loxocardium ________________________________ 21, 23
Lucina columbiana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
ﬁlasa ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45
(Here) ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23
Lucinidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45
Lucinoma ____________________________ 17, 19, 20, 45
acutilineata ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28, 46
annulata ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
columbiana ,,,,,,,,,, 8, 14, 15, 16, 26,45, pl, 10
hannibali __________________________________ 46
M
Macorna ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22, 23
inquinata ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
(Heteromacoma) vancouuerensis ,,,,,,,,,,,,,, 28
Macracallista ____________________________ 48, pl. 17
piltsburgensis ,,,,,,,,,,,,,,,,,,,,,,,,,, 2, 9, 48
community ,,,,,,,,,,,,,,,,
(Macrocallista), Callista ,,,,,,,,,,,,
nimbosa, Callista ____________________________ 48
pittsburgensis, Callista .......... 3, 15, 16, 19, 26,
48,‘pL 12
Macrouridae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17
Mactra ovalis ,,,,,,,,,,,,,,,,,,,,,, W 49
pittsburgensis 6
solida ......
Mactracea __.
Mactridae H,
Mactromeris ,,,,,,,,
(Mactromeris), Spisula 1, W 17, 18, 50
pittsburgensis, Spisula __ ,,,,,, 14, 15, 16, 26,
49, pl. 14
ueneriformis, Spisula ______________ 11, 15, 16, 26,
50, pl, 14
Malletia ___________ 1 __ 20
mamillaria, Natica , 32
Margaritan Stage ,,,,,,, 9
Marrowstone Shale, Wash ,,,,,,,,,,,,,,,,,,,, 34, 48
Martesia

sp ,,,,,,,
maximus, Brisaster
Megafaunal zones, Tertiary .1-
Meretrix (Callista) pittsburgensis ,,,,,,
merriama, Nuculana

 
Mesodesmatidae
minima, Acila (Truncacila) nehalemensis _____
Minormalletia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 22
sp ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
Miocene, provincial correlation ,,,,,,,,,,,,,,,,,, 25
Mist, Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,, 2, 5, 11,20, 21
Mitra ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22
modesta, Ficus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Modiolus
eugenensis ,,,,,,,,,
(Maerella) lincolnensis, Tellina ,,,,,,,,,,,,,,,,,,,, 28
Mollusca ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29
Mollusks, Alaska ,,,,,,
Alsea Formation ,,
Asiatic origin ______
Bastendorff Shale“
Calif ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 6 8
faunal zones ______________________________ 14
fragments ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
habitats ,,,,,
infaunal community ,,,,,,,,,,,,,,,,,,,,,,,, 17
Keasey Formation ,,,,,,,,,,,,,,,,,,,,,,,, 28, 29
Lincoln Stage 9
Newport area _____________
Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8
Paciﬁc Coast ______________ 9, 23
Pittsburg Bluff Formation "H 2, 7, 11, 14, 16, 19,
20, 22, 25, 28
distribution

 
post-late Eocene

64

Mollusks—Continued.
stages _____________________
taxonomy
Tertiary, Calif 111
Tertiary formations 11
Tunnel Point Sandstone

 
Twin River Formation 1 8
zones _____________________________________ 9
Molopophorus ,,,,,,,,,, 19, 20, 35, pl. 17
biplicatus ,,,,,,,,,,,,,,,,,,,,,, 35
quadranadosum ,,,,,,,,,,,,,,,,,,,,,,,,,, 35
dalli ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 6, 8, 24, 28, 35
ﬁshii ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
gabbi ,,,,,,,,,,,,,,,,,, 1, 2, 3, 5, 11, 14, 15, 16,
23, 24, 26, 35, pl. 5
Zone ,,,,,,,,,,,,,,,,,, 2, 6, 7, 24, 34, 35, 37
of Durham ,,,,,,,,,,,,,,,,, 7
lincolnensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 35
Zone ,,,,,,,,,,,,,,,,,,,,,,,,,, 11 3, 4, 5
stephensoni Zone ,,,,,,,,,,,,,,,,,,,,, 6, 37
(Molopophorus) striata, Bullia 11
Monterey Bay, Calif ,,,,,,,,,,
Montereyan Stage
Montesano horizon ,,,,, 4
Moody Shale Member,
Toledo Formation ,,,,,,,,,,,,,,,,,,,, 7
rnorchi, Trophon _______
Muricacea _____________
Mya ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 22, 54
glycimeris ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52
nitens

 
(Arenomya) kusimensis 1.11
Myrica 5p ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21
Myrteinae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 45
Mysia (Felania) usta ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
Mytilidae ______________________________________ 44
Mytilus ____________________________ 17, 18, 19, 20, 44
decussatus __________________________________ 451
edulis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44
snohomishensis ________________ 14, 15, 16, 28,44
N
Natica brunnea ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 32
clausa ,,,,,,,,,,,

 
lincolnensis
mamillaria ,,,,,,,
tectula ______
washingtonensis
weaveri ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 31
(Natica) sp ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
(Natica) sp1, Natica ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Naticidae
Naticids ,,,,,,,,,,,,,,,,,,,,,,,
Naticinae
Nautilidae ,,,,,,,,,,,,,,,,,,,,
Nautililes angustatus ,,,,,,,,,,
Nautilus angustatus
Nehalem River, Oreg ,,,,,,,,,, 2, 3, 5, 11, 37, 50, 51
Nehalem River Highway,
near Pittsburg, Oreg ,,,,,,,,,,,,,,,, 7
nehalemensis, Acila ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 24
Acila (Truncacila) ,,,,,,,,,,,,,, 20, 21, 23, 28, 43
Isocrinus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
minima, Acila (Truncacila) ,,,,,,,,,,,, 111 28
Neill) oregona ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 111 44
Nekewis 111 20, 22
Nemocardium __________________________ 111 22, 47

 
lorenzanum 1111 .1- 8, 19,21, 47

     
samarangae __1

 
(Keenaea) ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
lorenzanum ________ 14, 15, 16, 26,47, pl. 10

Neptunea ,,,,,,,,,,,,,,,,,,,,,,,,, 1 1. 111 '22
Neptuneidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 111 33
Nestucca Formation ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23
Neuerita ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 16, 18, 20, 32

duplicata ,,,,,,,

jamesae

josephinia ,,,,,,,,,,,,

reclusiana

thamsonae ,,,,,,,,,,,,,,,,,,,,,, 8, 9, 21, 28, 32

 
INDEX
Page
Neverita—Continued,

(Glossaulax) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
reclusiana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
thomsonae 1 1 11, 14, 15, 26, 32, pl. 2

Newport, Oreg .1 25, 28

nimbosa, Callista 1111

Callista (Macrocallista) 1. 48
Venus ,,,,,,,,,,,,,, 11 48
nitens, Mya ,,,,,,,,,, 11 50
Norbisrath, Hans, quoted 111 2

Notorhynchus

 
castrensis
decisa 1 1 1

 
divaricaia 1111

hanniballi ,,,,,,,,,,,

vokesi

(Acila) decisa _________________________________ 42

shumardi ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
(Leionucula) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
nuculana ________________________________ 42

uokesi ,,,,,,,,,,,,,,,, 14, 15, 16,26, 42,13], 8
Nuculana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 16, 22

lincolnensis 4

merriarna

oregona ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44

washingtonensis ____________________ 9, 20, 28, 43

community ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 9
nuculana, Nucula (Leionucula) ,,,,,,,,,,,,,,,,,, 42
Nuculanidae ____________________________________ 43
nuculeus, Arca 1111111111111111111111111111111111 42
Nuculidae
Nye Shale ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 5

O
oamaruensis, Chiasmolithus ,,,,,,,,,,,,,,,,,,,,,, 25
obliquum, Sinum ,,,,,,,,,, 11, 15, 16, 19, 28, 33, pl. 1
obliquus, Solen ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52
Ocotea eocernua ________________________________ 21
Odonlaspis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17
Odostomia ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 16, 17, 20, 40

winlockiana ,,,,,,,,,,,,, 11, 15, 16, 26,40, pl, 3

(Odostomia) winlockiana ,,,,,, 40
(Odostomia) winklockiana, Odoslomia 111 ,,,,,, 40
Olequahia __________________________________ 20, 22

schencki ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Oligocene, climate 1111111111111111111111 4, 6, 8, 9, 19

faunal horizons ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 5

formations ,,,,,,,,,,,,,,,,,,,,,,,,, 6

marine rocks ,,,,,,,,,,,,,, 8

middle, US. Geological Survey

fossil localities ,,,,,,,,,,,,,,,,,,,,,, 55
provincial correlation ,,,,,,,,
Oligocene faunas, Alaska ,,,,,,,, 8

Oreg ,,,,,,,,,,,,,,,,,,,,,,,,

summary ________________

Paciﬁc Coast ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2
Oligocene sea ,,,,,,,,,, 111 7, 14, 19, 21
Oligocene sediments, deposition ________________ 7, 25

Paciﬁc Northwest ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 25
Oligocene-Miocene boundary ,,,,,,,,,,,,,,,,,,,, 24
Oliuella ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
olyrnpicensis, Perse __________________________ 24, 37

quirnpersensis, Perse ,,,,,,,,,,,,,,,,,, 6, 24, 37
Opalia ,,,,,,,,,,,,,,,,,,,,,, 16, 20, 30

colimana 1111 ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 31
(Dentiscala) ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18

hertleini ,,,,,,,,,,,, 11, 15, 16, 26, 30, pl. 3
Operculina sp 11 ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
Opertochasma 11 ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 22

turnerae ______________________ 28
Ophiuroidea _________________________________ 20
Oregon, Oligocene faunas ,,,,,,,,,,,,,,,,,,,,,,,, 19

Oligocene faunas, summary ,,,,,,,,,,,,,,,,,, 23
Oregon City, Oreg ______________________________ 44
oregona, Leda ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44

Neila

 
N uculana 1 1
Yoldia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44

 
Page

oregano—Continued,
(Cnestrium) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 44
(Kalayoldia) ,,,,,,,,,,,,,, 14, 15, 16, 26, 28,
44, pl. 9
(Portlandia) ____________________________ 44
oregonensis, Cryptanatica ________________________ 31
Easiphoualia ,,,,,,,,,, 3, 11, 15, 16, 26, 33, pl, 4
Epitonium (Boreoscala) condoni ,,,,,,,,,,,,,, 28
Ervilia ,,,,,,,,,,,,,,,,,,,, 15, 16, 26,50, pl. 16

Isocrinus 1 1 1 1
Siphonalia 11

 
(Eosiphonalia): ,,,,,,,,
Strepsidura
Turritella ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29, 30
Ostrea ______________________________________ 16, 40
Otoliths ________

oualis, Mactra 11

 
P
Pachydesma ,,,,,, 22
packardi, Plectofrondicularia 20
Spisula 1 22
Pandora 11111111 1 22
(Pandora) laevis 111 1 28
(Pandora) laevis, Pandora 111111111111111111111111 28
Panope 111111111111111111111111111111111111111111 52
aldrouandi 1111111111111111111111111111111111 52
ramonensis 1111111111111111111111111111111111 53
snohomishensis 111111111111111111111111111111 52
Panopea 111111111111111 17, 18, 19, 20,52
abrupta 1.1. 1111111111111111 53
ramanensis 1111111111 9, 14, 15, 16, 26,53, pl. 15
snohamishensis 1111111111 14, 15, 16, 26, 52, pl. 15
(Panapea) ramonensis 111111111111111111111111 28
(Panopea) ramonensis, Panopea 111111111111111111 28
Parasyrinx 11111111111111111111111111111111111111 39
parilis, Diplodonta 11111111111111111111111111 28, 46
Felaniella 1111111111111111111111111111111111 47
Parvicardiurn 111111111111111111111111111111111111 22
eugenense 111111111111111111111111111111111 28
parvuum, Acteon 1111111111111111111111111 28, 40, 41
Patella fornicata 1111111

Pebble Creek 11111111111 6
Pecten 11111111111111111111111111 16, 22, 40
pelagicus, Coccalithus 111 111111111111111 25
Pelecypoda 11111111111111111111111111111111111111 42
Pelecypods 11111111111111 11, 14, 15, 16, 17, 18, 19, 20,
21, 22, 23, 26, 28
Periplomatidae 1111111111111111111111111111111111 53
Perse 1111111111111111111111111 16, 19, 20, 36, pl, 17
corrugatum _1__ 111111111111111111111111111111 36
lincolnensis 11111111111111111111111111111111 28, 37
olympicensis 1 111111111111111111111111 24, 37
quimpersensis 11111111111111111111 6, 24, 37
pittsburgensis 1111111111 6, 11, 14, 15, 16, 24, 26,
36, 37, pl. 6
vernoniensis 1111111111 11, 14, 15, 26, 37, pl. 6

perspectivus, Trochus 111111111

Phacoides columbianum 1111111
Phanerolepida 11111111111111111111111111111111 20, 21
Pholas 111111111111111111111111111111111111111111 22
pileum, Crepidula 111111111111 11, 15, 16, 26,31, pl, 1
Crepidula (Spirocrypta) 1111111111111111111111 31
Crypta (Spirocrypla) 111111111111111111111111 31
Pitar 111111111111111111111111111111 17, 18, 20, 22, 47
dalli 111111111111111111111111111111111111 11 47
(Lamelliconcha) clarki 11111111111111111111 1. 28
(Pitar) dalli 111111111111 15, 16, 26, 28,47, pl, 12
sp 11111111111111111111111111111111111111 28
(Pitar) dalli, Pitar 1111111111 15, 16, 26, 28, 47, pl. 12
sp,, Pitar 111111111111111111111111111111111111 28
Pitaria dalli 111111111111111111111111111111111111 47
Pitarinae 111111111111111111111111111111111111 47, 49
Pittsburg, Oreg 1111111111111111 2, 5, 11, 25, 49, 50
Pittsburg Bluff, Oreg 11. 3
Pittsburg Bluff Formation 1111111 1, 4, 5, 6, 10, 23, 24,
41, 50
age 111111111111111111111111111111111 2, 23, 25, 29
coal 1111111111111111111111111111111111 7, 18, 19
correlation 1111111111111111 2, 4, 5, 6, 7, 10, 24,25

 
Page
Pittsburg Bluff Formation—Continued.

deposition ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
ecology ____________________________________ 16
equivalents ,,,,,,,,,,,,,,,,,,,,,,,,,,, 5, 28
fauna __________ 2, 3, 6, 7, 8, 11, 16, 17, 19,20, 21,
22,41, 47, 50

faunal zones ,,,,,,,,,,,,,,,,,,,,,,
fossil localities __________________________ 10, 55
fossil matrix ____________________________ 17, 18
geographic distribution ,,,,,,,,,,,,,,,,,,,,,, 10
habitats ______________________________ 17, 18, 19
lithology ,,,,,,,,,,,,,,,,,,,,,, 2, 3, 6, 7, 11,25
lower member ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2, 6
mollusks __________ 2, 3, 4, 6, 7, 8, 11, 14, 16, 17,
19,20, 22, 25, 28,29
distribution ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 25
northwestern Oregon ____________________ 10, 23
Oligocene faunas, Oregon ,,,,,,,,,,,,,,,,,,,, 19
Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 33, 34, 35, 37
shale ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3
species checklist ____________________________ 14
stratigraphic sections ,,,,,,,,,,,,,,,,,,,,,,,, 2
stratigraphy ,,,,,,,,,,,,,,,,,, -- 6, 7, 10, 19
terrestrial beds ..-- ._- 6
thickness ,,,,,,,,,, - 7 11 14, 19
type area ,,,,,,,,,,,,,,,,,,,,,,,,, 2, 5, 11, 42
type locality ,,,,,,,,,,,,,, 2,6, 7,11,21,24, 54
upper member ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2
Vernonia area ,,,,,,,,,,,, 19, 20, 30, 31, 33, 37,
38, 43, 49, 51
Pittsburg Bluff sandstone _______________________ 1
Pittsburg Bluffs ,,,,,,,,,, ._ _____ 1, 5
pittsburgensis, Callisto __________ 1, 4, 5, 6, 8, 21, 23,
28, 48, 49
Callisto (Macrocallista) ,,,,,,,, 3, 15, 16, 19, 26,
48, pl. 12
Cryptonatica ,,,,,,,,,,,, 11, 14, 15, 26, 31, pl, 1
Macrocallista 2, 9, 48
Mactra ,,,,,,,,, ..-. 6
Meretrix (Callista) _ __________________ 48
Parse __________________ 6, 11, 14, 15, 16, 24, 26,
36, 37, pl. 6
Spisula ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 5, 24, 28, 49
Spisula (Mactromeris) ____________ 14, 15, 16, 26,
49, pl, 14
Tellina - . 5, 14, 15, 16, 21,26, 28, 51, pl. 11
Turritella _______________ 11, 15, 16, 26, 29, pl. 3
uemaniensis, Perse - 11, 14, 15, 26,37, pl. 6
plagiaulax, Solen ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 52
Plantae ________________________ 20
Planulina haydoni .__ 8
Plectofrondicularia packardl ,,,,,,,,,,,,,,,,,,,,,, 2O
(Plectosalen) townsendensis, Solen ________________ 51
Pleito Formation ,,,,,,,,,,,,,, _ 4
plicatus, Turbo ,,,,,,,,,,,,,,,, __ - 40
Palinices ______________________________ 16, 20, 22, 32
albus -- ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 32
lincolnensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 32
washingtonensis ,,,,,,,,,,,, 8, 11, 14, 15, 21, 26,
28, 32, pl. 1
lincolnensis _____________________________ 32
sp __________________________________________ 20
(Polinices) ,,,,,,,,,,, 17, 18
washingtonensis lincolnensis ,,,,,,,,,,,,,, 32
(Polinices), Polinlces ,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18

washingtonensis lincolnensis,

Polinices ____________________________ 32

Polinicinae . .. .
Porter horizon

    
Porter Shale _____ .. ,,,,,,,,,,,,,,, 7
porterensis, Crenella _____ 11, 15, 16, 19, 26, 45, pl. 12
Dentalium A- ,,,,,,,,,,,,,,,,,,,,,,,,, 22
Turritella ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29, 30
Porterius ____________________________________ 20, 22
(Portlandella) chehalisensis, Yaldia ______________ 20
(Portlandia) oregona, Yoldia ,,,,,,,,,,,,,,,,,,,, 44
Poul Creek Formation _______ __ ... 5, 8, 25
Alaska ______________ 8, 28, 34, 36, 43, 44, 45, 46.

47, 48, 49, 50, 51, 52, 53, 54

mollusks ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 9

Priscofusus __________________________ 16, 19, 20, 36

 
INDEX
Page
Pr'iscofusus—Continued. '
chehalisensis __________ .- _ ,,,,,,,,,, 36
stewarti ,,,,,,,, .. 11, 15, 16, 26,36, pl. 3

 
(Prisca/usus) stewarti, Fusinus
Pristiophorus ,,,,,,,,,,,,,,
Propeamussium -

sp ,,,,,,,,,
Protocardiinae ,,,,,
Pseudacardium ,,,,,

sp ,,,,,,,,,,,,,,,,,
Psychosyrinx ,,,,,,,,,
Puncturella ,,,,,,,,,,,
punicea, Tellina
Purpose and scope ..--
Pyramidellidae _______________

Q

quadranodasum, Molopophorus biplicatus ,,,,,,,, 35
Quercus cansimilis .-
Quimper Sandstone .

 
Wash__ ,,,,,,, 32, 34, 35, 41, 44, 50, 51, 52, 54
quimpersensls, Perse olympicensis ,,,,,,,,,, 6, 24, 37
R
radiata, Tellina ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 50

 
ramonenszs, Panope -
Panopea ,,,,,,
(Panopea) _

Rat tails -
Ray teeth ..__

 
reclusiana, Neverita ,,,,,
Neuerita (Glossaulax)
recurvus, Isthmolilhus_- ,,,,,,,,,,,,,,, 25
Refugian Stage ________ 1, 5, 6, 7, 9, 23, 24
deﬁnition _..
foraminifers
Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 23
type locality ..._ 23, 24
Wash ...................................... 23
Reports dealing with Oligocene Formations
and fossils, annotated chronology ..-- 3
Restoration Point, Wash ........................ 36
Restoration Point horizon ........................ 5
Rices Mudstone Member,
San Lorenzo Formation ........ 8, 44, 47
rosaceus, Solen .................................. 52
S
Salenia ....................................... 20, 21
schencki ................................... 20
samarangae, Nemocardium .................... 47
San Emigdio Canyon, Calif ...................... 5
San Emigdio Formation .............. 4, 5, 6, 28, 32
Calif ........................................ 43
mollusks .............................. 8, 25
San Emigdio Mountains, Calif .................. 5, 9
San Lorenzo Formation ...................... 3, 8, 28
Calif ................................ 33, 36, 54
deposition .................................. 9
foraminifera ............................... 8
members ................................... 8
mollusks .................................. 8, 25
Mount Diablo area .......................... 4
San Lorenzo Group .............
San Lorenzo Series ..............
San Ramon Formation ....
San Ramon horizon .' ...... 5
San Ramon Sandstone, Calif .............. 35, 36, 53
Santa Ynez Mountains, Santa
Barbara County, Calif ............... 23
Santa Ynez Range, Calif ........................ 24
Scalaria australis ................................ 30
Scaphander .......................... 17, 18, 22,41
slewarti ................ 11, 14, 15, 19, 20, 26,28,
41, pl. 7
washingtonensis ............................ 41
Scaphandridae ................................. 41

 
65

   
Page
Scaphopod .................. 14, 15, 16, 17, 18, 26, 28
Scaphopoda .-- _______ 41
Scappoose, Oreg 7

Scappoose Formation _ .. 6, 7, 10, 11, 29
Schenck, H, G., cited ..

quoted .....

 
schencki, Olequahia
Salenia --
Thracia __.
scapulosum, Sinum -. ..
scrippsae, Dictyacaccites
Seastars .....

 
Semele .........
willamettensis .............................. 28
semiasperum, Cardium .......................... 47
sericata, Taras ..........
serricata, Felaniella -
Shark teeth ... .......................... 17
shumardi, Acila ................ 1, 2, 3, 4, 5, 6, 8, 21,
24, 28, 42, 43
Acila (Truncacila) ...... 2, 14, 15, 16, 19, 21, 23,
24, 26, 28, 42, pl. 8
Nucula (Acila) .............................. 42
sicarius, Solen .............................. 28, 51
Siltstone, Newport area, Oreg .................... 9

Siltstone of Alsea .--
Sininae

 
Sinum ................................ 16, 17, 18,33
obliquum ............ 11, 15, 16, 19, 28,33, pl, 1
scopulasum ............................... 33

Siphonalia ................................... 33
oregonensis ............................... 33
(Eosiphonalia) oregoaensis ................. 33

snavelyi, Felam'ella ........................... 46, 47
Felaniella (Felaniella).... 14, 15, 16, 26,46, pl, 10

snohomishensis, Mytilus ............ 14, 15, 16, 28,44
Panape ...................................... 52
Panopea ............... 14, 15, 16, 26,52, pl. 15

Solemya ................. 20, 21, 22
(Acharax) willapaensis ...................... 20

Salen ................................ 17, 18, 20, 51
conradi ..............................
eugenensis ............................
obliquus ................
plagiaulax ..............
rosaceus .........................
sicarius ..........................
townsendensis ......... 14, 15, 16, 26, 51, pl. 13
vagina ................................... 51
(Plectosolen) townsendensis ................... 51

Selena ...................................... 20, 52
clarki ......................................
eugenensis
lincolnensis
lorenzana
(Easolen) columbiana ....................... 52

eugenensis ............ .- 14, 15, 16, 26, 28,
52, pl, 13

Solenidae ...................................... 51

solida, Mactra ................................. 49

solidissima, Spisula ..........................

solidum, Cardium ............................. 49

Sooke Formation ...... 4, 5
Vancouver Island, BC ...................... 46

soakensis, Calyptraea ............................ 28

(Spirocr‘ypta) pileum, Crepidula .......
pileum, Crypta ...................

Spirotropis .................. 17, 18, 20, 21, 22,39
carinata ................................... 39
kincaidi ................. 11, 14, 15, 26, 39, pl. 7
washingtaaensis ..- ...................... 39
(Spirotropisl winlockensis .................... 40

(Spirotrapis) winlockensis, Spiratropis ............ 40

Spisula .............................. 18, 19, 20, 49
eugenensis .............................. 28, 50
packardi ................................... 22
pittsburgensis ..................... 5, 24, 28, 49
solidissima .........
veneriformis .......

(Mactromeris) ........................ 17, 18, 50
pittsburgensis ...... 14, 15, 16, 26,49, pl. 14

66

 
Page
Spisula4Continued,
veneriformis ________ 11, 15, 16, 26, 50, pl. 14
Squalus ,,,,,,,,,,,,,,,,,
Squatina ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17
Stepof Bay, Alaska ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7
Stepovak Formation , 8, 25, 28, 43, 47, 53, 54
Stepovak Series ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8
stewarti, Fusinus (Priscofusus) ,,,,,,,,,,,,,,,,,,,, 36
Prisocofusus ,,,,,,,,,,,,,, 11, 15, 16, 26, 36, pl. 3
Scaphander ,,,,,,,,,,,, 11, 14, 15, 19, 20, 26, 28
41, pl, 7
Strata, Nehalem River ,,,,,,,,,,,,,,,,,,,,,,,,,, 3
Stratigraphic sections, Pittsburg
Bluff Formation ,,,,,,, 2

    
Strepsidura oregonensis H
washingtonensis HH
striata, Bullia (Molopophorus) ,,,,,,,,,,,,,,,,,,,, 35
Suauodrillia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 39
dickersoni ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 40
hertleini ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 39, 40
winlockensis ,,,,,,,,,,,,, 11, 14, 15, 26, 40, pl. 7
subtenta, Cyclocardia H 45
Surcula dickersoni H H ,,,,,,,,,,,, 40
Systematic descriptions ,,,,,,,,,,,,,,,,,,,,,,,,,, 29
T
Taranis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18, 20, 38
columbiana 11, 14, 15, 26,38, pl, 7
Taras goodspeedi

  
sericata
Tectonatica ,,,,,,,,,,,,,
tectula, Natica ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 31
Tegula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
Tejon Formation ,,,,,,,,,,,,,,,,,,,,,,,,, 5, 23, 31
Calif ,,,,,,,,,,,,,,,,,,, , 31, 33, 35
Tejon Pass, Calif ,,,,,,,, A... 31
Tejon Stage H, ,,,,,,,, 5
Tellina ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 22, 50
aduncanasa ,,,,,,,,,,,,,,,,,,,, H 8, 21, 28, 50
eugenia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
pittsburgensis ,,,,,,,,,,,,,, 5, 14, 15, 16, 21, 26,
28,51, pl. 11
punicea ,,,,,,,,,,,,,,,,,,, 5O
radiata ,,,,,, 50
sp ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 28
(Euljytellina) ,,,,,,,,,,,,,,,,,,, 17, 18
aduncanasa ....... 14, 15, 16, 26,50, pl, 11
(Moerella) lincolnensis ,,,,,,,,,,,,,,,,,,,, 28
Tellinidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,
Tellininae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 50
Temblor Formation H __ 9, 25, 28
Calif ,,,,,,,, H, 33, 34,39, 42, 53
Temblor Range, Calif
Temblorian Stage ,,,,,,,,,,,,,,,,,,,,,,,,, , 9
tenuissima, Yoldia ,,,,,,,,,,,,,,,,,,,,,,
terebra, Turbo
Thesbia columbiana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
thomsonue, Neverita ,,,,,,,,,,,,, 8, 9, 21, 28, 32
Neverita (Glossaulax) 11, 14, 15, 26, 32, pl, 2
Thracia H 17, 18, 20, 22,54
condoni ,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 21, 28, 54
corbuloides ,,,,,,,,,,,,,, .H 54
schencki ,,,,,,,,,,,,,,,,,,,,,,,,,,
trapezoides ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 54
(Thracia) condoni ,,,,,,,, 14, 15, 16, 26, 54, pl. 16

(Thracia) condoni, Thracia __ 14, 15, 16, 26,54, pl, 16
Thraciidae ,,,,,,

 
Thuja sp H

Thyasira ,

Tindaria ,,,,,

Toledo Formation ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 7, 9
Moody Shale Member ,,,,,,,,,,,,,,,,,,,,,,,, 7

tornatilis, Voluta ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 40

townsendensis, Solen ,
Solen (Plectosolen) ,
trapezoides, Thracia ,,,,,,,

14, 15, 16, 26, 51, pl. 13
,,,,,,,,,,,,,,,,,,, 51

  
INDEX
Page
Trochid, unidentiﬁed ,,,,,,,,,,,,,,,,, 15,29, pl. 1
Trochidae ,,,,,,,,,,,,,,,,,, 29
Troohus perspectiuus ,,,,,,,,,,,,,,,,,,,,,,,,,, 29
Trophon marchi H ,H 38
Truncacila ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19, 42
(Truncacila), Acila __________________ 17, 18, 22, 43
nehalemensis, Acila iiiiiiiiiiii 20, 21, 23, 28, 43
minima, Acila ,,,,,,,,,,,,,,,,,,,,,,,,,, 28
shumardi, Acila ,,,,,, 2, 14, 15, 16, 19, 21, 23, 24,
26, 28, 42, pl, 8
tumens, Venus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 47
Tumey Formation ,,,,,,,, 7, 8, 25, 28
Calif 43, 44, 48, 51
Tumey Sandstone ______________ 6
Tunnel Point, Oreg ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3
Tunnel Point beds ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3
Tunnel Point Formation ,,,,,,,,,,,,,,,, 5, 6, 23, 24
Tunnel Point Sandstone ............... 1, 5, 6, 22, 44
mollusks ,,,,,,,,,,,,,,,,,,,,,,,,,,, 22, 25, 28
southwestern Oreg ,,,,,,, 23, 32, 34, 36, 39, 43,
46, 48, 49, 50, 51, 52
Turbo crenata ..... 30
pli/Jatus ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 4O
terebra ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29
Turcicula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20, 21, 22
columbiana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29
turnerae, Opertochasma . H- 28
turneri, Cylichnina , - 22, 28
Turricula kincaidi , H, 39
Turriculinae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 37
Turridae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 37
Turrinae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
Turris kincaidi __________________________________ 39
Turritella ,,,,,,,,,,,,,,,,,, H 14, 16, 17, 18, 22,29
diversilineata blakeleyensis ,,,,,,,,,,,,,,,,,, 30
olympicensis Zone
oregonensis ,,,,,,,,,,,,,,,,,,,,,,,,
pittsburgensis ,,,,,,,,,,,, 11, 15, 16, 26, 29, pl, 3
porterensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29, 30
Zone ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 3, 4, 6, 34
uvasana ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29, 30
variata lorenzana Zone ,,,,,,,,,,,,,,,,,,,,,, 24
Zone ,,,,,,,,,
wheatlandensis H,
Turritellidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 29
Twin River Formation ,,,,,,,,,,,,,,,,,,,,,,,, 7, 10
Wash ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 10, 45
Two Bar Shale Member,
San Lorenzo Formation ,,,,,,,,,,,,,, 8
U
U mpquaia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 34
ungana, Crepidula ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
Ungulinidae ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 46
Ushikubitoga Formation ,,,,,,,,,,,,,,,,,,,,,,,, 8
Japan ,,,,,,,,,,,,,,,,,,,,,,,,, 45, 46
usta, Mysia (Felania) ,,,,,,,,,,,,,,,, _ 46
uvasana, Turritella H 29, 30
U uigerina cocoaensis ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 8
V
vagina, Solen ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 51
Vancouver Island 111111111111111111111111111111 4, 5
vancouverensis, Macoma (Heteromacoma) _ , 28
Vaqueros Sandstone 8
Vaquerosian Stage , 9

 
Veneridae ___________

 
veneriformis, Spisula ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 50
Spisula (Mactromeris)HH 11, 15, 16, 26,50, pl. 14
Venus chione ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 48
gigantea ,,,,, , 48
nimbosa ,,,,, , 48
tumensH,HH H H 47
Vernonia, Oreg ,,,,,,,,,,,,,,,,,,,,,,,,, 19, 25, 51

uemoniensis, Perse

 
Page
uernoniensis—Continued,
pittsburgensis HH 11, 14, 15, 26, 37, pl. 6
Vertebrata ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 20
Vicksburg Group ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 4
Vokes, H, E,, cited ,,,,,,,,,,,,,,,,,,,,,,,,,, 2, 7, 14
uokesi, Bruclarkia ,,,,,,,,,,,,,,,,,,,,,,,,,,, 28
N ucula ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 42
(Leionucula) 111111111 14, 15, 16, 26, 42, pl, 8
Voluta tornatilis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 40
W
Wahkiakum horizon ,,,,,,,,,,,,,,,,,,,,,,,,,, 4
wardi, Aforia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 38
Aforia clallamensis ,,,,,,,,,,,,,,,,,,,,,,, 16, 37
Washington County, Oreg,
stratigraphic section ,,,,,,,,,,,,,,,, 2
washingtonensis, Crenella ,,,,,,,,,,,,,,,,,,,,, 45
Eosiphonalia ,,,,,,,,,,,,,,,,,,,,,,,,, 33, 34
Leda ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 43
Litorhadia ,,,,,,,,,,,,,,,,,, 8, 14, 15, 16, 21, 26,
43, pl. 9
Natica ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 32
Nuculana ,,,,,,,,,,,,,,,,,,,,,, H 9, 20, 28, 43
Polinices ,,,,,,,,,,,,,,,, 8, 11, 14, 15, 21, 26, 28
32, pl. 1
Scaphander
Spirotropis ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 39
Strepsidura ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 33
lincolnensis, Polinices 1111111 , 32
Polinices (Polinices) ,,,,, , 32

washingtoniana, Hemifusus H,
Warren, W, C,, quoted
Weaver, D. W,, cited H
weaveri, Natica ,,,,,,,,
Welton, B, J,, quoted ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17
Wheatland Formation ,,,,,,,,,,,,,,,,,,,,,, 6, 28, 30
Calif ,,,,,,,,,,,,,,,,,,,,,,
wheatlandensis, Turritella _
Whitneyella ,,,,,,,,,,
Willamette Valley, Oreg
willamettensis, Semele ,,,,,,,,,,,,,,,,,,,,,,,, 28
willapaensis, Solemya (Acharax) ,,,,,,,,,,,, ____ 20

 
Wilson’s Bluff, Oreg HH 3
winlockensis, Spirotropis (Spirotropis) ____________ 40
Suauodrillia ,,,,,,,,,,,,,, 11, 14, 15, 26, 40, pl, 7
winlockiana, Odostomia ,,,,,, 11, 15, 16, 26,40, pl. 3
Odostomia (Odostomia) H, ,H 40
Worms, polychaete ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 40
Wygal Sandstone Member ,,,,,,,,,,,,,,,,, 9, 25, 28
Calif ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 33, 42, 53
Y
Yakataga Formation ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 5
Yaquina Formation ,,,,,,,,,,,,,,,,,,,,,,,, 1, 5, 23
Yoldia ,,,,,,,,,, HH 18, 19, 20, 22, 44
arctica ,,,,,,

cooperii

hyperborea ,,,,,,,,,,,,,,,,,,,,,, H, 44

oregona ,,,,,,,,,,,,,,,,,,,,,,,,, _H 44

tenuissima ,,,,,,,,,, H. 44

(Cnestrium) oregano

(Kalayoldia) ,,,,,,,,,,,,,,,,,,,,,,,,,,,, 17, 18
cooperi ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 19
oregona ,,,,,,,,,,,,,,,,,, 14, 15, 16, 26, 28,

44,pl, 9

(Portlandella) chehalisensis ,,,,,,,,
(Portlandia) oregona _ _ _

  
strigata Zone ,,,,,,,,,,,,,,,,,,, 4

Z
Zemorrian Stage ,,,,,,,,,,,,,,,,,,,,,,,, 5, 9, 23, 24
ziczac, Aturia ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 54
Zostera ,,,,,,,,,,,,,,,,,, - 21
sp ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,, 2O

﻿PLATES 1—17

[Contact photographs of the plates in this report are available, at cost, from U.S. Geological Survey Library, Federal

Center, Denver, Colo. 80225.]﻿PLATE 1

Figures 1-4.

5,8.

6,7.

9, 12, 13, 15, 16, 18, 19, 23.

10, 11. 14, 17, 20-22, 24.

Architectonica blanda Dali, p. 29

1-3. Height (incomplete) 10.0 mm, width (incomplete) 14.0 mm. Locality USGS 15588. USNM 213945.

4.	Height (incomplete) 8.5 mm, width (incomplete) 14.0 mm. Locality USGS 15588. USNM 213946. Crepidula pileum (Gabb), p. 31

Height 4.5 mm, width 8mm, length 18 mm. Locality USGS 15310. USNM 213947.

Unidentified trochid?, p. 29

Height (incomplete) 18.3 mm, width (incomplete) 24.8 mm. Locality USGS 15312. USNM 213948. Cryptonatica pittsburgensis, n. sp., p. 31

9.	Height (incomplete) 19.0 mm, width 12.1 mm. Locality USGS 15310. USNM 213949.

12.	Height	(incomplete)	17.8 mm, width (incomplete) 16.9	mm.	Locality USGS 15588. USNM 213950.

13.	Height	(incomplete)	16.0 mm, width (incomplete) 14.0	mm.	Locality USGS 15310h. USNM 213951.

15.	23. Height (incomplete) 18.4 mm, width 18.0 mm. Locality USGS 15310. USNM 213952.

16.	Height (incomplete) 18.4 mm, width (incomplete) 18.6 mm. Locality USGS 15588. USNM 213953.

18.	Height (incomplete) 12.5 mm, width 12.5 mm. Locality USGS 2714. USNM 213954.

19.	Height 11.9 mm, width (incomplete) 11.0 mm. Locality USGS 15310. USNM 213955.

Sinum aff. S. obliquum (Gabb), p. 33

Height (incomplete) 8.7 mm, width (incomplete) 9.2 mm. Locality USGS 15264. USNM 213956. Polinices washingtonensis (Weaver), p. 32

14.	22. Height (incomplete) 24.2 mm, width 23.7 mm. Locality USGS 15310. USNM 213957.

17.	Height(incomplete) 17.4 mm, width (incomplete) 17.9 mm. Locality USGS 15310h. USNM 213958.

20.	Height	(incomplete)	23.8 mm, width (incomplete) 23.4	mm.	Locality USGS 15310h. USNM 213959.

21.	Height	(incomplete)	29.8 mm, width (incomplete) 27.6	mm.	Locality USGS 15588. USNM 213960.

24. Height (incomplete) 21.0 mm, width 19.7 mm. Locality USGS 15310h. USNM 213961.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 1

Xl ’/>

ARCHITECTONICA, CREPIDULA, UNIDENTIFED TROCHID?, CRYPTONATICA .SINUM, AND POLINICES﻿PLATE 2

Figures 1-15. Neverita (Glossaulax) thomsonae Hickman, p. 32

I.	Height (incomplete) 34.0 mm, width (incomplete) 36.5 mm. Locality USGS 15264. USNM 213962.

2,5. Height (incomplete) 36.0 mm, width (incomplete) 41.2 mm. Locality USGS 5394. USNM 213963.

3.	Height (incomplete) 39.6 mm, width (incomplete) 37.7 mm. Locality USGS 15264. USNM 213964.

4.	Height (incomplete) 43.3 mm, width (incomplete) 45.2 mm. Locality USGS 15264. USNM 213965.

6.	Height (incomplete) 21.5 mm, width (incomplete) 21.7 mm. Locality USGS M3878. USNM 213966.

7.	Height (incomplete) 24.7 mm, width (incomplete) 29.0 mm. Locality USGS M3857. USNM 213967.

8.	12. Height 19.8 mm, width (incomplete) 23.3 mm. Locality USGS 15310. USNM 213968.

9.	Height 15.3 mm, width (incomplete) 10.4 mm. Locality USGS 15310. USNM 213969.

10. Height 44.7 mm, width 49.6 mm. Locality USGS 15264. USNM 213970.

II. Height 18.3 mm, width 19.6 mm. Locality USGS 15310. USNM 213971.

13.	Height 23.1 mm, width (incomplete) 27.3 mm. Locality USGS 15310. USNM

213972.

14.	Height 52.5 mm, width (incomplete) 46.5 mm. Locality USGS 15310. USNM

213973.

15.	Height (incomplete) 36.0 mm, width (incomplete) 36.6 mm. Locality USGS M3871. USNM 213974.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 2

xiy,

NEVE RITA﻿PLATE 3

Figures 1-5, 21-23.

6, 8, 20.

7, 9, 10.

11-16.

17-19.

Bruclarkia Columbiana (Anderson and Martin), p. 34

1.	Height (incomplete) 59.5 mm, width (incomplete) 48.3 mm. Locality USGS 15264. USNM 213975.

2.	Height 12.6 mm, width (incomplete) 8.0 mm. Locality USGS 15310. USNM 213976.

3.	4. Height (incomplete) 5.6 mm, width (incomplete) 3.5 mm. Locality USGS 15310. USNM

213977.	Note protoconch on figure 3.

5.	Height (incomplete) 44.7 mm, width (incomplete) 30.5 mm. Locality USGS 15264. USNM

213978.

21,	23. Height (incomplete) 68.5 mm, width (incomplete) 52.7 mm. Locality USGS 15588. USNM 213979.

22.	Height (incomplete) 59.5 mm, width (incomplete) 14.5 mm. Locality USGS 15310. USNM 213980.

Opalia (Dentiscala?) hertleini, n. sp., p. 30

6.	Height (incomplete) 6.6 mm, width 3.8 mm. Locality USGS 21612. USNM 213981.

8.	Height (incomplete) 13.2 mm, width (incomplete) 8.1 mm. Locality USGS 15588. USNM 213982.

20. Holotype. Height (incomplete) 29.7 mm, width (incomplete) 12.0 mm. Locality USGS 15588. USNM 213983.

Odostomia winlockiana Effinger, p. 40

7.	Height (incomplete) 4.5 mm, width 2.2 mm. Locality USGS 5329, Gries Ranch Formation. On the Nehalem road about 14,871 feet south of Clatskanie, sec. 24, T. 7 N., R. 5 W., Oregon. USNM 213984.

9,	10. Height 2.5 mm, width 1.0 mm. Locality USGS 15310. USNM 213985.

Turritella pittsburgensis, n. sp., p. 29

11.	Height (incomplete) 21 mm, width 6 mm. Locality USGS 15278. USNM 213986.

12. Height (incomplete) 30 mm, width 11 mm. Locality USGS 15519. USNM 213987.

13. Height (incomplete) 33 mm, width 12 mm. Locality USGS 15519. USNM 213988.

14.	Height (incomplete) 21 mm, width 8 mm. Locality USGS 15278. USNM 213989.

15.	Height (incomplete) 30 mm, width 11 mm. Locality USGS 15519. USNM 213990.

16.	Holotype. Height (incomplete) 28.6 mm, width (incomplete) 10.7 mm. Locality USGS 15588. USNM 213991.

Priscofusus stewarti (Tegland), p. 36

17.	19. Height (incomplete) 29.6 mm, width 12.7 mm. Locality USGS 15264. USNM 213992.

18.	Height (incomplete) 16.7 mm, width (incomplete) 10.6 mm. Locality USGS M3871. USNM 213993.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 3

vs

%

BRUCLARKIA, OP ALIA, ODOSTOMIA, TURRITELLA, AND PRISCOFUSUS﻿PLATE 4

Figures 1-9. Eosiphonalia oregonensis (Dali) p. 33

1,	3. Height 39.2 mm, width 27.5 mm. Locality USGS 15310. USNM 213994.

2.	Height 30.4 mm, width 23.2 mm. Locality USGS 15264. USNM 213995.

4,	6. Holotype. Height 30 mm, width 21 mm. Locality UW 500. In fine-grained brownish-gray sandstone in road cut near Pittsburg, Columbia County, Oreg. USNM 107395.

5, 8. Height 32.8 mm, width 24.5 mm. Locality USGS 15264. USNM 213996. 7, 9. Height 31.2 mm, width 23.7 mm. Locality USGS 15310. USNM 213997.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 4

1

EOSIPHONALIA﻿PLATE 5

Figures 1-22. Molopophorus gabbi Dali, p. 35

I,	2. Height (incomplete) 10.8 mm, width (incomplete) 7.5 mm. Locality USGS 15310f. USNM 213998

3.	6. Height (incomplete) 16.8 mm, width (incomplete) 12.6 mm. Locality USGS 15264. USNM 213999.

4.	Protoconch. Locality USGS M3871. USNM 214000.

5.	Height (incomplete) 16.7 mm, width (incomplete) 13.7 mm. Locality USGS 15310. USNM 214001.

7.	Protoconch. Locality USGS M3857. USNM 214002.

8.	Height (incomplete) 25.4 mm, width (incomplete) 17.7 mm. Locality USGS 15310. USNM 214003.

9.	Height (incomplete) 17.3 mm, width (incomplete) 20.0 mm. Locality USGS 15310. USNM 214004.

10.	Height 27.8 mm, width 20.9 mm. Locality USGS 15310a. USNM 214005.

II.	Height	27.0 mm, width 21.3	mm.	Locality USGS	15310. USNM	214006.

12.	Height	24.7 mm, width 20.0	mm.	Locality USGS	15310. USNM	214007.

13.	Height (incomplete) 26.2 mm, width (incomplete) 20.7 mm. Locality USGS 15310. USNM 214008.

14.	Height (incomplete) 24.2 mm, width (incomplete) 19.2 mm. Locality USGS 15310. USNM 214009.

15.	Height (incomplete) 19.8 mm, width (incomplete) 16.6 mm, Locality USGS 15264. USNM 21410.

16.	Height	27.0 mm, width 20.1	mm.	Locality USGS	15310. USNM	214011.

17.	Height	26.6 mm, width 21.0	mm.	Locality USGS	15310. USNM	214012.

18.	Height 24.7 mm, width (incomplete) 21.5 mm. Locality USGS 15310. USNM 214013.

19.	22. Holotype. Height 19 mm, width 12 mm. Locality USGS 2714. USNM 107377.

20.	Height (incomplete) 23.7 mm, width (incomplete) 17.0 mm. Locality USGS 2415. USNM 214014.

21.	Paratype. Height (incomplete) 16 mm, width 11.5 mm. Locality USGS 2714. USNM 214016.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 5

X1 ’/,

x1 ’/,


MOLOPOPHORUS﻿PLATE 6

Figures 1, 4, 6, 7, 9, Perse pittsburgensis Durham, p. 36

12-14, 18-20.	1, 4. Height 32.3 mm, width (incomplete) 15.8 mm. Locality USGS 15264. USNM 214017.

6.	Height (incomplete) 21.0 mm, width (incomplete) 11.5 mm. Locality USGS 15310. USNM

214018.

7.	Height (incomplete) 12.0 mm, width (incomplete) 10.0 mm. Locality USGS 15264. USNM

214019.

9.	Height (incomplete) 6.7 mm, width (incomplete) 4.6 mm. Locality USGS 15588. USNM

214020.

12.	Height (incomplete) 16.7 mm, width (incomplete) 12.2 mm. Locality USGS 15588. USNM

214021.

13.	Height (incomplete) 17.6 mm, width (incomplete) 13.3 mm. Locality USGS 15588. USNM

214022.

14.	Height (incomplete) 15.4 mm, width (incomplete) 11.5 mm. Locality USGS 15588. USNM

214023.

18.	Protoconch. Locality USGS 15264b. USNM 214024.

19.	Height (incomplete) 11.8 mm, width (incomplete) 9.8 mm. Locality USGS 15588. USNM

214025.

20.	Height (incomplete) 13.5 mm, width (incomplete) 8.9 mm. Locality USGS 15588. USNM

214026.

2, 3, 5, 8, 10, 11, 15-17.

Perse pittsburgensis vernoniensis, n. subsp., p. 37

2,	3. Height (incomplete) 23.8 mm, width (incomplete) 14.6 mm. Locality USGS 15588. USNM

214027.

5,	8. Height (incomplete) 30.4 mm, width (incomplete) 15.1 mm. Locality USGS 15588. Holotype USNM 214028.

10.	Height (incomplete) 23.4 mm, width (incomplete) 13.0 mm. Locality USGS 15588. USNM

214029.

11.	Height (incomplete) 27.6 mm, width (incomplete) 19.4 mm. Locality USGS 15588. USNM

214030.

15.	Height (incomplete) 24.3 mm, width (incomplete) 16.7 mm. Locality USGS 15588. USNM

214031.

16.	Height (incomplete) 28.0 mm, width (incomplete) 15.2 mm, Locality USGS 15588. USNM

214032.

17.	Height (incomplete) 23.0 mm, width (incomplete) 11.6 mm. Locality USGS 15588. USNM

214033.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 6

PERSE

\ *﻿PLATE 7

Figures 1,9,10,13.

2, 3, 5-8, 16, 37.

4, 11, 12, 15, 33-36, 38.

14, 17. 18, 23-32.

19.

20, 21.

22.

Spirotropis kincaidi (Weaver), p. 39

1.	Protoconch. Height (incomplete) 10.4 mm, width (incomplete) 6.4 mm. Locality USGS M3871. USNM 214034.

9.	Height (incomplete) 17.2 mm, width (incomplete) 7.8 mm. Locality USGS 15588. USNM 214035.

10.	Height 15.1 mm, width (incomplete) 7.3 mm. Locality USGS 15310a. USNM 225304.

13.	Height (incomplete) 6.3 mm, width (incomplete) 5.0 mm. Locality USGS 15264. USNM 214036.

Taranis Columbiana (Anderson and Martin) p. 38

2.	Height (incomplete) 10.7 mm, width (incomplete) 5.0 mm. Locality USGS 15264a. USNM 214037.

3.	Height (incomplete) 7.7 mm, width (incomplete) 4.7 mm. Locality USGS 15264. USNM 214038.

5.	Height (incomplete) 10.8 mm, width 4.9 mm. Locality USGS M3871. USNM 214039.

6.	Smooth-keeled form. Height (incomplete) 10.9 mm, width (incomplete) 6.1 mm. Locality USGS M3871. USNM 214040.

7.	Height (incomplete) 8.1 mm, width (incomplete) 4.3 mm. Locality USGS 15310. USNM 214041.

8.	Protoconch. Height 10.0 mm, width (incomplete) 4.8 mm. Locality USGS M3871. USNM 214042.

16.	Smooth-keeled form. Height (incomplete) 9.6 mm, width (incomplete) 5.0 mm. Locality USGS 15264b. USNM

214043.

37.	Intermediate form. Height (incomplete) 11.4 mm, width (incomplete) 5.7 mm. Locality USGS 15310. USNM

214044.

Suavodrillia winlockensis (Effinger), p. 40

4.	Protoconch. Height (incomplete) 8.0 mm, width (incomplete) 4.0 mm. Locality USGS 15310a. USNM 214045.

11.	Height (incomplete) 3.5 mm, width (incomplete) 1.8 mm. Locality USGS 15310. USNM 214046.

12.	Height (incomplete) 10.2 mm, width (incomplete) 4.4 mm. Locality USGS 15310. USNM 214047.

15. Height (incomplete) 4.9 mm, width 2.4 mm. Locality USGS 15310. USNM 214048.

33. Height (incomplete) 6.0 mm, width 3.3 mm. Locality USGS 15264b. USNM 214049.

34.	Height (incomplete) 5.1 mm, width (incomplete) 2.2 mm. Locality USGS 15310. USNM 214050.

35.	36. Height 10.6 mm, width 4.5 mm. Locality USGS 15310a. USNM 214051.

38.	Height (incomplete) 6.9 mm, width 3.2 mm. Locality USGS 15310. USNM 214052.

Dentalium (Fissidentalium?) laneensis Hickman, p. 41

14.	Length (incomplete) 19.0, diameter: greatest 5.2 mm, least 3.3 mm. Locality USGS 2723. USNM 214053.

17.	Length (incomplete) 30.6 mm, diameter: greatest 10.0 mm, least 5.3 mm. Locality USGS 15264. USNM 214054. Scaphander stewarti Durham, p. 41

18.	29. Height (incomplete) 10.9 mm, width (incomplete) 6.0 mm. Locality USGS 15264. USNM 214055.

23,	Height (incomplete) 9.8 mm, width (incomplete) 5.0 mm. Locality USGS 15264b. USNM 214056.

24,	27. Height (incomplete) 8.8 mm, width 4.9 mm. Locality USGS 18638. USNM 214057.

25,	26. Height (incomplete) 13.8 mm, width (distorted) 8.3 mm. Locality USGS 15310. USNM 214058.

28. Height (incomplete) 10.7 mm, width (incomplete) 6.1 mm. Locality USGS 15264b. USNM 214059.

30, 31. Height 12.1 mm, width 7.6 mm. Locality USGS 15588. USNM 214060.

32. Height (incomplete) 9.4 mm, width 9.0 mm. Locality USGS 2714. USNM 214061.

Acteon? n. sp.?, p. 41

Height (incomplete) 4.1 mm, width (incomplete) 3.0 mm. Locality USGS 15588. USNM 214062.

Acteon chehalisensis (Weaver), p. 40

20.	Height (incomplete) 8.2 mm, width (incomplete) 4.4 mm. Locality USGS 15264. USNM 214063.

21.	Height (incomplete) 10.0 mm, width (incomplete) 5.4 mm. Locality USGS 15588. USNM 214064.

Aforia campbelli Durham, p. 37

Height (incomplete) 28.0 mm, width (incomplete) 21.0 mm. Locality USGS 15519. USNM 214065.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 7

SPIROTROPIS, TARANIS, SUAVODRILLIA, DENTALIUM, SCAPHANDER, ACT EON1., ACTEON, AND AFORIA﻿PLATE 8

Figures 1-9, 11, 12, 14, 15, 18.

10, 13, 16, 17.

Acila (Truncacila) shumardi (Dali), p. 42

I.	Length 18.0 mm, width (both valves) 9.7 mm, height 13.4 mm. Locality USGS 15264. USNM 214066.

2,3, 7. Length 24.4 mm, width 14.5 mm, height 18.7 mm, Locality USGS 2714. USNM 107402.

2.	End view of escutcheon.

3.	Left valve.

7. Top view of lunule.

4.	Length 28.0 mm, width 7.7 mm, height 20.2 mm. Locality USGS 15310. USNM 214067.

5,	6. Holotype. Length 24.2 mm, height 17.8 mm. Locality USGS 2714. USNM 406405.

8.	Length 26.2 mm, width (one valve) 7.5 mm, height 19.9 mm. Locality USGS 15588. USNM

214068.

9.	Length 14.1 mm, width (one valve) 4.5 mm, height 10.3 mm. Locality USGS 15264. USNM

214069.

II.	Length 25.1 mm, width (one valve) 7.3 mm, height 19.3 mm. Locality USGS 15264. USNM

214070.

12.	Hinge. Length 23.0 mm, height 16.8 mm. Locality USGS M3871. USNM 214071.

14.	Hinge. Length (incomplete) 22.9 mm, height (incomplete) 18.0 mm. Locality USGS M3871. USNM 214072.

15. Hinge. Length 26.6 mm, height 19.9 mm. Locality USGS M3871. USNM 214073.

18.	Hinge. Length 23.3 mm, height 16.9 mm. Locality USGS M3871. USNM 214074.

Nucula (Leionucula) vokesi, n. sp., p. 42

10.	Holotype. Length 6.5 mm, height 4.7 mm. Locality USGS 18638. USNM 214075.

13.	Length 7.5 mm, width 3.2 mm, height 5.7 mm. Locality USGS 2714. USNM 214076.

16.	Hinge, left valve. Locality USGS 18638. USNM 214077.

17.	Hinge, right valve. Locality USGS 18638. USNM 214078.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 8

1/2

1/2

x11/a

ACILA AND NUCULA﻿PLATE 9

Figures 1-10, 12.

11, 13, 15.

14, 16-18.

Litorhadia washingtonensis (Weaver) p. 43

1.	Length (incomplete) 22.7 mm, height (incomplete) 12.3 mm, width 3.0 mm. Locality USGS 15310. USNM 214079.

2.	8. Length (incomplete) 17.1 mm, height (incomplete) 8.1 mm. Locality USGS 19004, Lincoln Creek Formation, Washington. USNM 214080.

3.	Length (incomplete) 23 mm, height (incomplete) 12 mm. Locality USGS 15310. USNM 214081.

4.	Length (incomplete) 17.6 mm, height (incomplete) 10.5 mm. Locality USGS 18638. USNM 214082.

5.	Length (incomplete) 20.4 mm, height 10.2 mm. Locality USGS 15310. USNM 214083.

6.	Length (incomplete) 19.5 mm, height (incomplete) 9.3 mm. Locality USGS 18638. USNM

214084.

7.	Length (incomplete) 16.2 mm, height (incomplete) 7.5 mm. Locality USGS 15310. USNM

214085.

9.	Length (incomplete) 11.0 mm, height (incomplete) 5.2 mm. Locality USGS 15588. USNM

214086.

10.	Length 20.0 mm, height 9.3 mm. Locality USGS 15264. USNM 214087.

12.	Length 29.2 mm, height 13.7 mm. Locality USGS 15588. USNM 214088.

Cyclocardia (Cyclocardia) cf. C. (C.) hannibali (Clark), p. 45

11.	Length (incomplete) 17.6 mm, height (incomplete) 17.8 mm. Locality USGS 15537. USNM

214089.

13.	Length (incomplete) 15.5 mm, height (incomplete) 12.0 mm. Locality USGS 15537. USNM

214090.

15.	Right valve and hinge of left valve. Length (incomplete) 14.0 mm, height (incomplete) 13.0 mm. Locality USGS 15537. USNM 214091.

Yoldia (Kalayoldia) oregona (Shumard), p. 44

14.	Length (incomplete) 43 mm, height 28.0 mm. Locality USGS 15586. USNM 214092.

16.	Hinge. Locality USGS 15310a. USNM 214093.

17.	Length (incomplete) 41.4 mm, height 23.0 mm. Locality USGS 15586. USNM 214094.

18.	Length (incomplete) 51 mm, height (incomplete) 23 mm. Locality USGS 15264e. USNM 214095.﻿GEOLOGICAL SURVEY

LITORHADIA, CYCLOCARDIA, AND YOLDIA﻿PLATE 10

Figures 1-8. Lucinoma Columbiana (Clark and Arnold), p. 45

1.	Length (incomplete) 18.7 mm, height 15.5 mm. Locality USGS 15588. USNM 214096.

2,	3, 6-8. Length (incomplete) 21.2 mm, height 20.0 mm, width (both valves) 11.6 mm. Locality USGS 15588. USNM 214097.

4,	5. Length 11.0 mm, height 10.3 mm, width (one valve) 2.3 mm, Locality USGS 15588. USNM 214098.

9-11. Felaniella (Felaniella) snavelyi, n. sp., p. 46

9.	Length 14.6 mm, height 13.0 mm. Locality USGS 15586. USNM 214099.

10.	Holotype. Length 21.6 mm, height 19.6 mm, width (one valve) 4.2 mm. Locality USGS 15264. USNM 214100.

11.	Length (incomplete) 15.0 mm, height 22.0 mm. Locality USGS 15310. USNM 214101.

12-14. Nemocardium (Keenaea) lorenzanum (Arnold), p. 47

12.	Length (incomplete) 11 mm, height (incomplete) 10.0 mm. Locality USGS 18638. USNM 214102.

13.	Length 12.3 mm, height 11.0 mm. Locality USGS 15264. USNM 214103.

14.	Height 4.5 mm, length 4.6 mm. Locality USGS 18638. USNM 214104.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 10

x21/2

x1 ’/2

8

LUCINOMA, FELANIELLA, AND NEMOCARDIUM﻿PLATE 11

Figures 1-6. Tellina! pittsburgensis Clark, p. 51

1.	Hinge. Locality USGS 15264. USNM 214105.

2.	Hinge. Locality USGS 15264. USNM 214106.

3.	Length (incomplete) 13.7 mm, height (incomplete) 8.4 mm. Locality USGS 15586. USNM 214107.

4.	Length (incomplete) 15.6 mm, height (incomplete) 9.6 mm. Locality USGS 15586. USNM 214108.

5.	Dorsal view. Length (incomplete) 22 mm, height 13.4 mm, width (both valves) 5.4 mm. Locality USGS 15264. USNM 214109.

6.	Height 13.3 mm, length (incomplete) 21.6 mm. Locality USGS 15264. USNM 214110.

7-12. Tellina (Eurytellina) aduncanasa Hickman, p. 50

7.	Length (incomplete) 36 mm, height (incomplete) 20 mm. Locality USGS 15588. USNM 214111.

8,11,12. Length (incomplete) 18.6 mm, height (incomplete) 9.7 mm, width (both valves) 2.8 mm. Locality USGS 15264. USNM 214112.

9.	Length (incomplete) 39 mm, height (incomplete) 19 mm. Locality USGS 15310b. USNM 214113.

10.	Length (incomplete) 27 mm, height (incomplete) 14 mm. Locality USGS 15586. USNM 214114.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 11

TELLINA? AND TELLINA﻿PLATE 12

Figures 1, 2, 4. Pitar (Pitar) dalli (Weaver), p. 47

1.	4. Length (incomplete) 65 mm, height (incomplete) 46 mm, width (both valves, internal mold) 28.5 mm. Locality USGS 15532. USNM 214115.

2.	Left hinge. Locality USGS 15310a. USNM 214116.

3,	5-11, 13. Callista (Macrocallista) pittsburgensis Dali, p. 48

3.	Left hinge. Length 13.0 mm, height 8.6 mm. Locality USGS 15264. USNM 214177.

5.	Left hinge. Length 19.3 mm, height 13.0 mm. Locality USGS 15264. USNM 214118.

6.	Length (incomplete) 42 mm, height 24.3 mm. Locality USGS 15264. USNM 214119.

7.	9. Length 34.0 mm, height 21.4 mm, width (one valve) 6.1 mm. Locality USGS 15264. USNM 214120.

8.	Length (incomplete) 22.0 mm, height 16.5 mm. Locality USGS 15264. USNM 214121.

10.	Right hinge. Length (incomplete) 7.1 mm, height (incomplete) 4.9 mm. Locality USGS 18638. USNM 214122.

11.	Paratype. Length (incomplete) 31 mm, height (incomplete) 22 mm. Locality USGS 2714. USNM 107399.

13. Lectotype. Length (incomplete) 36 mm, height (incomplete) 21 mm. Locality USGS 2714. USNM 107396.

12.	Crenella porterensis Weaver, p. 45

Length (incomplete) 5.0 mm, height (incomplete) 5.4 mm. Locality USGS 15583. USNM 214123.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 12

PITAR, CALLISTA, AND CRENELLA﻿PLATE 13

Figures 1, 2, 6. Solena (Eosolen) eugenensis (Clark), p. 52

1.	Hinge of left valve. Length (incomplete) 87 mm, height (incomplete) 21 mm. Locality USGS 15588. USNM 214124.

2.	Length (incomplete) 70 mm, height (incomplete) 26 mm, width (both valves, compressed) 12.7 mm. Locality USGS 15588. USNM 214125.

6.	Interior of left valve. Locality USGS 15588. USNM 214126.

3-5. Solen townsendensis Clark, p. 51

3.	5. Length (incomplete) 54 mm, height (incomplete 14 mm, width (one valve) 3.5 mm. Locality USGS 15310. USNM 214127.

4.	Length (incomplete) 21 mm, height 5.6 mm. Locality USGS 15264. USNM 214128.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 13

SOLENA AND SOLEN﻿PLATE 14

Figures 1, 2, 9. Spisula (Mactromeris?) veneriformis Clark, p. 50

1.	Rubber impression of left hinge. Locality USGS 15516. USNM 214129.

2.	Rubber impression of right hinge. Locality USGS 15516. USNM 214130.

9.	Length (incomplete) 83.2 mm, height (incomplete) 70.9 mm. Locality

USGS 15516. USNM 214131.

3-8, 10, 11. Spisula (Mactromeris) pittsburgensis Clark, p. 49

3.	Right hinge. Length (incomplete) 48 mm, height (incomplete) 34 mm, width (one valve) 9.7 mm. Locality USGS 15310d. USNM 214132.

4.	Right hinge. Length (incomplete) 49 mm, height (incomplete) 36 mm. Locality USGS 15586. USNM 214133.

5.	Left hinge. Length 32.1 mm, height 22.7 mm. Locality USGS 15264. USNM 214134.

6.	10, 11. Length (incomplete) 56.2 mm, height 39.6 mm, width (both valves) 21.0 mm. Locality USGS 15588. USNM 214135.

7.	Right hinge. Locality USGS 18638. USNM 214136.

8.	Left hinge. Locality USGS 15310b. USNM 214137.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 14

SPI SUL A﻿Figures

PLATE 15

-3. Panopea ramonensis Clark, p. 53

1.	Length 48.9 mm, height 28.5 mm. Locality USGS 15588. USNM 214138.

2.	Length (incomplete) 42.0 mm, height (incomplete) 27.0 mm, width (both valves) 18.9 mm. Locality USGS 15499. USNM

214139.

3.	Length (incomplete) 45 mm, height (incomplete) 34 mm, width (both valves) 22.6 mm. Locality USGS 15588. USNM

214140.

4.	Aturia angustata (Conrad), p. 54

Height (incomplete) 30 mm, width (incomplete) 30 mm. Locality; roadcut on Scappoose-Vernonia road, about 2 mi from the junction with State Highway 47. USNM 214142.

5.	Panopea snohomishensis Clark, p. 52

Length 83.4 mm, height (incomplete) 52.3 mm. Locality USGS 15516. USNM 214141.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 15

PAN OPE A AND A TURIA﻿PLATE 16

Figures 1, 3. Thracia (Thracia) condoni Dali, p. 54

Length (incomplete) 46.7 mm, height (incomplete) 34.7 mm. Locality USGS 15586. USNM 214143.

2,	5. ?Ervilia oregonensis Dali, p. 50

Length (incomplete) 10.5 mm, height (incomplete) 7.0 mm. Locality USGS 18638. USNM 214144.

4,	6-11. Cochlodesma bainbridgensis Clark, p. 53

4,	8. Length (incomplete) 34.1 mm, height (incomplete) 21 mm, width (both valves) 8.2 mm. Locality USGS M3872. USNM 214146.

6.	Length (incomplete) 40.0 mm, height (incomplete) 29 mm. Locality USGS 15519. USNM 214145.

7.	Length (incomplete) 32.5 mm, height (incomplete) 23.5 mm. Locality USGS 15588. USNM 225305.

9.	Condrophore with mineralized resilium. Length (incomplete) 42 mm, height (incomplete) 30 mm. Locality USGS 15588. USNM 214147.

10.	Length (incomplete) 53 mm, height (incomplete) 35 mm. Locality USGS 15583. USNM 214148.

11.	Length (incomplete) 32 mm, height (incomplete) 23 mm. Locality USGS 15588. USNM 214149.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 16

THRACIA, TER VILIA, AND COCHLODESMA﻿PLATE 17

Two fossiliferous slabs from USGS locality 15310 in the Pittsburg Bluff Formation showing typical groupings of naticids, Molopophorus, Perse, Acila, and Macrocallista. Natural size.﻿GEOLOGICAL SURVEY

PROFESSIONAL PAPER 922 PLATE 17

NATICIDS; MOLOPOPHORUS, PERSE, ACILA, AND MACROCALLISTA﻿﻿﻿﻿7 DAYS

Stratigraphy of the North Half of the Western Sierra Nevada Metamorphic Belt, California

GEOLOGICAL SURVEY PROFESSIONAL PAPER 923

Prepared in cooperation with the California Division of Mines and Geology﻿﻿Stratigraphy of the North Half of the Western Sierra Nevada Metamorphic Belt, California

By LORIN D. CLARK

GEOLOGICAL SURVEY PROFESSIONAL PAPER 923

Prepared in cooperation with the California Division of Mines and Geology

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1976﻿UNITED STATES DEPARTMENT OF THE INTERIOR

THOMAS S. KLEPPE, Secretary

GEOLOGICAL SURVEY V. E. McKelvey, Director

Library of Congress Cataloging in Publication Data Clark, Lorin D.

Stratigraphy of the north half of the western Sierra Nevada metamorphic belt, California.

(Geological Survey Professional Paper 923)

Bibliography: p. 25-26.

Supt.ofDocs.no.: 119.16:923

1.	Geology, Stratigraphic-Paleozoic. 2. Geology, Stratigraphic-Mesozoic. 3. Rocks, Metamorphic. 4. Geology-Sierra Nevada Mountains. I. California. Division of Mines and Geology. II. Title. III. Series: United States. Geological Survey Professional Paper 923.

QE654.C54	557.94'4	76-608016

For sale by the Superintendent of Documents, U.S. Government Printing Office

Washington, D.C. 20402

Stock Number 024-001-02785-2﻿CONTENTS

Page

Abstract____________________________________________________ 1

Introduction________________________________________________ 1

Previous work___________________:____________________ 3

Fieldwork and scope of this investigation ______________ 3

Acknowledgments ________________________________________  4

Terminology_____________________________________________ 4

Summary of geology__________________________________________ 5

Paleozoic rocks_____________________________________________ 8

Shoo Fly Formation _____________________________________ 8

Lithology _________:_____________________________ 9

Stratigraphic relations_____________________________ 10

Age_________________________________________________ 11

Calaveras Formation_____________________________________ 11

Fossils and age ____________________________________ 12

Relief Quartzite ___________________________________ 12

Cape Horn Slate_____________________________________ 13

Delhi Formation_____________________________________ 13

Clipper Gap Formation_______________________________ 13

Tightner Formation _________________________________ 14

Kanaka Formation____________________________________ 14

Page

Paleozoic rocks—Continued

Volcanic rocks_________________________________________ 15

Paleozoic and (or) Mesozoic rocks __________________________ 15

Volcanic and sedimentary rocks_________________________ 15

Epiclastic rocks _____________________________________ 16

Metavolcanic rocks_____________________________________ 16

Mesozoic rocks______________________________________________ 16

Triassic(?) rocks______________________________________ 17

Jurassic rocks_________________________________________ 18

Sailor Canyon Formation____________________________ 18

Milton Formation __________________________________ 19

Amador Group of Taliaferro (1942, 1943) ___________ 20

Cosumnes-type rocks____________________________ 21

Logtown Ridge Formation _______________________ 22

Monte de Oro Formation_____________________________ 22

Unnamed epiclastic rocks___________________________ 23

Unnamed volcanic rocks ____________________________ 24

References cited____________________________________________ 25

ILLUSTRATIONS

Page

Plate 1. Geologic map of the northwestern Sierra Nevada__________________________________________________________________ In pocket

Figure 1. Generalized geologic map of the western Sierra Nevada metamorphic belt ---------------------------------------------- 2

2.	Index of topographic quadrangle maps within and bordering the north half of the western Sierra Nevada metamorphic belt __	4

3.	Sketch of fault-bounded structural blocks of the north half of the western Sierra Nevada metamorphic belt__________ 7

III﻿


﻿STRATIGRAPHY OF THE NORTH HALF OF THE WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

By Lorin D. Clark

ABSTRACT

A belt of metamorphic rocks, about 180 miles (290 km) long and 20-40 miles (32-64 km) wide, crops out in the western foothills of the Sierra Nevada from the latitude of Yosemite Valley northward. It lies between the Sierra Nevada batholith on the east and overlapping unmetamorphosed Tertiary strata on the west. The metamorphic rocks were derived from sparsely fossiliferous eugeosynclinal volcanic and epiclastic rocks of Paleozoic and Mesozoic age. Regional metamorphism is generally of low grade, in the greenschist facies.

Lithologic similarities between Paleozoic and Mesozoic rocks preclude correlation by lithology alone. The paleontologic record is incomplete, and some map units are undated. The Shoo Fly Formation is questionably correlated with the lithologically similar Taylorsville Formation of Silurian age exposed north of the report area. An unnamed unit of volcanic and sedimentary rocks has yielded fossils of probable Devonian age; the Calaveras Formation has yielded gastropods and corals of late Paleozoic age; an unnamed limestone contains fossils of Late Triassic(?) age; the Sailor Canyon Formation contains ammonites of Early and Middle Jurassic age; Cosumnes-type rocks have yielded ammonites of early Late Jurassic age; and the Monte de Oro Formation bears a Late Jurassic fauna.

As a result of successive deformations, the structure of the metamorphic belt is complex and incompletely understood. The structure can be generalized in terms of four blocks separated by three steeply eastward-dipping reverse faults along which younger strata have been thrust beneath older. These include, from west to east, (1) a block of predominantly Jurassic and probable Jurassic rocks, (2) a block of predominantly Jurassic rocks, (3) a disconnected block of upper Paleozoic and Mesozoic rocks, including the Calaveras Formation, and (4) a block of Paleozoic and Mesozoic rocks including the Shoo Fly Formation. Mesozoic rocks lie on both sides of the metamorphic belt, and the eastward-facing bedding tops predominating over westward-facing ones suggest the central position of the Paleozoic strata results chiefly from faulting.

Major fault zones are marked by zones of flaser rock or schist or both, which vary in width from about 100 feet (30 m) to nearly 3 miles (4.8 km) if large horses are included. Most major faults strike north or N. 30° W. Planar structures in the fault zones dip eastward more steeply than 70°. Lineations consisting of elongate rock fragments, amphibole crystals, and axes of minor folds of slip surfaces plunge steeply.

In general, Paleozoic rocks are more deformed than Mesozoic rocks in the report area, but exceptions are readily found. The present structure results from several stages of regional deformation. The greater deformation of the older rocks results partly from greater lithologic susceptibility or geographic position or both, but Silurian rocks were deformed at least twice before deposition of Triassic (?) and Jurassic strata. Jurassic rocks were folded about moderately plunging axes, and older rocks were refolded, before major faulting was completed.

INTRODUCTION

This report is based on fieldwork by L'orin D. Clark during the period 1955-61 and is an extension of his earlier work in the southern half of the western Sierra Nevada metamorphic belt. He prepared the bulk of the report in the mid-1960’s, but various factors, including illness, delayed its completion. This illness also prevented the preparation of a proposed major chapter on the structure of the metamorphic belt, and so this report is limited largely to stratigraphic considerations. The basic data that led to the interpretations herein are being released separately as a series of geologic maps and cross sections at a scale of 1:62,500, with lithologic annotations, along the American, Bear, and Yuba Rivers, and Camp Creek, a tributary to the Cosumnes River (Clark and Huber, 1975).

N. King Huber, who spent the summer of 1955 in the field with Clark, assembled the final manuscrupt. Many of the internal inconsistencies inherent in most draft manuscripts and maps have been reconciled, but some remain, particularly with respect to the regional map in this report and the larger scale separate maps.

In the western Sierra Nevada, metamorphic rocks are exposed in a 20-40-mile-wide (32-64 km) belt that extends about 180 miles (290 km) from about the latitude of Yosemite Valley northwestward to the north end of the Sierra Nevada (fig. 1). On the south and east they are bounded by granitoid rocks of the Sierra Nevada batholith, and on the north and west they pass beneath unmetamorphosed volcanic and sedimentary rocks of Tertiary age. The pre-Tertiary surface can be traced westward by means of drill-hole and seismic evidence to about the center of the Great Valley of California. Sparse samples suggest that basement rocks under the valley fill are similar to those exposed in the metamorphic belt.

The southern part of the metamorphic belt was described in an earlier j eport (Clark, 1964), and the northern part is describee herein. Throughout the belt the metamorphic rocks were derived from eugeosynclinal Paleozoic and Meso2oic volcanic and epiclastic rocks.

1﻿2

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

122° 121° 120“

Figure 1.—Generalized geologic map of the western Sierra Nevada metamorphic belt. Adapted from U.S. Geological Survey and California Division of Mines and Geology (1966).

Regional metamorphism is generally of low grade, in the greenschist facies. Original textures and structures are preserved in much of the belt but were destroyed by dynamic metamorphism in some places.

The metamorphic belt discussed here underlies the gentle western slope of the Sierra Nevada, a tilted block having a steep eastern slope that is partly a fault scarp. Most of the western slope is a moderately rolling and deeply weathered upland surface formed during Late

Cretaceous and early Tertiary time. As a consequence of westward tilting during the late Tertiary, this surface is dissected by youthful canyons cut by streams draining west and southwest toward the Great Valley. Canyon walls are in many places steeper than the angle of repose, and debris from rockslides is common along major streams. Depth of the canyons varies from about 5,000 feet (1,500 m) in the eastern part of the region to a few tens of feet near the margin of the Great Valley.﻿INTRODUCTION

3

Most major roads in the region follow the upland surface and, in general, parallel the canyons; only one major road runs northward through most of the area. Other roads crossing river canyons are steep and tortuous.

The vegetation reflects progressively higher rainfall and altitudes eastward from the edge of the Central Valley toward the crest of the Sierra Nevada. Elevations of about 300-500 feet (90-150 m) are marked by grassland, and groves of deciduous trees are common at elevations of about 1,000 feet (300 m). Conifers become prominent at about 2,000 feet (600 m) altitude and are dominant at greater altitudes.

Much of the total California gold production was obtained from placer and lode mines in the northern Sierra Nevada, and the present towns of the region were established as centers of gold-mining activity. Copper and chromite were also mined in the past, but in 1973 little metal-mining activity in the northwestern Sierra Nevada remains. However, production of aggregate, limestone products, roofing granules, and other industrial materials has grown in response to the requirements of rapid population growth and industrialization in northern California.

PREVIOUS WORK

No attempt is made to present a complete bibliography of the numerous publications treating various aspects of the geology of the northwestern Sierra Nevada. Papers cited below provide a summary of the evolution of knowledge of the stratigraphy and structure of the region, and additional papers are cited elsewhere in this report.

Although more recent studies have made valuable contributions, the regional investigation described here was made possible by a series of geologic folios spanning the northern Sierra Nevada that were prepared between 1890 and 1900 by Lindgren and Turner (cited elsewhere in this report). These maps show rock distribution with considerable accuracy, although their structural interpretations are inadequate by modern standards and volcanic formations were treated as igneous rocks having no stratigraphic significance. Ferguson and Gannett (1932), in their study of the Alleghany mining district, refined the breakdown of lithologic units exposed near Alleghany. They were the first to recognize a major fault in that part of the Sierra Nevada and to suggest that it was an extension of a great reverse fault previously recognized by Knopf (1929, p. 46) along the Mother Lode, south of the area described here.

Although most of Taliaferro’s (1942, 1943) work on the western Sierra Nevada was in the part of the metamorphic belt that lies south of the area of this

report, his contributions to our knowledge of the stratigraphy and structure of the Jurassic rocks aid in understanding the northern part of the metamorphic belt. Hietanen (1351) and Compton (1955) studied chiefly the petrolo^ y of metamorphic and plutonic rocks in the northwestern part of the metamorphic belt, but their work also elucidated the structure of the metamorphic rock > as well as structural relations between the intrusive bodies and their wallrocks. Radiometric dates on isolated felsic plutons in the metamorphic belt md in the Sierra Nevada batholith, summarized by Evsrnden and Kistler (1970), are a valuable aid in work ng out the complex structural and intrusive history of the western Sierra Nevada. The regional geologic map accompanying this report was adapted from Burrett and Jennings (1962) and Strand and Koenig (1965). Among the sources cited by Burnett and Jennings for their compilation are unpublished maps by geologists of the Southern Pacific Company; their maps are not cited in the list of references herein.

FIELDWORK AND SCOPE

OF THIS INVESTIGATION

Field mapping during this regional study was chiefly along major streams where exposures are nearly continuous and stream-polished surfaces facilitate observation of textures and minor structures. The purpose of the fieldwork was to obtain new structural and stratigraphic information that could be used to supplement existing information, chiefly from the folios by Turner and Lindgren, and thereby yield new structural and stratigraphic interpretations. Neither the plutonic rocks nor the Cenozoic strata that unconformably over-lie the metamorphic rocks were studied.

Field observations, occupying a total of about 9 months during 1955 to 1961 inclusive, were compiled mostly on 1:24,000-scale topographic maps (fig. 2) but partly on aerial photographs.

Results of detailed mapping, together with the reports and maps of previous investigators, were used to compile a regional map (pi. 1) at a scale of 1:316,800. Strip maps and cross sections were prepared at a scale of 1:62,500 for most of the streams studied and have been published separately (Clark and Huber, 1975). These maps or the topographic quadrangle maps will be required for location of some of the place names referred to in this report. Along much of the Bear River and lower part of the Middle Fork of the American River, preparation of detailed cross sections was not warranted because gravel choking the stream channels conceals the bedrock. Rocks exposed along the Middle Feather River and Slate Creek are so sheared that detailed cross sections would show only steeply dipping schistosity and small widely separated bodies of bedded rocks.﻿4

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

120° 15'o

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121°45’	t20° 15'

Figure 2.—Index of topographic quadrangle maps within and bordering the north half of the western Sierra Nevada metamor-phic belt.

ACKNOWLEDGMENTS

N. King Huber and Hal G. Stephens assisted in the fieldwork as indicated on the individual geologic maps, and Huber also contributed to a petrologic study of the Shoo Fly Formation. Cordell Durrell freely discussed results of his work on the petrology of the Shoo Fly Formation and showed me in the field the stratigraphic and structural relations that he had established during his study of the northeastern Sierra Nevada. Discussions with Vernon McMath on results of his work in the Taylorsville area contributed to an understanding of Paleozoic stratigraphy in part of the report area. Ralph Imlay’s diligent search for fossils in the usually barren Jurassic tuff and siltstone resulted in discoveries that contributed substantially to the stratigraphic interpretations of this report.

TERMINOLOGY

Terminology used herein is similar to that in the earlier report on the southern part of the metamorphic belt (Clark, 1964, p. 5-6) but will be repeated for ease of reference. Because the emphasis of this study is on stratigraphy, most of the lithologic terms, such as "sandstone” and "pillow lava,” relate to the original character of the rock rather than to their metamorphic

equivalents. Nevertheless, conspicuous metamorphic planar structures in most of the fine-grained rocks are reflected in the use of the terms "slate,” "phyllite,” or "schist” rather than "siltstone” or "shale.” Some rocks of volcanic origin in which original structures were obliterated by metamorphism are referred to simply as "metavolcanic rocks.”

Original textures and structures of pyroclastic rocks forming much of the volcanic formations are indistinguishable from those of rocks of similar grain size composing the sedimentary formations. This similarity indicates that both sandstone and tuff, for example, were transported and deposited in the same manner— they are both sedimentary rocks. The significant difference between them is the origin and manner of comminution of the component fragments. In recognition of this, shale, sandstone, conglomerate, and the like are designated "epiclastic” rocks to indicate that the component debris was formed by weathering of preexisting rocks.

The term "graywacke” designates poorly sorted sandstone with a matrix of silt-size and clay-size material (Pettijohn, 1957, p. 290-292.) The sand grains in the graywacke are mostly chert or other lithic fragments, but various amounts are mineral grains, most commonly quartz. Rocks in which the sand-size fraction consists entirely of volcanic rock and mineral detritus are called tuff, but those containing even widely scattered grains of nonvolcanic material are called graywackes. No fundamentally important aspect of the interpretation of geologic history of the region is masked by this usage, as sequences of definite volcanic material alternate with sequences of definite epiclastic material on both the regional scale and the scale of a single formation. The term "tuffaceous sandstone” is used only where it is known that the rock contains both grains formed by epiclastic processes and first-cycle grains formed by pyroclastic processes.

Two kinds of conglomerate are distinguished: the gravelly conglomerate or paraconglomerate collected by ordinary water currents (Pettijohn, 1957, p. 254) and very poorly sorted conglomeratic mudstone (Pettijohn, 1957, p. 254) or pebbly mudstone (Crowell, 1957, p. 994), which in the western Sierra Nevada was emplaced as mudflows. Most conglomerate and conglomeratic mudstone in metamorphic rocks of this region are immature, for preserved in them are abundant pebbles of readily weathered rocks such as slate, tuff, and limestone. Such conglomerates are termed "petromict” (Pettijohn, 1957, p. 255).

Flaser rocks occupy most of the wide fault zones in the area. They result from shearing and are marked by phacoidal rock fragments and by pronounced line and planar structures (Tyrrell, 1929, p. 286, fig. 69). Some﻿SUMMARY OF GEOLOGY

5

narrower fault zones are filled with cataclasite, "a structureless aggregate of fragmental material of various sizes” (Tyrrell, 1929, p. 284).

In the absence of a purely descriptive term, the name "chert” is applied to microcrystalline, granoblastic rocks composed of quartz. Bedding characteristics and sparse structure suggestive of replaced radiolaria imply that these rocks were indeed derived from chert. In this area, such rocks have been referred to by most previous workers as either phtanite or quartzite. Phtanite has fallen into disuse in this country, and although quartzite is often used as a descriptive term, it suggests a rock formed from quartz sand. Most of the chert is sericitic, and rock containing so much sericite that it can be scratched with a hammer point is here referred to as quartzose slate.

Three terms, "cleavage,” "schistosity,” and "slip cleavage,” distinguish different kinds of parting surfaces of metamorphic origin. Cleavage designates the planar structure characteristic of slate, the slaty cleavage referred to by many authors. In this region, development of cleavage is widespread. It has formed in fine-grained pyroclastic rocks and sandstones as well as slate. It commonly crosses bedding, forms a simple regional pattern, and in places is about parallel to the axial planes of folds. Schistosity designates a planar structure formed by the parallel arrangement of tabular mineral grains and clastic fragments in rocks sufficiently coarse grained to be termed schist. In strongly sheared schist, slip surfaces parallel to grains and fragments accentuate the cleavage. Slip cleavage consists of closely spaced crinkles and microfaults (White, 1949) cutting earlier schistosity and cleavage. Mica flakes formed prior to the slip cleavage are commonly bent to a direction parallel to the microfaults.

SUMMARY OF GEOLOGY

Metamorphic rocks in the northwestern Sierra Nevada were derived from eugeosynclinal volcanic and epiclastic rocks of Paleozoic and Mesozoic age. Most of the rocks are of low to intermediate metamorphic grade, but higher grade contact metamorphism is evident near some plutonic contacts. Bedding and original textures are distinguishable in most of the region but have been destroyed by development of metamorphic planar and linear structures in large parts of the area. Fossils are sparse, and some large bodies of metamorphic rock have not been dated. Formational units are measurable in thousands of feet, and structural and stratigraphic continuity are interrupted by nearly vertical faults having large displacements.

There are some compositional differences between Paleozoic and Mesozoic rocks, but there are also similarities between the two groups that preclude using

lithologic similarity to correlate unfossiliferous map units. Bodies of mafic intermediate volcanic rocks in the central part of the map area, for example, must be considered to be of Paleozoic or Mesozoic age until they can be dated, for late Paleozoic gastropods and Jurassic ammonites have been found in similar-appearing tuff exposed at different localities.

In general, Mesozoic (Jurassic and probable Jurassic) rocks underlie the western third of the map area (pi. 1) and form a narrower belt in the eastern part. Paleozoic rocks crop out between the two belts of Mesozoic rocks and in a small area east of Auburn. The preponderance of east-facing bedding tops suggests that the central position of the Paleozoic rocks results from faulting combined with regional tilting.

The oldest known rock in the western area is limestone containing tabulate corals and stromatoporoids of probable Devonian age, which is exposed 3 miles (4.8 km) east of Auburn (pi. 1). The limestone is apparently interbedded with volcanic rocks exposed in the immediate vicinity, but there is no assurance that all these volcanic rocks are of the same age. The volcanic rocks are of mafic to intermediate composition, but in the northern part of the unit, petromict conglomerate and bedded chert are interbedded with the volcanic rocks.

The Shoo Fly Formation, exposed in the eastern part of the map area, can be partly correlated with the Silurian Taylorsville Formation north of the area of plate 1. The Shoo Fly Formation is divided into lower and upper lithologic members. The lower member, exposed east of the north-trending fault zone in the central part of the map area, consists largely of dark-gray slate but includes some bedded chert and sparse petromict conglomerate. The upper member consists largely of quartzose and locally feldspathic sandstone here referred to as graywacke. Subordinate rock types in the upper member are slate, quartzite, carbonate rocks, and mafic and felsic volcanic rocks. In the earlier report on the southern part of the metamorphic belt (Clark, 1964), rocks of the Shoo Fly Formation were included in the Calaveras Formation.

The late Paleozoic Calaveras Formation is exposed in a wedge between two major fault zones in the north-central part and in a small area at the south edge of the map area (pi. 1). The Calaveras Formation consists largely of thinly interbedded chert and carbonaceous slate or phyllite. It includes some mafic lava and mafic or intermediate pyroclastic rocks and lenses of crinoidal limestone. Nearly everywhere in the map area, bedding in the Calaveras Formation has been destroyed by shearing.

Unnamed volcanic rocks exposed in the vicinity of Gold Lake in the northeastern part of the map area are﻿6

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

believed by Durrell and Proctor (1948, p. 171) to be of late Paleozoic age. They found that these rocks consist from bottom to top of metarhyolite with a thin basal conglomerate derived from the Shoo Fly Formation, a sequence of interbedded chert, slate, and mafic tuff, and a thick series of mafic lava flows and tuffs.

Several other Paleozoic formations have been recognized previously in the northwestern Sierra Nevada, mostly as a result of mapping during the latter part of the 19th century. The present investigation indicates that the definition of some of these formations does not coincide with the outcrop pattern of lithologic units, and so detailed mapping is necessary to establish their validity.

Some rocks in the northern part of the map area are mapped as epiclastic rocks of Paleozoic and Mesozoic age. These rocks are lithologically similar to Jurassic formations described below, but since no fossils were found in them, the present information does not preclude the possibility that these rocks accumulated during the Paleozoic. Several long narrow belts, chiefly near the fault zone that extends through La Mar Flat and Auburn, were mapped by Lindgren (1894) as the Calaveras Formation. Along the Bear River on the same fault zone, rocks also mapped as the Calaveras Formation by Lindgren and Turner (1895) are (laser rock derived from volcanic rocks of Jurassic age.

Undated volcanic rocks in the central part of the area are mapped as metavolcanic rocks and assigned a Paleozoic or Mesozoic age. They are largely of mafic or intermediate composition but include some felsic rocks. Most rocks of this unit are schistose, but some are massive as a result of recrystallization; fine-grained bedded tuff exposed along the Middle Yuba River east of the mouth of Humbug Creek is included in this unit.

A chert breccia and limestone unit of Triassic(?) age overlies the Shoo Fly Formation with pronounced angular unconformity in the eastern part of the area near the North Fork of the American River. The lower part consists of coarse chert breccia derived from the Shoo Fly Formation. The upper part consists of limestone, which is commonly argillaceous.

The Triassic(?) rocks are overlain by the Sailor Canyon Formation from which ammonites of Early and Middle Jurassic age were collected. The Sailor Canyon Formation consists of slate derived from siltstone, graywacke, and tuff but contains sparse calcarenite. Bedding in the Sailor Canyon Formation is apparently concordant with that in the underlying carbonate rock, but relief on the intervening contact suggests an erosional unconformity.

Along the North Fork of the American River, the Sailor Canyon Formation grades upward through a zone marked by an increasing proportion of volcanic

rocks into a section composed of mafic or intermediate volcanic rocks that are assigned to the Milton Formation. In its type area, near Milton Reservoir (pi. 1) in the northeastern part of the map area, the Milton Formation consists predominantly of mafic or intermediate pyroclastic rocks but contains some felsite tuff, calcarenite, and epiclastic breccia. No fossils have been reported from the Milton Formation.

The Cosumnes Formation of Taliaferro (1942, 1943), exposed in a belt extending discontinuously from the vicinity of Colfax to the south boundary of the map area, contains ammonites of early Late Jurassic age. The Cosumnes has been abandoned as a formational name, as discussed in a later section of this report, and rocks originally defined as the Cosumnes Formation are herein informally called "Cosumnes-type rocks.” Cosumnes-type rocks are predominantly slate and graywacke, but tuff, petromict conglomerate, and conglomeratic mudstone are commonly interbedded with these. Blocks several feet long are common in the pebbly mudstones, and one well-exposed block, probably derived from the Calaveras Formation, is about 30 feet (9 m) long and 15 feet (4.5 m) wide.

Near the south boundary of the map area, Cosumnes-type rocks are overlain by the Late Jurassic Logtown Ridge Formation, which consists of pyroxene-bearing pyroclastic rocks and some pillow lava. Near the North Fork of the American River, the Cosumnes-type rocks are overlain by volcanic rocks possibly equivalent to the Logtown Ridge Formation.

The Monte de Oro Formation, exposed in a small area near Oroville in the northwestern part of the map area, is of Late Jurassic age, but the stage is uncertain; study of the fauna (Imlay, 1961, p. D8) suggests a late Oxfordian and early Kimmeridgian age, whereas later investigation of the flora (Fry, 1964) suggests a late Oxfordian to and including Portlandian age. If part of the Monte de Oro Formation is as young as Portlandian, it is the youngest unit yet dated in the metamorphic belt, but this remains to be confirmed. The Monte de Oro Formation, like other Late Jurassic epiclastic units, consists mostly of slate, graywacke, and polymictic conglomerate but is distinguished by the presence at its base of crossbedded sandstone and conglomerate of apparent littoral origin. The sandstone and conglomerate consist largely of debris from volcanic rocks but contain pebbles of vein quartz and fossiliferous limestone.

The Copper Hill Volcanics, named by Clark (1964), is exposed near the southwest corner of the map area. It is also one of the youngest formations in the metamorphic belt, for it intertongues with and overlies the Salt Spring Slate of Late Jurassic (Kimmeridgian) age.

Some bodies of epiclastic rocks in the central and eastern parts of the area have been mapped as epiclastic﻿SUMMARY OF GEOLOGY

7

rocks of Jurassic age. Although no fossils were found in this map unit, stratigraphic and structural relations suggest that the strata are of Late Jurassic age. In the southern part of the area, this unit consists of slate, graywacke, and tuff and overlies the Logtown Ridge Formation of Late Jurassic (Callovian to late Oxfordian or early Kimmeridgian) age. Northward this unit is mostly dark-gray phyllite, but it contains some volcanic rocks and bedded chert. No top directions were found in these epiclastic rocks, but east-facing tops in volcanic rocks overlying Cosumnes-type rocks to the west suggest that the epiclastic rocks may also be east facing. The epiclastic rocks of Jurassic age, near the eastern side of the map area, consist largely of dark-gray hornfels along the North Fork of the American River but contain thin layers of conglomeratic mudstone and sparse quartzite layers. Top directions suggest that these strata overlie the Milton Formation.

Volcanic rocks that underlie much of the western third of the map area are assumed to be of Jurassic age; in most places they are moderately deformed and are exposed along the projection of a belt of similarly deformed Late Jurassic rocks that extends about 100 miles southeastward from the boundary of the map area of plate 1. The unit is mostly tuff and volcanic breccia, but lava flows, with some pillow structure, occur in some places. Field relations suggest that a body of volcanic rocks north of Greenwood, which is included with this unit, is possibly equivalent to the Logtown Ridge Formation, but there is little information to suggest the age of other bodies included in the same unit.

Plutonic rocks, not studied in detail during this investigation, are mostly, if not entirely, of Jurassic and Cretaceous age. Similar to plutonic rocks south of this report (Clark, 1964, p. 41-42), they range in composition from ultramafic through a diverse assemblage of less mafic intrusive and metamorphic rocks to granodiorite. Serpentine, most abundant of the ultramafic rocks, is associated chiefly with sheared metamorphic rocks in major fault zones west of the Shoo Fly Formation. Rocks of gabbroic aspect, identified in this report as mafic plutonic rocks of Paleozoic or Mesozoic age, include medium- to coarse-grained contact metamorphic rocks as well as rocks of intrusive origin. Most of these plutonic rocks are generally considered to be parts of the composite Sierra Nevada batholith.

The present distribution of metamorphic rocks in the region results chiefly from folding and reverse faulting during Late Jurassic and, possibly, Early Cretaceous time, but at least one deformation, and probably two, preceded deposition of the Late Triassic(?) carbonate rocks. The facings of bedding tops across the area underlain by Jurassic volcanic rocks are unknown, but

facings across Cosumnes-type rocks, the Shoo Fly Formation, and the eastern belt of Mesozoic rocks are generally eastward. The order of succession of strata that would be inferred from bedding facings is reversed as a result of movement along the fault zone at the west boundary of the Shoo Fly Formation, the west boundary of the Calaveras Formation, and the west boundary of the Paleozoic and Mesozoic mafic intrusive and metamorphic rocks. Along all of these faults, younger strata underlie older, and the faults thus divide the area into four structural blocks (fig. 3). These major fault, zones were originally thought to have predominantly strike-slip displacement (Clark, 1960, 1964), but more recent data derived from many ongoing studies in the Sierra Nevada suggest that they are steeply eastdipping reverse fault zones (Bateman and Clark, 1974).

The fault zone along the west side of the Calaveras Formation extends the full length of the metamorphic belt, a distance of about 180 miles (290 km), and throughout nearly the whole distance, the fault forms the boundary between Jurassic rocks on the west and Paleozoic rocks on the east. This fault is the northward extension of the Melones fault zone described previously (Clark, 1964). The fault zone at the west side of the Shoo Fly Formation can be traced from the north end of the

Figure 3.—Fault-bounded structural blocks of the north half of the western Sierra Nevada metamorphic belt.﻿8

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

metamorphic belt many miles southward and is inferred to continue to the south margin of the map area. It is likely that a fault zone of this magnitude continues even farther south, but this has not been established. The third fault zone, that on the west side of the undivided Mesozoic and Paleozoic rocks, appears to trend southward into the Bear Mountains fault zone (Clark,

1964). Other fault zones shown on plate 1 exhibit smaller stratigraphic separation and presumably had less total movement than the three fault zones mentioned above.

Lineations and minor fold axes within the fault zones and in many places outside of the fault zones plunge steeply. The lineations consist of amphibole crystals, mineral pods, and elongate rock fragments in a matrix of schist or crush rock. Minor folds having steeply plunging axes are marked by deformed slip and schistosity surfaces.

Recumbent folds in the southern part of the area underlain by the Shoo Fly Formation probably mark the earliest folding recorded in the region. Recumbent folds were not observed north of the Middle Fork of the American River, but bedding-plane schistosity, which is associated with the recumbent folds in the southern part of the area, was recognized as far northward as the North Yuba River. Complicated structure and steeply plunging fold axes in the eastern part of the Shoo Fly Formation along the North Fork of the American River suggest that the Shoo Fly Formation was folded more than once before the overlying Late Triassic(?) rocks were deposited.

Regional strikes and large folds in the Jurassic rocks result from folding about gently plunging northwesttrending axes. This stage of folding also accounts for the generally homoclinal structure of the eastern belt of Jurassic rocks, homoclinal structure of Jurassic strata exposed near State Highway 49 in the southern part of the area, and folds south of Lake Folsom and in the vicinity of Colfax (pi. 1). Folds in the area underlain by Jurassic volcanic rocks are of diverse orientation, but bedding attitudes near Oroville, northeast of Smart-ville, and near Colgate Power Station are concordant with the regional trend attributed to this stage of deformation. Where age relations of folds and faults in Late Jurassic rocks were determined, the faults are younger.

Near the north boundary of the map area, strikes of regional structures swing westward and project toward the Klamath Mountains (fig. 1; pi. 1). The part of the gross structure that is exposed in the northwestern Sierra Nevada is an anticline whose axis plunges steeply to the northeast. Felsic plutons in the northwestern part of the area are clustered in the axial region of this anticline. According to Compton (1955), plutons

of this group that he studied were intruded by stopping and pushing aside wallrocks. Although Compton’s evidence for both of these processes is convincing, it is possible that development of the anticline aided the magma in pushing aside the wallrocks.

PALEOZOIC ROCKS

All metasedimentary and metavolcanic rocks in the area described here were included in the Calaveras Formation as defined by Turner (1893a, p. 309; 1893b, p. 425). In part of the area (Colfax 30-minute quadrangle), Lindgren (1900) later divided the Calaveras Formation into the Blue Canyon Formation, Relief Quartzite, Cape Horn Slate, Delhi Formation, and Clipper Gap Formation at the expense of Turner’s name Calaveras. In the vicinity of Alleghany, Ferguson and Gannett (1932, p. 6-7) recognized two older formations, the Tightner and Kanaka Formations, which Lindgren had previously mapped simply as "amphibolite.”

Of the formation names listed above, only the name Calaveras Formation is used on maps accompanying this report, and it is considerably restricted from Turner’s original definition. The name Blue Canyon Formation was abandoned by Clark, Imlay, McMath, and Silberling (1962, p. B17) when its rocks were found to be part of the Shoo Fly Formation named previously by Diller (1892). Although the boundaries of other units as previously mapped do not consistently correspond to lithologic boundaries found during this investigation, their names, even though not used on the maps accompanying this report, should not be abandoned until more detailed mapping is available. Problems related to use of these formation names are discussed later.

SHOO FLY FORMATION

The name Shoo Fly Formation was applied originally by Diller (1892, p. 375; 1908, p. 23) to a distinctive and uncommon sequence of stratified rocks exposed north of the 40th parallel and 5-10 miles (8-16 km) southwest of Taylorsville. Subsequently, other parts of a continuous belt containing the same lithologic assemblage were assigned to the Calaveras Formation or Group (Diller, 1895; Lindgren and Turner, 1894; Lindgren, 1896, p. 80-81; Turner, 1897, 1898) and to the Blue Canyon Formation (Lindgren, 1900). The name Shoo Fly Formation, having priority, was later extended to designate the entire belt of rocks characteristic of its type locality (Clark and others, 1962, p. B17). According to this usage, the Shoo Fly Formation underlies a belt as much as 20 miles (32 km) wide, extending the length of the map area (pi. 1). Its southern limit of exposure has not been determined; it was not differentiated from the Calaveras Formation in the earlier report (Clark, 1964). The formation is at least 5,000 feet (1,500 m) and proba-﻿PALEOZOIC ROCKS

9

bly more than 10,000 feet (3,000 m) thick. It is here divided into two intertonguing lithologic members, a lower member consisting largely of dark-gray slate and phyllite and an upper member consisting largely of quartz-rich graywacke, slate, and quartzite. Intertonguing relations are most readily observed near the mouth of Scotchman Creek 1 mile (1.6 km) east of Washington on the South Yuba River.

LITHOLOGY

The lower member of the Shoo Fly Formation is exposed in a narrow belt east of a major fault zone in the central part of the map area and forms the core of a steeply plunging fold along the Middle Fork of the American River. Thin-bedded chert, sparse coarse epiclastic rocks, and sparse metavolcanic rocks in addition to slate are found in the lower member of the Shoo Fly Formation. A layer of calcarenite about 20 feet (6 m) thick is interbedded with slate about 800 feet (240 m) southeast of the tunnel near Horseshoe Bar on the Middle Fork of the American River. Conglomerate consisting largely of slate, chert, and volcanic rock fragments crops out along the North Yuba River in the eastern part of Downieville. A similar conglomerate crops out about 50 feet (15 m) west of the bridge in Washington.

Conglomerate exposed along the Middle Fork of the American River at the northwest end of American Bar differs from those mentioned above in that it contains fragments of quartz-rich graywacke as well as slate and chert pebbles. The graywacke pebbles are very similar to graywacke in the upper member of the Shoo Fly Formation, suggesting either that rocks near American Bar are younger than the Shoo Fly Formation or that a tongue of quartz graywacke occurred at a lower stratigraphic position in the Shoo Fly Formation.

The upper member of the Shoo Fly Formation is a eugeosynclinal assemblage of rocks derived chiefly from a terrane composed of metamorphic and granitic rocks but partly from contemporaneous volcanic rocks. The formation consists largely of sandstone and slate or phyllite but includes subordinate thin-bedded chert, carbonate rocks, conglomerate, pebbly mudstones, intraformational breccia, and felsic and mafic volcanic rocks. Sandstone is predominant in most of the area, but slate and phyllite are predominant along the Middle Fork of the Feather River and near the east edge of the metamorphic belt along the North and Middle Forks of the American River.

Sandstones in the Shoo Fly Formation are medium to dark gray, bluish gray, or greenish gray on fresh surfaces. Graywacke is the most abundant sandstone, but composition and texture are variable and even include well-sorted orthoquartzite. The coarsest frac-

tion in most of the graywacke is medium to very coarse sand, but some graywackes, particularly in the southern part of the area, contain granules. The matrix of the sandstones consists of white mica, quartz, and feldspar. Quartz is the dominant detrital mineral, and in some graywackes, as well as in the orthoquartzites, it constitutes more than 90 percent of the sand fraction. Potassium feldspar and plagioclase are found in much of the graywacke and in some places constitute about 10 percent of the sand and granule fractions. Sparse sand grains composed of granoblastic microcrystalline quartz are probably derived from chert. Most beds are between about 4 and 20 inches (10 and 50 cm) thick, but some beds are as much as 6 feet (1.8 m) thick. Graded beds are abundant throughout most of the area underlain by the upper member of the Shoo Fly Formation but are sparse along Silver Creek (pi. 1) where quartzite is the most abundant sandstone.

Under the hand lens, glassy quartz is commonly the only recognizable detrital component of the sandstones, but in some graywacke, grains of quartzite distinguished by a sugary texture and feldspar can be seen. Most quartz and quartzite grains are nearly circular or elliptical in outline, but in some feldspathic sandstones they are angular. Among the glassy quartz grains, colorless, gray, and opaline varieties can be distinguished.

In thin section both monocrystalline and polycrystalline quartz grains can be distinguished. Nearly all show undulatory extinction, but because the Shoo Fly Formation is itself deformed, it is difficult to distinguish provenance on this basis alone. Many monocrystalline quartz grains have fluid inclusions, and others contain needlelike inclusions, probably of rutile. Internal boundaries of some polycrystalline grains are characterized by many straight segments, suggesting that these grains were derived from vein quartz or possibly from granitic rocks. Sparse grains, possibly derived from quartzite, have exceptionally pronounced undulatory extinction, marked internal planar structure, and deeply sutured internal boundaries.

The upper member of the Shoo Fly Formation contains coarse-grained clastic rocks of both extrafor-mational and intraformational origin; conglomerate consisting of well-rounded fragments of quartz in a matrix of coarse sand is most abundant. In most conglomerates the fragments are 1 inch (2.5 cm) or less in diameter. Most pebbles are colorless vein quartz, but some conglomerates contain pebbles of gray vein quartz and, particularly in the southern part of the area, of quartzite. A conglomerate exposed along Camp Creek that consists mostly of well-rounded quartz pebbles also contains angular slabs of black slate of probable intraformational origin.﻿10

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

Conglomeratic mudstone more than 20 feet (6 m) thick is exposed at the base of the Commodore mine trail on the Middle Yuba River. The mudstone consists of fragments of very fine grained felsite or slate and dolomite in a matrix of dark-gray phyllite. The dolomite blocks are as much as 4 feet (1.2 m) long. Another very poorly sorted breccia of probable mudflow origin, exposed along the North Fork of the American River in the western part of sec. 4, T. 15 N., R. 11 E., consists of fragments of slate, chert, quartz-rich graywacke, limestone, and volcanic rocks in a slate matrix. Intraformational granule conglomerate beds less than 2 feet (0.6 m) thick are exposed on the divide between the mouth of Big Granite Creek and the North Fork of the American River. The granules are rounded and consist of chert similar to that in the enclosing beds.

Chert in the upper member of the Shoo Fly Formation is interbedded with gray and gray-green slate and phyllite. Most of the chert is light to medium gray, grayish green, or grayish blue and forms beds that are mostly less than 4 inches (10 cm) thick. In thin section, the chert is seen to be chiefly granoblastic quartz, but much of the chert contains white mica. Some chert contains round or elliptical bodies of more coarsely crystalline quartz that are possibly replaced radiolarians.

Carbonate rocks constitute less than 1 percent of the upper member of the Shoo Fly Formation but are widely distributed. Most of the carbonate rocks are in parts of the section where orthoquartzitic sandstone and slate predominate over graywacke. Limestone, the most abundant carbonate rock, is mostly light- to dark-gray calcarenite containing detrital quartz and feldspar. Original textures of most of the carbonate rock are lost as a result of recrystallization, but in some thin sections, fragments of crinoid plates and echinoids can be distinguished. The noncarbonate fraction varies from less than 10 percent to about 50 percent and is comparable to the better sorted sandstones with respect , to quartz-feldspar ratios.

The largest carbonate body found in the upper member of the Shoo Fly Formation is best exposed on the north wall of the Middle Fork of the Feather River Canyon about 3 miles (4.8 km) west of the mouth of Nelson Creek. The body contains dolomite, limestone, and dolomitic limestone and some interbedded poorly sorted orthoquartzite and quartz-pebble conglomerate. Limestone in this body is similar to that previously described, but the dolomite and dolomitic limestone contain closely packed pisolites as much as one-fourth inch (6 mm) in diameter. In some specimens the pisolites are completely replaced by chert, and in others only the matrix or a thin shell on the periphery of pisolites is replaced by chert.

Although felsic volcanic rocks probably contributed detritus to sandstones in the Shoo Fly Formation, mafic

volcanic rocks have been identified in only a few places. Pillow lava is associated with felsic volcanic rocks along the Middle Yuba River in the SE14 sec. 9, T. 19 N., R. 12 E. Felsic tuff occurs along the North Fork of the American River about a quarter of a mile (0.4 km) east of the mouth of Big Granite Creek but is more abundant near the granitic pluton that intrudes the upper member of the Shoo Fly Formation along Canyon Creek and the Middle Yuba River. Felsic volcanic rocks are interlayered with epiclastic rocks of the Shoo Fly Formation west of the pillow lava and along the North Yuba River; felsite tuff, partly quartz bearing, occurs between Sierra City and the small pluton to the west.

Abundant felsite dikes, many containing quartz and feldspar phenocrysts, cut the Shoo Fly Formation along the Middle Yuba River east of the large pluton, suggesting a possible genetic relation between the pluton, dikes, and felsic pyroclastic rocks.

STRATIGRAPHIC RELATIONS

The lower member of the Shoo Fly Formation is in fault contact with rocks exposed to the west. On the east, the upper member is unconformably overlain by volcanic rocks of late Paleozoic age in the northeastern part of the area and by Late Triassic(?) and Early Jurassic rocks near the North Fork of the American River.

Durrell and Proctor (1948, p. 175) found that in the northeastern part of the area rocks here included with the Shoo Fly Formation were folded before the overlying late Paleozoic rocks were deposited but that the angular discordance at the contact is small. They suggested that the pre-late Paleozoic folding was not severe and that intricate folds in the Shoo Fly Formation probably are mostly the result of a later deformation during which the Shoo Fly Formation and the more competent overlying rocks were folded together. In contrast, the Shoo Fly Formation near the North Fork of the American River is overlain with pronounced angular unconformity by rocks of Triassic(?) age (Lindgren, 1900, p. 2-3; Clark and others, 1962). The contact is well exposed on the north side of the canyon of the North Fork of the American River and near New York Canyon (Clark and others, 1962, fig. 6.1). The Shoo Fly Formation is immediately overlain by chert breccia. Both bedding and cleavage in the Shoo Fly Formation are truncated at the contact. Although the contact is a nearly straight line at map scale, it shows in detail a relief of several feet. In some places the contact alternately follows bedding of the Shoo Fly Formation and fracture surfaces that cut across that bedding. Owing to complex folding near the contact, the angle of unconformity between the Shoo Fly Formation and the overlying strata varies from near 0° to near 90°.﻿PALEOZOIC ROCKS

11

AGE

The Shoo Fly Formation has yielded few fossils, but according to Clark, Imlay, McMath, and Silberling (1962, p. B17-B18) and McMath (1966, P. 176,179), who correlated its upper part with the more fossiliferous Montgomery Limestone of Silurian age (Diller, 1908, p. 16) exposed near Taylorsville, the Shoo Fly Formation is of Silurian age. Four fossil localities have been attributed previously to the Shoo Fly Formation. Of two localities described by Lindgren (1900, p. 2), one is in a limestone exposed near the confluence of Big Granite Creek and the North Fork of the American River that was subsequently shown to be of Triassic(?) age, and the other yielded fossils that suggested only Paleozoic age. Diller (1908, p. 23) found "Carboniferous fossils, such as Fusulina” near Spanish Ranch, north of the area of this report, in rocks that he considered correlative with the Shoo Fly Formation, but McMath (1966, p. 178) considered that rocks at this locality are almost certainly separated from the Shoo Fly by a fault. Poorly preserved stromatoporoids suggesting a Devonian or Mississippian age were found by Clark (1930) in a chert lens near the contact between the Shoo Fly Formation and an overlying volcanic sequence southwest of Long Lake. His description of the locality does not permit unequivocal assignment of the fossiliferous rocks to either the Shoo Fly Formation or the overlying volcanic sequence.

McMath’s (1966) extension of the name Shoo Fly Formation, the type locality of which is in the lower plate of a thrust near Taylorsville, to the nearby upper plate is based upon lithologic similarity of the Shoo Fly and overlying units in both plates. The type Shoo Fly Formation in the lower plate west of Taylorsville consists of the same assemblage of sandstones and slates that characterizes the formation elsewhere. An overlying unit in the Shoo Fly Formation is about 2,000 feet (600 m) thick and consists largely of black or grayish-green obscurely laminated phyllite and slate and also thin beds, commonly graded, of feldspathic, possibly tuffaceous graywacke. The same sequence occurs in the Shoo Fly Formation in the upper plate.

CALAVERAS FORMATION

The Calaveras Formation as mapped during this investigation includes rocks named the Blue Canyon Formation, Relief Quartzite, Cape Horn Slate, and Delhi Formation by Lindgren (1900) in the Colfax 30-minute quadrangle and rocks assigned to the Calaveras Formation by Turner (1897, 1898) and Lindgren and Turner (1894) in the Downieville, Bidwell Bar, and Placerville 30-minute quadrangles.

The Calaveras Formation consists largely of in-terbedded chert and dark-gray commonly graphitic phyllite with subordinate interbedded mafic and inter-

mediate volcanic rocks and sparse lenses of carbonate rock.This assemblage of rocks closely resembles a unit mapped as undivided argillaceous and chert members of the Calaveras Formation in the southern part of the metamorphic belt (Clark, 1954, p. 5-8; 1964, p. 8) and is probably stratigraphically equivalent to that unit. Strong shearing of the Calaveras F ormation precludes a meaningful estimate of its thickness.

The Calaveras Formation is nearly everywhere in fault contact with adjacent metamorphic rocks. Possibly some blocks derived from the lower member of the Shoo Fly Formation have been mapped with the Calaveras Formation where the two units are separated only by fault zones or by fault zones and serpentine. The two map units are lithologically similar enough to make distinction difficult in greatly sheared areas.

The phyllite and most of the chert in the Calaveras Formation are dark gray on fresh surfaces and light gray where weathered. On stream-polished surfaces chert beds are commonly much lighter colored than the surrounding slate, apparently as a result of percussion figures and other fractures. The chert in which mica is sparse has a chalcedonic luster and conchoidal fracture. In thin section the chert is seen to consist of microcrystalline quartz containing in some places roundish blebs of more coarsely crystalline quartz that possibly are replaced radiolarians. Much of the chert contains some mica, and composition grades from phyllite with little quartz to chert with almost no mica. Chert and slate are not uniformly interbedded in the Calaveras Formation; near Sherman Bar, for example, thinly interbedded phyllite and chert form units as much as 80 feet (24 m) thick in a belt several hundred feet wide that consists mostly of phyllite. Bedding is preserved only locally and is strongly crumpled in these places.

A body of dark-gray fine- to medium-grained limestone or dolomite is exposed in an abandoned quarry on the east side of Bear River due west of Colfax. The rock contains abundant crinoid fragments, and corals were distinguished in one loose block. Foraminifera were recognized in thin sections. This body was considered by Lindgren (1900) to be a detached block of Clipper Gap Formation. Exposures are poor near the carbonate body, and its stratigraphic and structural relations to surrounding rocks are unclear. An exposure of sheared volcanic rock was found on the east side of the carbonate rock, and a small exposure of sheared epiclastic rock was found on the west side of it. The carbonate rock probably is a horse in a major fault zone (pi. 1) but is possibly a block that slumped into the area of deposition of the Cosumnes Formation of Taliaferro.

Tentatively included in the Calaveras Formation is a block, exposed in sec. 18, T. 17 N., R. 10 E., along the South Yuba River, that is bounded by faults. Most of the﻿12

WESTERN SIERRA NEVADA MET AMORPHIC BELT, CALIFORNIA

block consists, as does the formation elsewhere, of chert, phyllite, and mafic or intermediate volcanic rocks but also includes some epiclastic breccia and conglomerate. From the belt of schistose volcanic rocks exposed in sec. 17 westward, the rocks are as follows: a belt about 700 feet (210 m) wide of bedded chert with slate partings; massive locally fossiliferous tuff about 100 feet (30 m) wide; dark-gray phyllite about .75 feet (23 m) wide that contains some conglomerates; and mafic volcanic rocks, about 700 feet (210 m) wide, with interbedded chert. Most pebbles in the conglomerate are chert, but some consist of carbonate rock that contains fossil fragments. Breccia consisting largely of chert fragments, but containing some volcanic rock fragments, is exposed •near the mouth of New York Canyon on the South Yuba River. The breccia is possibly of tectonic origin but is not sheared, as is most tectonic breccia in the region. Small bodies of carbonate rock exposed about 200 feet (60 m) downstream from the mouth of New York Canyon are surrounded by volcanic rocks and are probably slivers in a narrow gently dipping fault zone. Coarse-grained epiclastic rocks are not characteristic of the Calaveras Formation but also were found along the Merced River (Clark, 1964, p. 10) south of the area described here.

FOSSILS AND AGE

Fossils found at three localities in the Calaveras Formation suggest a late Paleozoic age but do not permit closer age assignment. In view of the lack of stratigraphic control within the area mapped as Calaveras Formation, it is possible that rocks included in the formation span much of late Paleozoic time. Although crinoid fragments are abundant in many of the carbonate rocks of the Calaveras Formation, more diagnostic fossils are sparse. Permian fossils were collected from the southern part of the metamorphic belt (Clark, 1964, p. 13-14) from rocks that are not necessarily stratigraphically equivalent to the Calaveras Formation exposed in the area of this report.

A large isolated block of fossiliferous limestone is exposed along the Bear River west of Colfax. This block is believed to have slumped from an exposure of Calaveras Formation and been incorporated in the Cosumnes Formation of Taliaferro during Late Jurassic time. Lindgren (1900, p. 2), who first reported finding fossils in this limestone body, considered the limestone to be of early Carboniferous age on the basis of Clisiophyllum gabbi Meek, Lithostrotion whitneyi, and brachiopod fragments of various species. Helen Duncan (written commun., 1956) reported that a partly crushed and metamorphosed coral found at this locality during the present investigation is Stylidophyllum? sp. indet. She further stated that although Stylidophyllum is regarded as a zone fossil for the Permian by Asian

workers, her own work suggests that in parts of the western United States it is associated with Late Mississippian faunas. However, she believed it certainly to be of late Paleozoic age.

Fragmentary corals found in a small body of carbonate rock on the bank of the South Yuba River in the SWV4 sec. 18, T. 17 N., R. 10 E., were studied by W. J. Sando. He found (written commun., 1958) that although generic and specific determinations were impossible, one specimen appears to be a simple zaphrentoid coral and the others are possibly lithostrotionoid corals. He found the material suggestive of a late Paleozoic age but felt that further refinement of its stratigraphic implications could not be made.

Three external molds of gastropods were found in massive tuff exposed at the mouth of a small tributary canyon on the north side of the South Yuba River south of North Bloomfield, about 500 feet (150 m) west of the east boundary of sec. 18, T. 17 N., R. 10 E. The specimens were identified by Ellis Yochelson (written commun., 1958) as Euphemites, a bellerophontid gastropod ranging from Mississippian to Permian. Yochelson stated that the specimens do not appear to have been previously described, but show some similarities to Euphemites blaneyanus McChesney, and are more likely to be of Pennsylvanian than of Mississippian or Permian age. He did not believe that the specimens warranted a systemic designation.

RELIEF QUARTZITE

Lindgren (1900, p. 2) named the Relief Quartzite for exposures near the hamlet of Relief, about 3 miles (4.8 km) west of Washington, Nevada County. He mapped it as a belt of rock about 1 mile (1.6 km) wide extending from a point northwest of Washington to near Towle (pi. 1) along the line of a major fault zone. He described the Relief as a very hard grayish siliceous rock with streaks of siliceous clay slate and noted that the stratification planes are extremely contorted. Ferguson and Gannett (1932, p. 12) later correlated several bodies of schistose micaceous quartzite exposed in the vicinity of Alleghany with the type Relief Quartzite and extended the formation beyond its northern limit as mapped by Lindgren.

The Relief Quartzite is not differentiated on maps accompanying this report, and its validity as a formation is doubtful; the Relief Quartzite as mapped by Lindgren is a shear zone containing thin layers of serpentine and abundant sheared metamorphic rocks derived from formations exposed on either side of the shear zone (Clark, 1960, p. 490-491). Exposures along the South Yuba and Bear Rivers that were originally mapped as Relief Quartzite consist of blocks of volcanic rock and of chert in a matrix of flaser rocks.﻿PALEOZOIC ROCKS

13

Rocks mapped as Relief Quartzite by Ferguson and Gannett, in areas too small to plot on plate 1, were examined during this study only at a point along Kanaka Creek about 1% miles southwest of Alleghany. There, the rock is true quartzite, unlike the shear-zone assemblage originally mapped by Lindgren as Relief Quartzite. The quartzite near Alleghany constitutes part of a stratigraphic unit that is distinct from those shown on maps accompanying this report or, more probably, is in fault blocks detached from the upper member of the Shoo Fly Formation.

CAPE HORN SLATE

Lindgren (1900, p. 2) applied the name Cape Horn Slate to a unit of clay slate and sparse bodies of limestone typically exposed at Cape Horn, a prominent point overlooking the North Fork of the American River, about 2 miles (3.2 km) northeast of Colfax. The rocks form a belt lVfe-5 miles (2.4-8 km) wide that extends northward through the central part of the map area (pi. 1). During the present investigation, sparse bedded chert and volcanic rocks were found interbedded with the slate, and in the northern part of the area, chert and volcanic rocks are more abundant than slate. The lithology of the Cape Horn Slate does not appear either sufficiently distinctive or consistent to warrant retaining the name. Rocks in the southern part of the area that were mapped originally as Cape Horn Slate are here tentatively shown as epiclastic rocks of Late Jurassic age, and the more cherty rocks in the northern part of the belt are mapped as Calaveras Formation.

Lindgren (1900, p. 2) reported finding crinoid fragments in a small limestone body in the Cape Horn Slate below Cape Horn. This limestone is probably a fault block; it is in strata here included with Cosumnes-type rocks and is along the strike projection of conglomeratic mudstones exposed along the North Fork of the American River.

DELHI FORMATION

The Delhi Formation was named by Lindgren (1900, p. 2) for its typical development near the Delhi mine, about 5 miles (8 km) northwest of North Bloomfield, Nevada County. He stated that it consists mostly of dark-brown to black flinty rock that resembles hornfels and rarely shows bedding or schistosity. He noted that some rocks in the formation show a clastic character and others resemble chert. Crinoid fragments found in one of the few carbonate rock lenses in the formation suggested to Lindgren that the Delhi Formation is of Paleozoic age.

Most of the characteristics ascribed to the Delhi Formation by Lindgren were confirmed during this

investigation, but the absence of planar structures was not substantiated; rocks originally mapped as Delhi Formation show marked schistosity except in narrow zones of contact metamorphism near some intrusions. The Delhi Formation as mapped by Lindgren is indistinguishable from rocks mapped in the southern part of the metamorphic belt as undifferentiated chert and argillaceous members of the Calaveras Formation (Clark, 1964, p. 8), the formation to which its rocks are here reassigned.

CLIPPER GAP FORMATION

The Clipper Gap Formation was named by Lindgren (1900, p. 2) for exposures at the village of Clipper Gap, about 6 miles (9.6 km) northeast of Auburn in Placer County. He distinguished the Clipper Gap Formation only in the Colfax 30-minute quadrangle but stated that contiguous parts of the undivided Calaveras Formation in the adjacent Sacramento, Placerville, and Smartsville quadrangles should also be included in the Clipper Gap. As mapped by Lindgren, and subsequently by Chandra (1961, pi. 1), the Clipper Gap Formation includes a variety of rock types, some indistinguishable from rocks considered to be Jurassic by both authors. Stratigraphic problems are compounded by poor exposures, for most of the area underlain by the Clipper Gap Formation as originally mapped is a deeply weathered upland surface of moderate relief. The name Clipper Gap Formation probably should be abandoned, but more detailed mapping must precede formal action.

According to Lindgren (1900, p. 2), the Clipper Gap Formation consists of slate, argillaceous sandstone, bedded and massive chert, and limestone. Chandra (1961, p. 14) included grit and conglomerate in the formation, as well as the rock types listed by Lindgren. During the present investigation, mafic pyroclastic rocks and massive volcanic rocks were found to be common within the area mapped by Lindgren and Chandra as Clipper Gap Formation. Ellipsoidal por-phyritic lava of unknown extent and age is conspicuous along Interstate Highway 80 between Clipper Gap and Applegate (pi. 1), within areas formerly mapped as Clipper Gap Formation. The ellipsoidal lava is exposed in roadcuts that were made after Chandra’s work was completed.

In this report, epiclastic rocks assigned to the Clipper Gap Formation are mapped as Cosumnes-type rocks, and the volcanic rocks and chert, except for the ellipsoidal lava, are included with the undifferentiated Paleozoic and Mesozoic volcanic and sedimentary rocks. Contacts between these units in upland areas are generalized on plate 1. Graywacke, slate, petromict conglomerate, and conglomeratic mudstone exposed along Interstate Highway 80 between Bowman and﻿14

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

Applegate and along the North Fork of the American River, in areas previously mapped as Clipper Gap Formation, are indistinguishable from rocks characteristic of the Cosumnes-type rocks as used in this report. Chandra (1961, p. 17-18), noting the similarity of conglomeratic mudstones and conglomerates in the Clipper Gap Formation to those in the Mariposa Formation (Cosumnes-type rocks of this report), suggested that those in the younger strata had been derived from the older by submarine sliding. This interpretation is untenable because current-bedded conglomerate as well as conglomeratic mudstone occur in both units as previously mapped and because the conglomeratic mudstone and conglomerate are not interbedded with the chert-bearing part of the Clipper Gap Formation but overlie them where they were seen during this study. No difference in the proportions of such labile constituents as slate and carbonate rock pebbles has been noted between conglomerates and pebbly mudstones assigned to the Clipper Gap Formation and those of Jurassic age.

The Clipper Gap Formation was assigned an early Carboniferous age by Lindgren (1900, p. 2) on the basis of fossils found at three localities. The fossiliferous carbonate rocks at two of these localities are transported blocks. One such block, described by Lindgren as a small limestone mass and bearing fragments of crinoids and poorly preserved shells, crops out 2 miles (3.2 km) above Mammoth Bar along the Middle Fork of the American River in an area assigned by Lindgren to the Clipper Gap Formation but is here included with Cosumnes-type rocks. The locality could not be determined with certainty, but strata in this vicinity include conglomeratic mudstones with blocks of carbonate rocks that are as much as several feet long. Fossils at a second locality are in a limestone block west of Colfax along the Bear River, which Lindgren believed to have been torn loose from the main body of the Clipper Gap Formation by the intrusion of a diabase pluton. He reported finding here Clisiophyllum gabbi Meek, Lithostrotion whitneyi, and brachiopod fragments. The third locality is, from Lindgren’s description, apparently a limestone body exposed in a quarry in a small valley near the east boundary of sec. 8, T. 13 N., R. 9 E., and about 800 feet (245 m) south of the south portal of a Southern Pacific Railroad tunnel (Greenwood, Calif., Wi-minute quad.), where Phillipsastrea and Pleurotomaria were found. The stratigraphic relation of this carbonate rock to volcanic rocks that form the sparse surrounding exposures has not been established.

TIGHTNER FORMATION

The Tightner Formation, named for the Tightner mine, later part of the Sixteen-to-One mine, is about

one-half mile (0.9 km) south of Alleghany and consists mostly of fine-grained greenish schist probably derived from andesitic volcanic rocks (Ferguson and Gannett, 1932, p. 6-7). It contains subordinate schist that is possibly derived from siliceous igneous rocks and some limestone lenses. The Tightner Formation was believed by Ferguson and Gannett (1932, p. 6-8) to be in fault contact with the Blue Canyon Formation (Shoo Fly Formation of this report) on the east and to be overlain unconformably by the Kanaka Formation on the west, although they recognized that the western contact was poorly exposed. No fossils were found in the Tightner Formation.

The Tightner Formation is a mappable unit in the vicinity of Alleghany, but it is unlikely that it can be correlated with confidence over a larger area, owing to the great structural complexity of the belt in which the formation was originally mapped and the lack of distinctive lithologic criteria. The type area of the formation, about one-third mile (0.8 km) southeast of Alleghany, is in a block bounded by faults of large but unknown displacement (pi. 1). The Tightner Formation is similar to many bodies of schistose metavolcanic rock in the western Sierra Nevada associated with less metamorphosed volcanic rocks of both Paleozoic and Mesozoic age. In the absence of fossils, rocks outside of this fault block cannot be correlated with the type Tightner Formation except by lithology.

KANAKA FORMATION

The Kanaka Formation was named by Ferguson and Gannett (1932, p. 7-12) for exposures along Kanaka Creek, about three-quarters mile (1.2 km) south of Alleghany, Sierra County. They divided the formation into a basal conglomerate member, lower slate and greenstone member, chert member, and an upper slate and greenstone member, stating that the Kanaka Formation unconformably overlies the Tightner Formation and is conformably overlain by the Relief Quartzite. No fossils were found in the formation, but a Carboniferous age was assigned on the basis of Lindgren’s earlier interpretation of the age of rocks in that area.

The two slate and greenstone members of the Kanaka Formation are megascopically similar to many other bodies composed of slate and metavolcanic rocks in the region and in this report are mapped as metavolcanic rocks of Paleozoic and Mesozoic age. The chert member is indistinguishable from rocks mapped as the Delhi Formation by Lindgren (1900) and is included with the Calaveras Formation in this report.

The conglomerate member of the Kanaka Formation was not recognized along the three forks of the Yuba River during this investigation, and its outcrop is too﻿PALEOZOIC AND (OR) MESOZOIC ROCKS

15

narrow to show on plate 1; however, it constitutes a distinctive unit from Lafayette Ridge to Oregon Creek. The mode of origin of the rock is uncertain: It is either a tectonic breccia or a greatly sheared conglomeratic mudstone. Although it resembles coarse fragmental rocks in Jurassic strata of the region, it is exposed in an area that is distant from known Jurassic rocks.

According to Ferguson and Gannett (1932, p. 8-9), the texture of the conglomerate member ranges from slate containing scattered pebbles to closely spaced pebbles in a slate matrix. The size of the rock fragments varies widely; the largest fragment observed was 14 feet (4 m) long. The most numerous pebbles are altered pyroxene andesite, and possibly dacite, but pebbles of quartz diorite are also numerous. Less common are pebbles of arkose and quartzite. During the present investigation, blocks of bedded chert were found in the conglomerate member along Kanaka Creek. Possibly the volcanic rock pebbles were derived from the Tightner Formation (Ferguson and Gannett, 1932, p. 9), which is separated from the conglomerate member by thin septa of gabbro and serpentine. The quartzite and arkose pebbles could have been derived from the Shoo Fly Formation and the chert blocks from the Calaveras Formation.

Several possible modes of origin of the conglomerate member—pyroclastic, mudflow, tillite, fanglomerate, or fossil talus slope—were discussed by Ferguson and Gannett (1932, p. 10), but no definite conclusion was reached. The mudflow hypothesis is consistent with the concept that the conglomerate member is a sheared conglomeratic mudstone and cannot be eliminated on the basis of present information. On the other hand, the matrix of the conglomerate, which "though containing small fragments of probably detrital quartz*** consists largely of very fine grained opaque black material” (Ferguson and Gannett, 1932, p. 10), is more typical of flaser rocks found in the region than of the pebbly mudstones and is unlike the matrix of pebbly mudstones found elsewhere in the region. The matrix of the conglomeratic mudstones is not opaque and consists of white mica and silt- to sand-size grains of minerals and rocks.

VOLCANIC ROCKS

Volcanic rocks of Paleozoic age exposed along the northeast border of the area were mapped by Durrell and Proctor (1948, p. 171), who found that these rocks consisted of a lower unit of metarhyolite about 4,000 feet (1,200 m) thick, an 80-300-foot-thick (24^90 m) unit of shale, chert, and mafic tuff, and an exceedingly thick unit of mafic lava and pyroclastic rocks. The lower unit rests unconformably on rocks here included with the Shoo Fly Formation and has a thin basal conglomerate (Durrell and Proctor, 1948, p. 171,175). The thick series of mafic lava and pyroclastic rocks is probably of

Permian age (Durrell and Proctor, 1948, p. 171; Wheeler, 1939, p. 107) and is overlain by the Milton Formation (Turner, 1897).

PALEOZOIC AND (OR) MESOZOIC ROCKS

VOLCANIC AND SEDIMENTARY ROCKS

Volcanic and sedimentary rocks constitute a unit mapped in the southern part of the area; in the Colfax area it forms outcrops too small to map separately. It consists largely of mafic or intermediate volcanic rocks but is distinguished from other map units because conglomerate, carbonate rocks, and chert are interbed-ded with the volcanic rocks and because fossils older than those found elsewhere in the area were collected from a limestone body in the unit. The unit includes some of the rocks that were mapped by Lindgren (1894, 1900) and by Lindgren and Turner (1894) as diabase, Calaveras Formation, and Clipper Gap Formation.

This unit crops out in the south-central part of the map area in the same general area as the Cosumnes-type rocks. The volcanic rocks in this unit consist mostly of breccia but include subordinate pillow lava and tuff. Bedding is obscure in the coarse volcanic breccia along the North and Middle Forks of the American River, and farther south most of the volcanic rocks are schistose. Coarse-crystalline carbonate rock, partly limestone, forms lenses in the volcanic rocks in the vicinity of Lake Clementine (North Fork Reservoir on some maps). The largest of these lenses, more than 1 mile (1.6 km) long and as much as 250 feet (710 m) wide, crosses the Middle Fork of the American River about 1.8 miles (2.4 km) upstream from the State Highway 49 bridge. Part of a carbonate rock lens, near where the south line of sec. 10,

T.	13 N., R. 9 E., crosses the North Fork of the American River, is replaced by chert. Thin-bedded chert is interlayed with the volcanic rocks about 200 feet (60 m) upstream from the massive chert near the Colfax railroad station and along Interstate Highway 80. Thin-bedded chert is interbedded with slate, graywacke, and tuff within the dominantly volcanic section at several places between the dam at Lake Clementine and the juncture of the Middle and North Forks of the American River.

The west boundary of the volcanic and sedimentary rocks is a fault zone, and the east boundary is faulted in places. Moderately dipping volcanic rocks with interbedded chert, believed to be part of this unit, are unconformably overlain by conglomerate of Cosumnes type in a cutbank at the Colfax railroad station. Truncated beds below the contact show an angular unconformity of a few degrees. Along the North Fork of the American River, slate and graywacke of Cosumnes type is in fault contact with the undivided volcanic and sedimentary rocks. Along Interstate Highway 80﻿16

WESTERN SIERRA NEVADA MET AMORPHIC BELT, CALIFORNIA

between Clipper Gap and Applegate, exposures of rocks typical of the Cosumnes alternate with exposures of volcanic rocks with interbedded chert. Low-dip angles that characterize these two units at this locality suggest that the contact between them is folded so as to cause an irregular pattern very difficult to trace on the deeply weathered and rolling upland surface.

Tabulate corals collected from the limestone quarry south of the Middle Fork of the American River in sec. 6, T. 12 N., R. 9 E., are of probable Devonian age, according to C. W. Merriam (oral commun., 1962). Bryozoa collected from the same locality were identified by Helen Duncan (written commun., 1967), who believes that these also suggest a Devonian age. Exposures at the quarry suggest that this limestone body is interbedded with the adjacent volcanic rocks, but owing to the meager information on the internal structure and stratigraphy of this map unit, it cannot be assumed that all rocks in the unit are of the same age. The unit is therefore considered to be of Paleozoic and Mesozoic(?) age.

EPICLASTIC ROCKS

Epiclastic rocks near the site of Las Plumas, now flooded by Lake Oroville, in the northwest corner of the area (pi. 1) consist mostly of dark-gray phyllite but contain some graywacke, volcanic rock, and conglomerate. Phyllitic conglomerate exposed in railroad cuts northwest of Las Plumas consists largely of pebbles of light- to dark-gray slate and dark-gray chert in a slate matrix with sparse granules of dark-gray quartz. A block of coral-bearing carbonate rock, 10 by 4 feet (3 by 1.2 m) in size, surrounded by sheared phyllite is exposed in the bank of Grizzly Creek at the west boundary of the Las Plumas 71/2-minute quadrangle, about 3,500 feet (1,065 m) S. 80° W. of the Las Plumas powerhouse. Because the slate is sheared, it is uncertain whether the carbonate block was emplaced by faulting or by slumping, as were some of the blocks in the Cosumnes-type rocks, but it is unlikely that fossils in the block can be used confidently to date the surrounding slate. Blocks of fusulinid-bearing limestone occur on the west wall of Spring Valley Gulch at the 900-foot (270 m) elevation, the high-water mark of Lake Oroville. These blocks appear to be in fault contact with adjacent slate.

METAVOLCANIC ROCKS

Metavolcanic rocks occur in the central part of the map area and are spatially closely associated with the Calaveras Formation. They were mapped as amphibolite by Lindgren and Turner (1894, 1895), by Turner (1897), and by Lindgren (1900) and also as diabase and porphyrite by Lindgren (1900). Ferguson and Gannett (1932, p. 6-7) applied the name Tightner Formation to

schistose metavolcanic rocks near Alleghany (pi. 1). Most metavolcanic rocks appear in the field to be basaltic or andesitic, but felsic volcanic rocks constitute the western part of the sheared and metamorphosed body of metavolcanic rocks along the North Fork of the American River south of Dutch Flat. The abundance of quartz in contorted banded schistose metavolcanic rocks assigned by Ferguson and Gannett (1932, p. 7) to the Tightner Formation was interpreted by them to suggest felsic composition.

Bedded metavolcanic rocks along the North Yuba River east of Indian Valley consist largely of aphanitic dark-gray rocks that form massive beds 1-2 feet (0.3-0.6 m) thick. Interbedded with these are sparse beds of sand-size tuff. The massive aphanitic rocks superficially resemble chert but have a duller luster, and the beds are much thicker than normal for chert. Bedded metavolcanic rocks in the western part of the Middle Yuba River west of the mouth of Indian Creek consist largely of pyroclastic rocks, but one layer of lava shows suggestions of pillow structure. Chert is interbedded with the pyroclastic rocks near the pluton there. Massive metavolcanic rocks, some having the appearance of gabbro with grain size ranging from about 1-2 mm, are associated with the schistose metavolcanic rocks along the Middle Yuba River near Orleans Flat, and massive metavolcanic rocks constitute most of the eastern part of the body exposed along the North Fork of the American River.

Massive and pillow lavas occur near the east and west ends of the segment of Slate Creek that is marked by structure symbols (pi. 1) and on the Middle Fork of the Feather River near a large serpentine body. Distorted pillow structure is retained in schistose metavolcanic rocks at the State Highway 49 bridge across the North Yuba River west of Indian Valley.

Few clues are to be found regarding the age of the metavolcanic rocks, but some bodies may be temporally correlative with the late Paleozoic Calaveras Formation or, in the southern part of the area, with the Silurian Shoo Fly Formation. Preservation of original structures in some metavolcanic rocks near Slate Creek in the northern part of the map area (pi. 1), as well as the association with epiclastic rocks that are indistinguishable from Jurassic strata, suggests that at least part of these volcanic rocks may be Jurassic. If so, the volcanic rocks, as well as the associated sedimentary rocks, probably rest unconformably on the more deformed Calaveras Formation. In the absence of additional data, the metavolcanic rocks are tentatively assigned a Paleozoic or Mesozoic age.

MESOZOIC ROCKS

Epiclastic and volcanic rocks of Mesozoic and proba-﻿MESOZOIC ROCKS

17

ble Mesozoic age underlie wide belts east and west of the belt of older rocks marked by the Shoo Fly Formation. They form smaller bodies that are associated with the Calaveras Formation in the central and northern parts of the map area. Probably none of these metamorphic rocks is younger than Cretaceous, for most map units are intruded by granitic rocks and no granitic rocks younger than Cretaceous have been recognized in the Sierra Nevada. Sparse Late Cretaceous sedimentary rocks in the region, not differentiated in this report, are neither folded nor metamorphosed (Lindgren, 1894; Creely, 1965, p. 34-35).

Fossils are generally sparse in the Mesozoic rocks, and they have been found in but a few map units. Epiclastic rocks here considered to be of Mesozoic age are lithologically similar to dated Jurassic rocks and resemble only the slate member of the Shoo Fly Formation among the Paleozoic strata. Some volcanic rocks in the northeastern part of the area (pi. 1), here considered to be of Mesozoic age, are possibly deformed outliers of the Paleozoic volcanic rocks that occur near the northeast boundary. Available structural and faunal evidence indicates that the Mesozoic rocks of the eastern belt are, in general, successively younger from west to east, but strata in the western belt are faulted and repeated by folds. The Triassic(?) rocks, comprising a basal chert breccia and an overlying limestone unit, are suggestive of miogeosynclinal deposition, whereas the Jurassic strata are eugeosynclinal deposits of metavolcanic rocks, silty slate, graywacke, and conglomeratic mudstone.

Mesozoic strata in the eastern part of the area are broadly divisible into eastern and western outcrop belts of epiclastic rocks separated by an intermediate belt of volcanic rocks. Turner (1894b) assigned the name Sailor Canyon Formation to the western belt of epiclastic rocks (pi. 1) and the name Milton Formation to strata composed chiefly of tuff and lapilli tuff exposed in the vicinity of what is now Milton Reservoir. However, he excluded massive volcanic breccia that is interbedded with the Milton. Lindgren (1897, 1900) included both bands of epiclastic rocks with the Sailor Canyon Formation and did not discuss the stratigraphic significance of the intervening volcanic rocks. Clark (1930, p. 8, 19-20, 28, fig. 6), who viewed the two bands of epiclastic rocks as opposite limbs of a syncline, included the volcanic rocks as well as both bands of epiclastic rocks in the Milton Formation. In this report, the name Sailor Canyon Formation is restricted to the western belt of epiclastic rocks, in accordance with the original definition. The name Milton Formation is extended to include the interbedded massive volcanic breccia that Turner mapped separately, as well as volcanic rocks east of the Sailor Canyon Formation and

along the regional strike of the type locality of the Milton Formation. The eastern belt of Mesozoic epiclastic rocks is herein discussed under the informal term "epiclastic rocks.”

Taliaferro (1943, fig. 2) correlated the Gopher Ridge Volcanics of this report with the Logtown Ridge Formation. Turner (1894a) and Taliaferro (1943, fig. 2) included both the Salt Spring Slate and the epiclastic rocks east of the Logtown Ridge Formation with the Mariposa Formation of Late Jurassic (upper Oxfordian and lower Kimmeridgian) age. A sparse fauna in the Salt Spring Slate (Imlay, 1961, table 2, loc. 8) suggests that its age is about the same as that of the type Mariposa Formation, but no fossils have been recovered from the unnamed epiclastic rocks that overlie the Logtown Ridge Formation. Because the fossil record is inadequate for precise correlation, the author prefers to use separate stratigraphic nomenclature for the two fault blocks.

Rocks of Jurassic and probable Jurassic age west of the Shoo Fly are more folded than those in the eastern belt, and stratigraphic continuity is interrupted by faults of large but unknown displacement. Stratigraphy and correlation problems are best illustrated near the south boundary of the area where stratigraphic sequences in two different fault blocks can be compared. South of Folsom Reservoir (pi. 1) the Gopher Ridge Volcanics of Jurassic (probable Late Jurassic) age, and the Salt Spring Slate and overlapping Copper Hill Volcanics, both of Late Jurassic age, constitute a sequence of folded concordant formations (Clark, 1964, p. 27-31, pis. 2, 8) that are more extensively exposed south of the area of this report. Farther east and separated from the above area by an intervening fault block, a similar sequence consists of Cosumnes-type rocks of Middle!?) and Late Jurassic (Callovian) age, the Logtown Ridge Formation of Late Jurassic (Callovian to upper Oxfordian or lower Kimmeridgian) age and an unnamed epiclastic formation of Late Jurassic (probably Kimmeridgian) age.

Formations in the western fault block, particularly the Copper Hill Volcanics, possibly constitute parts of unnamed map units elsewhere in the area, but they have been identified in so little of the-area that further description here is unwarranted.

TRIASSIC(?) ROCKS

Rocks of Triassic(?) age were recognized only near the North Fork of the American River immediately east of the Shoo Fly Formation (pi. 1) where they include a basal chert breccia and an overlying limestone. The limestone is possibly equivalent to the Hosselkus Limestone of Late Triassic age near Taylorsville and Redding (McMath, 1966). Although the breccia and﻿18

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

limestone were included by Lindgren (1900) with the Paleozoic rocks to the west, he was the first to recognize the existence of an unconformity in this vicinity. The lower of two units questionably assigned to the Triassic is medium to very coarse poorly sorted chert breccia having a thickness of 75 feet (23 m) or more. Chert and quartzose slate fragments similar to the rocks in the Shoo Fly Formation west of the unconformity are the most abundant rocks in the breccia; however, fragments of fine-grained dioritic or quartz-monzonitic rocks are common near Little Granite Creek, and sparse mica-schist pebbles occur on the north side of the main river canyon. Fragments of thin-bedded dark-gray slate and fine-grained graywacke or silicic tuff derived from the Shoo Fly Formation are common locally. In most places the largest fragments in the breccia are about 4 inches (10 cm) long, but near Little Granite Creek some are as much as 20 inches (50 cm) long. Near the contact on the divide between Big Granite Creek and the North Fork of the American River are outcrops of Shoo Fly Formation as much as 20 feet (6 m) long and 5 feet (1.5 m) wide that are surrounded by chert breccia; such an outcrop pattern might result either from deposition of the breccia on a very irregular erosion surface or from incorporation of detached blocks of the Shoo Fly Formation in the breccia.

The limestone that overlies the chert breccia is about 400 feet (120 m) thick on the crest of the divide between the North Fork of the American River and Big Granite Creek. It is absent in New York Canyon and is absent or concealed on the south side of the main river canyon. The lower part of the limestone unit consists of alternating layers of thin-bedded argillaceous gray limestone that weathers very light gray. Well-rounded granules or angular fragments of chert characterize some of these beds. The middle part consists of less argillaceous cliff-forming limestone, and the upper part is thinly interbedded light-gray limestone and light-greenish-gray very fine grained pyritic sandstone probably derived from silicic tuff.

The chert breccia overlies the Shoo Fly Formation with pronounced angular unconformity, and owing to pre-Triassic(?) folding of the Shoo Fly Formation, the angle between bedding in the Shoo Fly and that in the Mesozoic rocks varies from near 0° to near 90°. At the unconformity the surface of the Shoo Fly shows a relief of several feet; the contact alternately follows bedding and joints in the Shoo Fly Formation. North of the North Fork of the American River, the chert breccia is conformably overlain by limestone of Late Triassic(?) age. In New York Canyon it is overlain with possible erosional, but not angular, unconformity by the Sailor Canyon Formation. Although no fossils were found in

the chert breccia, it is considered to be of Triassic(?) age.

Evidence for the age of the limestone was stated by Norman Silberling (in Clark and others, 1962, p. B18) as follows:

A Late Triassic(?) age for the limestone is based mainly on the occurrence *** (USGS Mes. loc Ml 167) of numerous spherical objects with the surficial and internal structure ofHeterastridium, a supposed hydrozoan coelenterate that is widely distributed in deposits of Norian (late Late Triassic) age. However, in view of the doubtful biologic affinities and unknown evolutionary history of this organism, the age must be considered provisional. A post-Paleozoic age for the limestone is corroborated by the presence of poorly preserved scleractinian corals, large cidarid echinoid spines, and Pentacrinus-like crinoid columnals with petaloid crenulations on the articulating surfaces.

Lindgren (1900) reported finding Lithostrotion, Avicu-lopecten, Murchisonia, crinoid stems, and lamelli-branchs where, according to his field notes, the limestone crosses a trail on the southeast side of Big Granite Creek, but similar material was not found during the present investigation.

JURASSIC ROCKS

SAILOR CANYON FORMATION

The Sailor Canyon Formation, named by Turner (1894b, p. 232) for exposures on a tributary to the North Fork of the American River, is mostly graywacke, silty slate, and tuff. Its maximum thickness is at least 10,000 feet (3,000 m). The lowest part of the formation is greenish-gray-weathering sparsely bedded andesitic tuff about 500-700 feet (150-210 m) thick. Its texture ranges from very fine grained tuff to lapilli-tuff. The tuff is overlain by silty, locally pyritic, or calcareous slate about 1,000 feet (300 m) thick that extends eastward to the mouth of New York Canyon. Some conglomerate and graywacke are interbedded with the slate; pebbles in some conglomerate beds are restricted to carbonate rocks and chert, but others also contain pebbles of vein quartz and amygdaloidal volcanic rocks.

The most abundant rocks from the mouth of New York Canyon to the east side of Sailor Canyon are graywacke and silty slate, but tuff occurs throughout; the frequency of pyroclastic beds increases markedly near the top of the formation. Current-ripple bedding and graded bedding are common in the graywacke. In thin section, sand grains in the graywacke are seen to be mostly plagioclase and mottled untwinned feldspar, but quartz is common; some beds contain grains of microcrystalline volcanic rocks, granoblastic chert, and quartzite. Poorly sorted calcarenite or calcareous graywacke beds at the mouth of Sailor Canyon are less than 1 foot (0.3 m) thick. Detrital carbonate grains and recrystallized carbonate constitute most of these beds, but other rocks and minerals also occur.﻿MESOZOIC ROCKS

19

Where the base of the Sailor Canyon Formation is well exposed in New York Canyon, its lower tuff unit rests on Triassic(?) chert breccia along an irregular surface having a local relief of about 10 feet (3 m). The tuff here contains a 4-foot (1.2 m) layer of chert breccia about 20 feet (6 m) above its base. The absence of Triassic(?) limestone and the relief of the upper surface of the breccia are interpreted as evidence of an erosional unconformity at the base of the Sailor Canyon Formation. The available evidence indicates that the Sailor Canyon Formation is structurally concordant with the Triassic(?) rocks, and the paleontologic record indicates but a very short time break at the unconformity.

The upper part of the Sailor Canyon Formation grades into, or intertongues with, the overlying Milton Formation through a stratigraphic interval about 1,600 feet (490 m) thick. The transitional zone, here included with the Sailor Canyon Formation, consists of interbed-ded conglomerate and volcanic rocks. The top of the Sailor Canyon Formation is drawn at the base of a thick layer of massive dark-gray volcanic breccia with abundant needlelike amphibole crystals, which is exposed on the north canyon wall.

The Sailor Canyon Formation is of Early and Middle Jurassic age. Hyatt (1894, p. 396-398) first identified Monotis semiplicata, Monotis symmetrica, Daonella? subjecta, Daonella boechiformis, Daonella cardinoides, Gryphaea, and ammonites including Peronoceras? americanum (an undescribed species). He believed that the presence of species of Daonella would ordinarily be regarded as evidence of a Triassic age, except for the fact that they extended into the ammonite bed which he dated as Early Jurassic (Lias) (Hyatt, 1894, p. 397). Lindgren (1900, p. 2) assigned the Sailor Canyon Formation to the Juratrias Period. Smith (1927) held that the Monotis species listed by Hyatt were synonyms for Pseudomonotis and that the Sailor Canyon Formation was therefore of Late Triassic (Noric) age. Smith’s age assignment was accepted by K. B. Ketner (in McKee and others, 1959, p. 6-7) for the lowermost part of the Sailor Canyon.

C. H. Crickmay (in Clark, 1930, p. 49) studied collections made by Clark at three localities near the North Fork of the American River. Among fossils collected in Sailor Canyon above the Trinidad mine (probably the Sterrett mine of earlier reports), Crickmay determined two species of Arniotites, "Tubel-lites” sp. (=Gemmeltaroceras), and a hildoceratid. He thought that the first two indicated an early Lias date but that the third indicated middle Lias. Arniotites sp. and "Tubellites” sp. were identified also in a collection from the divide Between Big Granite Creek and the North Fork of the American River. In a collection from

near the Placer Queen mine in the upper part of Wildcat Canyon, Crickmay identified sphaerocehatinid ammonites, which he believed to indicate a much younger age than fossils at the Trinidad mine locality. Similar ammonites near that mine were also mentioned by Clark (1930). In addition, Crickmay (1933, p. 52) redescribed and illustrated Monotis semiplicata Hyatt and Monotis symmetrica Hyatt, placed them in the genus Entolium, and dated them as "Lower Jurassic, Deroceratan.” Stratigraphically, these are the lowest known fossils in the Sailor Canyon Formation. Taliaferro (1942, p. 100) stated that Upper Triassic fossils were found at or near the base of the Sailor Canyon Formation along the North Fork of the American River, Lower Jurassic fossils occur 2,500 feet (750 m) above the base, and Middle Jurassic fossils occur 9,500 feet (2,900 m) above the base.

More recently, all U.S. Geological Survey fossil collections from the Sailor Canyon Formation were studied by Imlay (1968, p. C7, C8, C12-C17; Clark and others, 1962, p. B19), who concluded that the formation reprsents most of the Early Jurassic and at least the early Middle Jurassic. The evidence consists of the late Sinemurian ammonite Crucilobiceras about 1,000 feet (300 m) above the base of the formation, the late Pliensbachian ammonites A rieticeras and Reynesoceras about 2,000 feet (600 m) above the base, and the early Bajocian ammonite Tmetoceras from 9,000 to 10,000 feet (2,700 to 3,000 m) above the base. The unverified report of sphaeroceratid ammonites near the Placer Queen mine suggests that the upper part of the formation may be as young as middle or late Bajocian.

Several stratigraphically useful pelecypods collected in the Sailor Canyon Formation include Entolium? semiplicatum (Hyatt), associated with the late Sinemurian ammonite Crucilobiceras, and Lupherella boechiformis, associated with the late Pleinsbachian ammonites Arieticeras and Reynesoceras. In addition, Bositra buchii (Roemer) occurs with Tmetoceras of early Bajocian age, but its total range is late Toarcian to Kimmeridgian. Of these pelecypods Entolium? semiplicatum (Hyatt) occurs in Nevada, eastern Oregon, and southern Alaska in beds of the same age, and Lupherella boechiformis (Hyatt) occurs in eastern Oregon associated with many ammonites of late Pliensbachian age (Imlay, 1967, p. B9).

MILTON FORMATION

The Milton Formation was named by Turner (1894b, p. 232-234) for exposures near an old stage station at about the present site of the dam for the Milton Reservoir on the Middle Fork of the Yuba River. The Milton consists mostly of andesitic pyroclastic rocks;﻿20

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

subordinate rocks are felsite tuff, calcarenite, conglomerate, mudflow breccia, and dark-gray slate or very fine grained tuff. Graded beds are few in the Milton Formation, but current-ripple bedding, small cut-and-fill structures, and load casts mark some tuff beds. Along Haypress Creek contact metamorphism has converted slate or fine-grained tuff to hornfels and destroyed original textures and structures of most volcanic rocks east of the pillow lava. Following Turner (1896, p. 624), isolated exposures of coarse-crystalline limestone along Pass Creek are included arbitrarily with the Milton Formation, although stratigraphic relations of the limestone are uncertain. The Milton Formation exposed along the North Yuba River is at least 10,000 feet (3,000 m) thick if not folded in concealed areas. Along the North Fork of the American River, the Milton is apprently equally as thick, but this is uncertain because contact metamorphism has obscured bedding in the eastern part of the formation. Owing to more moderate and variable dips along the Middle Yuba River, the exposed part there is probably less than 5,000 feet (1,500 m) thick. Near the North Fork of the American River, the western part of the Milton is coarse mostly thick-bedded mafic or intermediate volcanic breccia. The eastern part, owing to contact metamorphism, is mostly massive fine-grained rock of dioritic appearance.

Thin- to thick-bedded tuff of probably andesitic composition constitutes most of the Milton Formation near the Middle Yuba River and much of the formation along Haypress Creek. Massive amygdaloidal lava occurs near the mouth of Haypress Creek, and at Loves Falls the North Yuba River cuts through a thick massive layer of pyroclastic or flow breccia. Massive felsite containing quartz phenocrysts occurs in roadcuts of State Highway 49 at the west boundary of sec. 27, T. 20 N., R. 12 E., and at the mouth of Haypress Creek. Very fine grained dark-gray slate with some interbed-ded fine- to medium-grained tuff and chert or quartzose tuff extends about 3V2 miles (5.6 km) north from Wild Plum Campground.

Along the Middle Y uba River west of the mouth of the Milton-Bowman tunnel, bedded felsite lapilli-tuff having interbedded layers of dark-gray slate and chert as much as IY2 feet (0.5 m) thick is overlain by poorly sorted intraformational conglomeratic mudstone about 50 feet (15 m) thick with chert fragments in a matrix of felsite tuff. The fragments range from small massive pebbles to internally thin-bedded blocks more than 8 feet long and 2 feet thick (2.4 m and 0.6 m). Obscure layering in the conglomeratic mudstone is marked by differences in spacing of fragments and by parallel arrangement of elongate or tabular fragments. Con-stitutents of the breccia were apparently derived from

tuff and chert beds that occur within 40 feet (12 m) stratigraphically below the breccia.

Along the road about 500 feet (150 m) west of the Milton Reservoir dam, conglomerate layers less than 10 feet (3 m) thick are interbedded with tuff. Most of the pebbles are fine-grained dioritic and gabbroic rocks; less common pebbles are chert, mafic volcanic rocks, and biotite schist.

Medium-grained dark-gray obscurely bedded calcarenite is exposed along the Middle Yuba River near the center of sec. 18, T. 19 N., R. 13 E. The calcarenite contains pebbles of mafic volcanic rocks, and under the microscope sand-size grains of plagioclase, untwinned feldspar, and mafic minerals are visible. Carbonate rocks along Pass Creek appear to be much less contaminated by noncarbonate detritus.

Along the Middle and North Yuba Rivers, stratigraphic relations between the Milton and Shoo Fly' Formations to the west are obscured by shear zones marking faults of probable large displacement. On the North Yuba, this contact is tentatively drawn at a shear zone that marks the east limit of chert in this vicinity. Sheared mafic or andesitic volcanic rocks occur both east and west of the contact as drawn, but such rocks are known to occur in both the Shoo Fly and Milton Formations. On the Middle Yuba River, this contact is drawn at a narrow serpentine body at the west limit of unsheared rocks of the Milton Formation. Near the North Fork of the American River, the Milton grades into or intertongues with the underlying Sailor Canyon Formation. Turner (1894b) considered the Milton Formation to be younger than the Sailor Canyon Formation and older than the Mariposa Formation, that is, within the range of late Middle to early Late Jurassic age. This interpretation is consistent with available structural and stratigraphic information. Along all three rivers the Milton is truncated on the east by granitic intrusive rocks.

AMADOR GROUP OF TALIAFERRO (1942, 1943)

The Amador Group was named by Taliaferro (1942, p. 89-90; 1943, p. 282-284); he divided the group into the Cosumnes and overlying Logtown Ridge Formations on the basis of exposures along the Cosumnes River, the north boundary of Amador County. His original definition was slightly modified by Clark (1964, p. 17) as the result of reexamination of its type locality. Both Taliaferro and Clark described the Cosumnes Formation as consisting predominantly of sedimentary rocks and the Logtown Ridge Formation as consisting predominantly of pyroclastic rocks with associated volcanic breccia and pillow lava.

Recent detailed mapping in Amador County, including the type locality of the Amador Group (Sharp and﻿MESOZOIC ROCKS

21

Duffield, 1973; Duffield and Sharp, 1975), has resulted in the following major revisions within the Amador Group:

1.	The basal contact of the Logtown Ridge Formation is

located 2,000 feet (600 m) farther west than originally designated.

2.	This contact is a fault, and thus the Logtown Ridge

Formation is not conformable with the Cosumnes Formation as previously described.

3.	Most strata originally defined and mapped as the

Cosumnes Formation are part of a diverse assemblage of tectonically intermixed rocks—a melange—and thus the Cosumnes is not a valid formational rock-stratigraphic unit in Amador County.

4.	The names Consumnes Formation and Amador

Group are both inappropriate in their type areas and thus are abandoned.

The decision of Sharp and Duffield to abandon the Cosumnes Formation and Amador Group is accepted in the present report, although a belt of rocks similar to the Cosumnes Formation as originally defined has been mapped northward from its original type locality on the Cosumnes River into the southern part of the area of this report (pi. 1). To provide continuity between the present report and the earlier report on the south half of the foothill belt (Clark, 1964) and still recognize the recent contributions of Duffield and Sharp, these rocks are here referred to informally as Cosumnes-type rocks, in much the same way that Duffield and Sharp (1975) describe some rocks of the melange discussed by them as having Cosumnes affinities.

Cosumnes-type Rocks

Cosumnes-type rocks include strata along the regional strike of the type locality of Taliaferro’s (1943) Cosumnes Formation as far northward as the Bear River (pi. 1). Much of the western part of the belt so included was assigned by Lindgren and Turner (1894) to the Calaveras Formation and a small part northeast of Applegate was assigned by Lindgren (1900) to the Clipper Gap Formation. Most of the rocks north of the North Fork of the American River that are here included with Cosumnes-type rocks were assigned to the Mariposa Formation by Lindgren (1900) and Chandra (1961). They were identified as slate and tuff of the Colfax Formation by Smith (1910, chart opposite p. 217). In some places between the South and Middle Forks of the American River, the east boundary of the unit is drawn arbitrarily, and much of the west boundary is also arbitrary owing to scarcity of exposures. The unit is at least 4,000 feet (1,200 m) thick in the map area.

Cosumnes-type rocks include dark-gray silty slate, gravelly conglomerate, conglomeratic mudstone, graywacke, and a small proportion of volcanic rocks. Major components of the graywacke and conglomerate are angular fragments of light- to dark-gray chert, volcanic rocks, and quartz. Minor constituents of the graywacke identified in thin sections are detrital grains of quartz-rich graywacke having sparse plagioclase probably derived from the Shoo Fly Formation and, from other sources, quartzite distinguished by pronounced undulatory extinction and deeply sutured contacts between its component grains, quartz-mica schist, and microcrystalline graphite-bearing quartz phyllite.

Current-bedded conglomerate and conglomeratic mudstone are sparse along the South Fork of the American River but are common farther north. Conglomeratic mudstone containing blocks of carbonate rock occurs along the Middle Fork of the American River from Kennebeck Bar to Poverty Bar, in Bunch Canyon, along the river near the south boundary of sec. 36, T. 15 N., R. 9 E., and along Interstate Highway 80. A conglomeratic mudstone about 1,000 feet (300 m) north of the south boundary of sec. 36, T. 15 N., R. 9 E., contains a block of deformed thin-bedded chert about 15 feet (4.5 m) wide and 30 feet (9 m) long. Most pebbles and boulders in the conglomeratic mudstone are of thin-bedded chert. Pebbly mudstone about 50 feet (15 m) thick, exposed 0.7 mile (1.1 km) northeast of the mouth of Codfish Creek, truncates bedding in the underlying slate and graywacke. Enclosed in the mudstone are blocks of interbedded slate and graywacke similar to strata underlying the pebbly mudstone. Other pebbly mudstones in that vicinity include contorted masses of slate and graywacke.

Few contacts of Cosumnes-type rocks with other units are exposed in the map area, and of these, several contacts are with units that are not well fixed stratigraphically. Thick conglomerate in the basal part of the Cosumnes-type rocks suggests but does not prove that the basal contact is an unconformity. In cut banks east and west of the railroad station in Colfax, coarse breccia containing abundarlt fragments of volcanic rocks and some chert fragments, here included with Cosumnes-type rocks, unconformably overlies volcanic rocks having some interbedded chert. Truncation of the chert below the contact at the south end of the cut east of the railroad station suggests an angular unconformity of a few degrees, but the age of the rocks beneath the unconformity is uncertain.

Cosumnes-type rocks contain rocks of early Late Jurassic (Callovian) age, which were originally considered younger. Hyatt (1894, p. 424-425, 427; in﻿22

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

Lindgren, 1900, p. 3) identified Perisphinctes colfaxi Gabb collected from a railroad cut 1 mile (1.6 km) west of Colfax and Olcostephanus lindgreni Hyatt occurring about IV2 miles (2.4 km) south-southwest of Colfax and concluded that they indicated a Late Jurassic (Tithon-ian) age. Smith (1910, chart facing p. 217) mentioned the occurrence of Perisphinctes colfaxi Gabb in these strata, which he named the Colfax Formation, and believed them to be of Late Jurassic age and younger than the Mariposa Formation. Crickmay (1933, p. 57) identified Olcostephanus lindgreni Hyatt as Galilaeiceras lindgreni and gave its age as early Late Jurassic (Callovian). Imlay (1961, p. D6-D7) listed Ammonites colfaxi Gabb, Kepplerites lorinclarki Imlay, and K. (Gowericeras) lindgreni (Hyatt) from the Colfax Formation of Smith (1910) as Callovian ammonites. A fossil identified by Imlay (1961, p. D7-D8, table 3) as Perisphinctes (Dichotomosphinctes) mulbachi Hyatt of possible early Oxfordian but probably late Oxfordian (Late Jurassic) age is reported to have been found near Greenwood (pi. 1). A late Oxfordian age is more in accord with the age of the Mariposa Formation south of the area of this report than with Cosumnes-type rocks at Greenwood, but as the geologic structure in this area, as well as the name of the collector and precise locality of the fossil, is uncertain, the age is questionable.

Logtown Ridge Formation

In its type locality immediately west of the Huse Bridge on State Highway 49 over the Cosumnes River, the Logtown Ridge Formation consists largely of pyroclastic rocks, ranging from very fine grained tuff to very coarse volcanic breccia, but contains some pillow lava. Within the area covered by this report, it was examined only along the South Fork of the American River, where it consists of pyroclastic rocks ranging in texture from very fine grained tuff to volcanic breccia. The pyroclastic rocks consist largely of fragments of mafic or intermediate volcanic rocks, but some breccia also contains fragments of slate and felsic volcanic rocks.

As mapped by Lindgren and Turner (1894), rocks here assigned to the Logtown Ridge Formation are continuously exposed from its type locality, 6 miles (9.6 km) south of the boundary of the present study area, to a point southwest of Placerville where they are truncated by a felsic intrusion (pi. 1). Similar pyroclastic rocks bordering the east side of Cosumnes-type rocks from a point south of Georgetown northward to a point near Cape Horn (pi. 1) probably belong to the Logtown Ridge Formation; however, no paleontologic confirmation was found, and thus they have been mapped simply as volcanic rocks of Jurassic age.

The Logtown Ridge Formation is of early Late

Jurassic (Callovian to late Oxfordian or early Kim-meridgian) age (Imlay, 1961, p. D6) on the basis of the presence of Pseudocadoceras in its lower 600 feet (180 m) and ofIdoceras aff. I. planula (Heyl) in its upper part.

MONTE DE ORO FORMATION

The Monte de Oro Formation was named by Turner (1896, p. 548) for a conglomerate-bearing slate exposed in sec. 33, T. 20 N., R. 4 E., along the road immediately south of Monte de Oro, a point on the southeast end of North Table Mountain about 3 miles (4.8 km) north-northeast of Oroville where it occupies a faulted syncline (pi. 1). Silty slate, part of which contains abundant plant fossils, constitutes most of the formation, but graywacke and poorly sorted conglomerate are interbedded with the slate. On the west side of the syncline, this sequence is underlain conformably by a 200-foot-thick (60 m) section of littoral sandstone and conglomerate, partly crossbedded, that contains-pebbles of vein quartz, carbonate rocks, and volcanic rocks and is much better sorted than the overlying silty beds to the east. Although the marked contrast between the littoral and deeper water facies suggests a hiatus at their contact, the littoral beds are here included in the Monte de Oro Formation following Taliaferro (1942, p. 92), who interpreted them as evidence of the west margin of a Jurassic sea. A more detailed description of the formation is given by Creeley (1965, p. 24-28).

Although no depositional contact between the epi-clastic rocks of the Monte de Oro Formation and the underlying volcanic rocks was found, the synclinal structure of the formation and directions of tops of beds indicate that the Monte de Oro Formation overlies the adjacent volcanic rocks. There is no evidence to suggest that offset along faults that bound the Monte de Oro Formation is sufficient to invert the stratigraphic sequence. Deformation of the Monte de Oro is similar to that of other pre-Portlandian rocks of the western Sierra and is dissimilar to the moderately dipping and less metamorphosed strata of the latest Jurassic Knoxville Formation on the west side of the Sacramento Valley. There the Knoxville unconformably overlies metamorphic and intrusive rocks that appear to be comparable in their age and geologic history to the pre-Knoxville rocks of the western Sierra Nevada.

Both flora and fauna of the Monte de Oro Formation suggest a Late Jurassic age, although agreement between the two is not precise. Results of paleontologic studies of the Monte de Oro Formation prior to 1942 are summarized by Taliaferro (1942, p. 91). More recently, Fry (1964, p. 64A) concluded that its flora indicated an age ranging from late Oxfordian to and including Portlandian, on the basis of Macrotaeniopteris, Baiera, Ctenis, Ctenophyllum,Pagiophyllum, and Taeniopteras.﻿MESOZOIC ROCKS

23

However, the plant fossils lack an epidermis, and therefore specific and generic determinations are uncertain, according to Jack Wolfe of the U.S. Geological Survey (oral commun., 1968). Imlay (1961, p. D8-D9) concluded that the fauna is of Late Jurassic (late Oxfordian to early Kimmeridgian) age, on the basis of an ammonite similar to Perisphinctes (.Dichotomosphinctes) elisabethaeformis Burckhardt and two crushed specimens of Buchia that probably belong to B. concentrica Sowerby. Imlay (1961, p. D9) stated that the presence of Buchia in the Monte de Oro Formation indicates that its age does not extend to Portlandian. Pachysphinctes, indicative of the Kimmeridgian Stage (Imlay, written commun., 1965), was found 150 feet (45 m) below the surface in an excavation for a highway bridge in the NW'A sec. 5, T. 19N., R. 4 E. (See topographic map of Oroville quadrangle.)

UNNAMED EPICLASTIC ROCKS

Unnamed epiclastic rocks presumably of Jurassic age occur chiefly near the east side, in the central part, and near the northwest corner of the map area (pi. 1). Epiclastic rocks near the east boundary of the area were indicated by Lindgren (1897) to be of Juratrias(?) age. Those in the south-central part of the area were included by Lindgren and Turner (1894) with the Mariposa and Calaveras Formations, and those in the central part of the area were included by Lindgren (1900) with the Cape Horn and Delhi Formations. Epiclastic rocks in the northwestern part of the area were mapped by Turner (1898) and Creeley (1965) as the Calaveras Formation. A narrow belt of sheared rocks that extends northward along a fault zone from La Mar Flat, north of Lake Combie on the Bear River, is here included arbitrarily with this map unit. Correlation of these rocks with the Calaveras Formation, as indicated by Lindgren and Turner (1895), is unlikely in view of the narrowness of the belt and its isolation from known Paleozoic rocks. Where observed near the Bear River during this investigation, the unit consists of flaser rocks derived from volcanic rocks bounding the fault zone, but in the absence of new information on the remainder of the belt, the original interpretation that these rocks are of epiclastic origin is accepted.

During this investigation the epiclastic rocks near the east boundary of the study area were examined only along the North Fork of the American River where they are more than 5,000 feet (1,500 m) thick and consist mostly of dark-gray slate now converted to hornfels. At the east boundary of the epiclastic rocks near the mouth of Serena Creek (pi. 1) is a conglomerate consisting of fragments of chert, quartz graywacke, black slate fragments, and angular to rounded quartz sand grains. Structure and top directions indicate that these

epiclastic rocks overlie the Milton Formation and suggest that their age is within the range of Middle to Late Jurassic.

Near the Drum Power Station on the Bear River, distant from any similar rocks (pi. 1), a block of epiclastic rocks about 2,500 feet (680 m) wide and more than 2,000 feet (600 m) long is surrounded, or nearly so, by serpentine. The block consists of dark-gray silty slate, graywacke, tuff, and bedded conglomerate. The conglomerate and coarse graywacke contain, in addition to quartz grains, fragments of chert, fine-grained quartz-bearing intrusive rock, graywacke similar to that of the Shoo Fly Formation, quartz-mica schist, mafic or intermediate volcanic rocks, and carbonate rock.

The epiclastic rocks along Slate Creek in the north-central part of the map area (pi. 1) are represented by poor exposures of slate and graywacke. To the south, near the State Highway 49 bridge across the North Yuba River, petromict conglomerate is interbed-ded with dark-gray slate on the river margins and in highway cuts south of the river. Exposures near the North Yuba River west of Goodyears Bar that are included with this unit consist largely of sheared phyllite containing fragments of chert that before deformation were probably interbedded with the originally slaty fraction of the phyllite. This belt contains some interbedded tuff and, near the west boundary of sec. 12, T. 19 N., R. 9 E., contains conglomerate with pebbles of chert and volcanic rocks. The map pattern and facing of bedding tops suggest that these epiclastic rocks intertongue with the surrounding volcanic rocks. Preservation of bedding details in the epiclastic and, to a lesser extent, in the volcanic rocks permits an interpretation that they rest unconformably on the much more deformed Calaveras Formation.

The unnamed epiclastic rocks along the Middle and North Forks of the American River differ from those farther south in that chert constitutes about 5 percent of the total section and some of the slate is quartzose. Volcanic rocks, some so altered that their original texture and structure are undecipherable, constitute about 10 percent of the section along the North and Middle Forks of the American River. Recognizable tuff occurs along the North Fork north of Iowa Hill. Pillow lava occurs on the North Fork at the mouth of a tributary canyon near the east boundary of sec. 30, T. 15 N., R. 10 E., and at Fords Bar on the Middle Fork. Volcanic breccia and tuff occur near the mouth of New Orleans Gulch along the Middle Fork.

Unnamed epiclastic rocks in the south-central part of the area occur approximately along the strike projection of epiclastic rocks that conformably overlie the Logtown Ridge Formation along the Cosumnes River 6 miles (9.5﻿24

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

km) south of plate 1. These epiclastic rocks consist mostly of black siltstone but contain some beds of tuff, graywacke, and fine conglomerate. Along the South Fork of the American River, the composition of the epiclastic rocks is similar, dark-gray silty slate constituting most of the section east and west of State Highway 49. Conglomerate or volcanic breccia occurs in the SEy4 sec. 27, T. 11 N„ R. 10 E.

Coarse fragmental rocks, some possibly of tectonic origin but most of epiclastic origin, occur along the North and Middle Forks of the American River. Conglomeratic mudstone containing fragments of carbonate rock and, in places, of volcanic rocks is interbedded with dark-gray phyllite in the bed of the North Fork of the American River about 500 feet (150 m) east of Cosumnes-type rocks. The matrix of the mudstone is phyllite similar to that with which the conglomeratic mudstone is interbedded. Conglomeratic mudstone is most readily observed along the Bunch Canyon road southeast of Colfax.

The unnamed Mesozoic epiclastic rocks in the south-central part of the area are bounded on the east by major faults; on the west the epiclastic rocks adjoin volcanic rocks that are either known or inferred to be of Late Jurassic age. Epiclastic rocks at the south boundary of the area are on strike with similar rocks that overlie the early Late Jurassic Logtown Ridge Formation 7 miles (11.2 km) south of the area of this report (Clark, 1964, p. 26-27, pi. 8). Stratigraphic relations of the unnamed epiclastic rocks suggest that the same relation holds near the South Fork of the American River. Farther north, structural and stratigraphic relations are less clear, but no flaser rocks such as those characteristic of major fault zones elsewhere in the region were found between the unnamed epiclastic rocks and the volcanic rocks to the west. In the absence of a major fault, the epiclastic rocks must be younger than the rocks to the west, for tops of beds face eastward and different lithologies on opposite sides of the contract preclude the existence of any but minor folds. Two ammonites in the unnamed epiclastic rocks suggest a Late Jurassic age: A single specimen of Perisphinctes (Dichotomosphinctes?) spp. (Imlay, 1961, pi. 5, fig. 6) was collected in Big Canyon about 2 miles north of Placerville in the SW14 sec. 36, T. 11 N., R. 11 E., and a specimen of P. (Dichotomosphinctes) muhlbachi Hyatt is reported to have been found near Greenwood (Imlay, 1961, p. D7-D8, pi. 4, fig. 8).

UNNAMED VOLCANIC ROCKS

Unnamed volcanic rocks of Late and probable Late Jurassic age underlie much of the area west of the Shoo Fly Formation. They were mapped as diabase, porphy-rite, and amphibolite by Lindgren (1894, 1900), by Turner (1898), and by Lindgren and Turner (1894,

1895). Lindgren and Turner considered the age of the volcanic rocks to be equivalent to or younger than that of the Mariposa Formation or, where stratigraphic information was especially scanty, simply as pre-Cretaceous. Creeley (1965, p. 11, pi. 2) considered volcanic rocks east of the Monte de Oro Formation near Oroville to be of late Paleozoic age on the basis of unspecified stratigraphic relations and degree of metamorphism. In this report these rocks are considered to be of Late and probable Late Jurassic age. In the southwestern, northwestern, and central parts of the area, the volcanic rocks are commonly schistose, but except in narrow shear zones, original textures and structures are readily identifiable. Most of these volcanic rocks appear in the field to be of basaltic or andesitic composition. Compton (1955, p. 13) found that in the vicinity of Bidwell Bar on the Feather River "by far the majority of the metavolcanic rocks were originally basalt or pyroxene andesite flows, dolerite flows and sills, and basic tuffs or tuffaceous sediments.” Hietanen (1951, p. 568) found that north of Bidwell Bar near the north boundary of the map (pi. 1), the metavolcanic rocks are metabasalt, metadiorite, metadacite, metarhyolite, and metamorphosed tuff and agglomerate.

Abundant dikes suggest eruptive centers near Lake Combie on the Bear River, near the south end of Englebright Reservoir on the Yuba River where dikes as much as 30 feet (9 m) thick constitute about half of the area of canyon walls, at a locality about 1 mile (1.6 km) west of the Colgate Power Station on the North Yuba River and near Bidwell Bar. Pillow lavas are most abundant within a few miles of the dike complexes.

The unnamed Jurassic volcanic rocks are generally similar to those in the southern part of the western Sierra Nevada metamorphic belt already described by Clark (1964, p. 18-23, 26-29) and to those in the northern part of the metamorphic belt described by Compton (1955, p. 13) and Creeley (1965, p. 21-24). Accordingly, descriptions of these rocks are here limited to localities of special interest. Evidence of submarine slumping and contemporaneous deformation is well displayed along the Bear River east of the shear zone in sec. 34, T. 14 N., R. 7 E., in layers of fragmental rocks that overlie a bedded tuff unit. The bedded tuff is undisturbed except that a slumped and rotated block about 10 feet (3 m) long broke loose from the top of the upper part of the bedded tuff unit and is now separated from the in situ tuff by clastic dikes. The bedded tuff is overlain by chaotically deposited intraformational breccia about 30 feet (9 m) thick, which consists of fragments of bedded tuff that range in size from pebbles to blocks. A 4-foot-thick (1.2 m) layer of bedded intraformational breccia divides the chaotic breccia into two parts. Downstream from the breccia, thick-bedded﻿REFERENCES CITED

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tuff is planar, but thin-bedded tuff is contorted into complex patterns.

Selvaged lava bodies of bizarre shapes occuring at The Narrows on the Yuba River and about 900 feet (270 m) S. 30° E. of the center of sec. 34, T. 14 N., R. 7 E., on the Bear River suggest submarine emplacement of lava into unconsolidated pyroclastic material. The bodies resemble pillows in that they are bounded by selvages but differ from pillows in their angular to amoeboid form and wide range in size. Jasper forms veinlike bodies and fills some amygdules at the Bear River locality. Transition of pillow lava upward into massive lava within a single flow unit is well shown on the Yuba River in sec. 15, T. 17 N., R. 7 E. The change from pillow to massive structure is marked by attenuation of pillow selvages into discontinuous partings that disappear upward into massive lava.

Within the area of this report, fossils were found only in the volcanic strata that underlie the Monte de Oro Formation northeast of Oroville (pi. 1). These beds, as well as those adjacent to Cosumnes-type rocks in the vicinity of the anticline near Colfax are possibly equivalent to the Logtown Ridge Formation. The rocks of this map unit are considerably more folded than the eastern belt of Mesozoic rocks and those near the south boundary of the map area, and the stratigraphic section is probably duplicated. The total thickness of the exposed part of the broad western belt of volcanic rocks could be as little as 10,000 feet (3,000 m).

Owing to facies changes and fault zones that interrupt stratigraphic continuity, most of the unnamed Mesozoic volcanic rocks cannot be assigned with confidence to named formations. The Gopher Ridge Volcanics possibly occurs in the broad western belt of volcanic rocks between Folsom Reservoir and Oroville, but fossils and more detailed mapping are needed to establish correlations. Graded bedding in the Cosumnes-type rocks and in the volcanic rocks adjacent to them on the east along the North and Middle Forks of the American River indicates that tops of beds face eastward and that the volcanic rocks overlie the Cosumnes-type rocks. Some evidence of faulting was found near the contact of these units along the North Fork of the American River east of Colfax, but no evidence of a fault was found at the contact farther south along the North Fork of the American River.

A specimen of Perisphinctes sp. suggests that the volcanic rocks transitionally underlying the Monte de Oro Formation are of Late Jurassic (Oxfordian) age (S. W. Muller, in Creeley, 1965, p. 24).

REFERENCES CITED

Bateman, P. C., and Clark, L. D., 1974, Stratigraphic and structural setting of the Sierra Nevada batholith, California: Pacific Geology, v. 8, p. 79-89.

Burnett, J. L., and Jennings, C. W., compilers, 1962, Geologic map of California, Olaf P. Jenkins edition, Chico sheet: California Div. Mines and Geology, scale 1:250,000.

Chandra, D. K., 1961, Geology and mineral deposits of the Colfax and Foresthill quadrangles, California: California Div. Mines Spec. Rept. 67, 50 p.

Clark, L. D., 1954, Geology and mineral deposits of the Calaveritas quadrangle, Calaveras County, California: California Div. Mines Spec. Rept. 40, 23 p.

------1960, Foothills fault system, western Sierra Nevada, California: Geol. Soc. America Bull., v. 71, p. 483-496.

------1964, Stratigraphy and structure of part of the western Sierra

Nevada metamorphic belt, California: U.S. Geol. Survey Prof. Paper 410, 70 p.

Clark, L. D., and Huber, N. K., 1975, Geologic observations and sections along selected stream traverses, northern Sierra Nevada metamorphic belt, California: U.S. Geol. Survey Misc. Field Studies Map MF-690, 3 sheets.

Clark, L. D., Imlay, R. W., McMath, V. E., and Silberling, N. J., 1962, Angular unconformity between Mesozoic and Paleozoic rocks in the northern Sierra Nevada, California, in Geological Survey research 1962: U.S. Geol. Survey Prof. Paper 450-B, p. B15-B19.

Clark, S. G., 1930, The Milton Formation of California: California Univ., Berkeley, Ph. D. thesis, 206 p.

Compton, R. R., 1955, Tronhjemite batholith near Bidwell Bar, California: Geol. Soc. America Bull., v. 66, p. 9-44.

Creely, R. S., 1965, Geology of the Oroville quadrangle, California: California Div. Mines and Geology Bull. 184, 86 p.

Crickmay, C. H., 1933, Some of Alpheus Hyatt’s unfigured types from the Jurassic of California: U.S. Geol. Survey Prof. Paper 175, p. 51-64.

Crowell, J. C., 1957, Origin of pebbly mudstones: Geol. Soc. America Bull., v. 68, p. 993-1009.

Diller, J. S., 1892, Geology of the Taylorsville region of California: Geol. Soc. America Bull., v. 3, p. 370-394.

------1895, Description of the Lassen Peak sheet [California]: U.S.

Geol. Survey Geol. Atlas, Folio 15, 4 p.

------1908, Geology of the Taylorsville region, California: U.S. Geol.

Survey Bull. 353, 128 p.

Duffield, W. A., and Sharp, R. V., 1975, Geology of the Sierra Foothills Melange and adjacent areas, Amador County, California: U.S. Geol. Survey Prof. Paper 827, 30 p.

Durrell, Cordell, and Proctor, P. D., 1948, Iron-ore deposits near Lake Hawley and Spencer Lakes, Sierra County, California, Pt. L of Iron resources of California: California Div. Mines Bull. 129, p. 165-192.

Evemden, J. F., and Kistler, R. W., 1970, Chronology of emplacement of Mesozoic batholithic complexes in California and western Nevada: U.S. Geol. Survey Prof. Paper 623, 42 p.

Ferguson, H. G., and Gannett, R. W., 1932, Gold quartz veins of the Alleghany district, California: U.S.Geol. Survey Prof. Paper 172, 139 p.

Fry, W. L:,1964, Significant aspects of the Late Jurassic flora from the Monte de Oro Formation in northern California [abs.]: Geol. Soc. America Spec. Paper 76, p. 64-65.

Hietanen, A. M., 1951, Metamorphic and igneous rocks of the Merrimac area, Plumas National Forest, California: Geol. Soc. America Bull., v. 62, p. 565-607.

Hyatt, Alpheus, 1894, Trias and Jura in the western states: Geol. Soc. America Bull., v. 5, p. 395-434.

Imlay, R. W., 1961, Late Jurassic ammonites from the western Sierra Nevada, California: U.S. Geol. Survey Prof. Paper 374-D, 30 p.

------1967, The Mesozoic pelecypods Otapiria and Lupherella Imlay,

new genus, in the United States: U.S. Geol. Survey Prof. Paper 573-B, 11 p.

------1968, Lower Jurassic (Pliensbachian and Toarcian) ammonites﻿26

WESTERN SIERRA NEVADA METAMORPHIC BELT, CALIFORNIA

from eastern Oregon and California: U.S. Geol. Survey Prof. Paper 593-C, 51 p.

Knopf, Adolph, 1929, The Mother Lode system of California: U.S.

Geol. Survey Prof. Paper 157s 88 p.

Lindgren, Waldemar, 1894, Description of the gold belt; description of the Sacramento sheet [California]: U.S. Geol. Survey Geol. Atlas, Folio 5, 3 p.

—	---1896, The gold-quartz veins of Nevada City and Grass Valley

districts, California: U.S. Geol. Survey Ann. Rept. 17, pt. 2,

p. 1-262.

------1897, Description of the gold belt; description of the Truckee

quadrangle [California]: U.S. Geol. Survey Geol. Atlas, Folio 39,8 P-

—	---1900, Description of the Colfax quadrangle [California]: U.S.

Geol. Survey Geol. Atlas, Folio 66, 10 p.

Lindgren, Waldemar, and Turner, H. W., 1894, Description of the gold belt; description of the Placerville sheet [California]: U.S. Geol. ■ Survey Geol. Atlas, Folio 3, 3 p.

------1895, Description of the gold belt; description of the Smartsville

sheet [California]: U.S. Geol. Survey Geol. Atlas, Folio 18, 6 p. McKee, E. D., Oriel, S. S., Ketner, K. B., MacLachlan, M. E., Goldsmith, J. W., MacLachlan, J. C., and Mudge, M. R., 1959, Paleotectonic maps of the Triassic System: U.S. Geol. Survey Misc. Geol. Inv. Map 1-300, 33 p.

McMath, V. E., 1966, Geology of the Taylorsville area, northern Sierra Nevada, in Geology of northern California: California Div. Mines and Geology Bull. 190, p. 173-183.

Olmsted, F. H., 1971, Pre-Cenozoic geology of the south half of the Auburn 15-minute quadrangle, California: U.S. Geol. Survey Bull. 1341, 30 p.

Pettijohn, F. J., 1957, Sedimentary rocks [2d ed.]: New York, Harper and Brothers, 718 p.

Sharp, R. V., and Duffield, W. A., 1973, Reinterpretation of the boundary between the Cosumnes and Logtown Ridge Formations, Amador County, California: Geol. Soc. America Bull., v. 84, no. 12, p. 3969-3976.

Smith, J. P., 1910, The geologic record of California: Jour. Geology, v. 18, p. 216-227.

-------1927, Upper Triassic marine invertebrate faunas of North

America: U.S. Geol. Survey Prof. Paper 141, 262 p.

Strand, R. G., and Koenig, J. B., compilers, 1965, Geologic map of California, Olaf P. Jenkins edition, Sacramento sheet: California Div. Mines and Geology, scale 1:250,000.

Taliaferro, N. L., 1942, Geologic history and correlation of the Jurassic of southwestern Oregon and California: Geol. Soc. America Bull., v. 53, p. 71-112.

-------1943, Manganese deposits of the Sierra Nevada, their genesis

and metamorphism: California Div. Mines Bull. 125, p. 277-332. Turner, H. W., 1893a, Some recent contributions to the geology of California: Am. Geologist, v. 11, p. 307-324.

-------1893b, Mesozoic granite in Plumas County, California, and the

Calaveras Formation: Am. Geologist, v. 11, p. 425-426.

-------1894a, Description of the gold belt; description of the Jackson

sheet [California]: U.S. Geol. Survey Geol. Atlas, Folio 11, 6 p.

-------1894b, Geological notes on the Sierra Nevada: Am. Geologist, v.

13,	p. 228-249.

----—1896, Further contributions to the geology of the Sierra

Nevada: U.S. Geol. Survey Ann. Rept. 17, pt. 1, p. 521-762.

-------1897, Description of the gold belt; description of the Downie-

ville quadrangle [California]: U.S. Geol. Survey Geol. Atlas, Folio 37, 8 p.

-------1898, Description of the gold belt; description of the Bidwell Bar

quadrangle [California]: U.S. Geol. Survey Geol. Atlas, Folio 43,

6p.

Tyrrell, G. W., 1929, The principles of petrology; an introduction to the science of rocks [2d ed.]: New York, E. P. Dutton and Company, 349 p.

U.S. Geological Survey and California Division of Mines and Geology, 1966, Geologic map of California: U.S. Geol. Survey Misc. Geol. Inv. Map 1-512, scale 1:2,500,000.

Wheeler, H. E., 1939, Helicoprion in the Anthracolothic (late Paleozoic) of Nevada and California, and its stratigraphic significance: Jour. Paleontology, v. 13, p. 103-114.

White, W. S., 1949, Cleavage in east-central Vermont: Am. Geophys. Union Trans., v. 30, p. 587-594.﻿﻿MESOZOIC AND PALEOZOIC

PALEOZOIC

Burnett, J. L., and Jennings, C. W., 1962

Compton, R. R., 1955

Hietanen, A. M., 1951

Lindgren, Waldemar, 1894, 1896

Lindgren, Waldemar, and Turner, H. W., 1894

Olmsted, F. H., 1971

Strand, R. G., and Koenig, J. B., 1965

Base from U. S. Army Map Service 1:250,000

Chico, 1961,and Sacramento, 1964, California

This map was reproduced by electronic color scanning

SEDIMENTARY AND VOLCANIC ROCKS — Gently dipping and nonmeta-morphosed. Differentiated only along western border of map

GRANITIC ROCKS - Mostly quartz diorite to granodiorite in composition

ULTRAMAEIC ROCKS Mostly serpentine. Includes some peridotite and dunite

COPPER HILL VOLCANICS (Upper Jurassic) - Mafic pyroclastic rocks and lava. Locally includes lava with pillow structure

MONTE DE ORO FORMATION (Upper Jurassic) - Slate, graywacke, tuff(?), and conglomerate. Contains plant fossils. Recognized only northeast of Oroville

SALT SPRING SLATE (Upper Jurassic) — Dark-gray slate with subordinate tuff and graywacke. Recognized only in southwest corner of map area

EPICLASTIC ROCKS — Dark-gray slate with some interbedded conglomerate, thin-bedded chert. Probably includes mafic tuff in eastern part of map area

VOLCANIC ROCKS - Chiefly mafic volcanic breccia and tuff. Includes pillow lava near Yuba and Bear Rivers

LOGTOWN RIDGE FORMATION (Upper Jurassic) — Volcanic breccia. Locally porphyritic with pyroxene phenocrysts, tuff, and subordinate pillow lava. Mafic to intermediate composition

GOPHER RIDGE VOLCANICS (Upper(?) Jurassic) - Mafic pyroclastic rocks. Mapped only in southwest corner of map area. Approximate correlative of Logtown Ridge Formation

COSUMNES-TYPE ROCKS - Slate, conglomerate, graywacke, and tuff or tuffaceous graywacke. Includes porphyritic ellipsoidal lava along Interstate Highway 80

MILTON FORMATION (Middle or Upper Jurassic) - Mostly mafic volcanic breccia and tuff. Includes dark-gray slate east of Sierra City. Includes sparse chert, conglomerate, and calcarenite near Milton Reservoir

SAILOR CANYON FORMATION (Lower and Middle Jurassic) - Chiefly slate and tuff with subordinate graywacke, sparse conglomerate, and calcarenite

CHERT BRECCIA AND LIMESTONE — Poorly sorted breccia consisting of chert fragments overlain by limestone that is in part argillaceous. Mapped only near North Fork of American River south of Cisco

EPICLASTIC ROCKS - Chiefly dark-gray slate, but contains graywacke, conglomerate, and tuff. Near State Highway 49, possibly consists of flaser rocks derived from volcanic rocks

VOLCANIC AND SEDIMENTARY ROCKS - Chiefly mafic pyroclastic rocks. Northern part contains some thin-bedded chert. Southern part includes subordinate slate. Is, fossilferous limestone east of Auburn

META VOLCANIC ROCKS Mostly mafic,schistose. Local amphibolite. Bedded near North Yuba River. Locally massive

MAFIC INTRUSIVE AND METAMORPHIC ROCKS — Gabbroic and dioritic rocks and amphibolite. In part intrusive and in part the products of regional and of contact metamorphism

CALAVERAS FORMATION (Paleozoic) - Dark-gray phyHite and schist derived from shale with interbedded thin-bedded metachert. Includes subordinate volcanic rocks of probable andesitic composition. Locally includes:

Limestone. Two distinct lenses: one, near Middle Fork of the Feather River, is coarsely crystalline; the other, near Bear River west of Colfax, is fossiliferous

Bedded pyroclastic rocks of probable andesitic composition, thin-bedded metachert,and subordinate limestone

VOLCANIC ROCKS - Mostly mafic pyroclastic rocks and some pillow lavas. Includes rhyolite along southwestern margin of unit

SHOO FLY FORMATION (Silurian) — Chiefly feldspathic quartz-rich sandstone and tuffaceous sandstone having graywacke texture and slate or very fine tuff. Subordinate thin-bedded chert, mafic volcanic rocks, and calcarenite. Locally includes:

Dolomitic limestone. In part oolitic. Mapped only near Middle Fork of the Feather River

Dark-gray slate with subordinate chert, conglomerate, and sandstone

Contact

1 Fault Dotted where concealed. Most faults are probably steeply east dipping reverse faults

Strike and dip of beds and lava flows Inclined Vertical Overturned

Crumpled. Dip and strike generalized

Strike and dip of planar structures. Symbols may be combined with bedding symbols

Inclined schistosity Vertical schistosity Inclined phyllitic or slaty cleavage Vertical phyllitic or slaty cleavage

Direction of tops of beds and flows. Plotted along strike with point of observation Graded beds Pillow lava

121°12’15"

121°00'

45'

SCALE 1:316,800 5	10

15

30'	laons'ao"

Interior—Geological Survey, Reston, Va.—19 7 6—G75119

20 MILES

10

15

20 KILOMETRES

GEOLOGIC MAP OF THE NORTHWESTERN SIERRA NEVADA, CALIFORNIA﻿Sr -4

7 DAY

HURRICANE AGNES RAINFALL AND FLOODS,

JUNE-JULY 1972

Report prepared jointly by the U.S. Geological Survey and the National Oceanic and Atmospheric Administration

U.S. DEPARTMENT OF THE INTERIOR • U.S. DEPARTMENT OF COMMERCE

LIBRARY

UNIVERSITY OF CALIFORNIA

SEP 2 4 1975

U.S.S-D-﻿


i-

■ .4 •:


.


﻿HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

By J. F. BAILEY and J. L. PATTERSON, U.S. Geological Survey and J. L. H. PAULHUS, National Weather Service, National Oceanic and Atmospheric Administration

GEOLOGICAL SURVEY PROFESSIONAL PAPER 924

Report prepared jointly by the U.S. Geological Survey and the National Oceanic and Atmospheric Administration

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON: 1975﻿UNITED STATES DEPARTMENT OF THE INTERIOR GEOLOGICAL SURVEY V. E. McKelvey, Director

UNITED STATES DEPARTMENT OF COMMERCE FREDERICK B. DENT, Secretary NATIONAL OCEANIC AND ATMOSPHERIC ADMINISTRATION Robert M. White, Administrator

Library of Congress Cataloging in Publication Data

Patterson, James Lee.

Hurricane Agnes rainfall and floods, June-July 1972.

(Geological Survey professional paper; 924)

Bibliography: p.

Includes index.

Supt. of Docs, no.: I 19.16:924

1.	Foods--Atlantic States. 2. Stream measurements-Atlantic States. 3. Atlantic States-Hurricane, 1972.

I.	Bailey, James F., joint author. II. Paulhus, Joseph L. H., joint author. III. United States. Geological Survey. IV. United States. National Oceanic and Atmospheric Administration. V. Title. VI. Series: United States. Geological Survey. Professional paper; 924.

GB1216.P37	557.3’08s	[551.4’8]	75-619211

For sale by the Superintendent of Documents, U.S. Government Printing Office

Washington, D.C. 20402﻿FOREWORD

The U.S. Geological Survey and the National Weather Service have a long history of cooperation in monitoring and describing the Nation’s water cycle—the movement of water as atmospheric moisture, as precipitation, as runoff, as streamflow, as ground water, and finally, through evaporation, its return to the atmosphere to begin the cycle over again. The cooperative effort has been a natural dovetailing of technical talent and responsibility: the National Weather Service as the Federal agency responsible for monitoring and predicting atmospheric moisture and precipitation, for forecasting river flow, and for issuing warnings of destructive weather events; and the U.S. Geological Survey as the primary agency for monitoring the quantity and quality of the earthbound water resources, including both ground water and surface water.

This report represents another step in the growth of our cooperative efforts. In some ways, this closer working arrangement has been spurred by five major flood disasters that have struck the Nation in the last 5 years. In August 1969, the remnants of Hurricane Camille caused flooding of the James River and other streams in central Virginia that left 152 people dead or missing. In February 1972, the failure of a coal-waste dam sent a flood wave down the Buffalo Creek Valley of West Virginia, leaving 118 people dead or missing. On June 9, 1972, extremely heavy rains over the eastern Black Hills of South Dakota produced record-breaking floods on Rapid Creek and other streams, leaving 237 dead and 8 missing. Beginning on June 18, 1972, the remains of Hurricane Agnes produced floods in the Eastern United States from Virginia to New York that killed 117 people in what has been called the worst disaster in American history. Most recently, the spring 1973 floods on the Mississippi River produced a record 89 days of floodflow at Vicksburg, Miss., and 78 days at St. Louis, Mo., inundated more than 11 million acres of land, and damaged over 30,000 homes.

These disasters have underlined the need to know more about and respect the force and flow of floodwater and have given impetus to further cooperation between the U.S. Geological Survey and the National Weather Service to combine their respective studies and information about flood events into single, unified reports. Hopefully, this documentation of the Hurricane Agnes floods will aid the understanding of such flood disasters and will help improve human preparedness for coping with future floods of a similar catastrophic magnitude.

Joseph S. Cragwall, Jr. Chief Hydrologist U.S. Geological Survey Department of the Interior

George P. Cressman Director

National Weather Service Department of Commerce

hi﻿﻿CONTENTS

Page

Abstract ______________________________________________ 1

Introduction __________________________________________ 1

Acknowledgments____________________________________ 2

Glossary___________________________________________ 3

Conversion factors--------------------------------- 4

Storm history__________________________________________ 4

Rainfall______________________________________________ 20

Flood frequency________________________________________ 56

The floods____________________________________________ 57

Streams tributary to Long Island Sound------------ 58

Delaware River basin______________________________ 58

Susquehanna River basin___________________________ 59

Susquehanna River main stem___________________ 59

Susquehanna River tributaries ________________ 60

Small basins tributary to Chesapeake	Bay______	63

Potomac River basin ______________________________ 65

Rappahannock River and York River	basins-----	68

James River basin_________________________________ 69

Chowan River and Roanoke River basins_____________ 72

Ohio River basin__________________________________ 73

Allegheny River basin ________________________ 73

Monongahela River basin_______________________ 74

Page

The floods—Continued

Ohio River basin—Continued

Kanawha River basin_____________________________ 74

Streams tributary to Lake Erie and	Lake Ontario.	75

Sedimentation____________________________________________ 76

Flood-crest elevations__________________________________ 78

Effect of regulation_____________________________________ 79

Susquehanna River basin_____________________________ 79

Small basins tributary to Chesapeake	Bay_______	80

Roanoke River basin ________________________________ 80

Ohio River basin___________________________________ 80

Streams tributary to Lake Ontario__________________ 81

Determination of flood discharge________________________ 81

Streamflow data at gaging stations and miscellaneous

measuring sites__________________________________ 82

Summary of peak stages and discharges-------------- 82

Station description and discharge tables___________ 82

Deaths and damage_______________________________________ 83

Selected references_____________________________________ 86

Streamflow data ________________________________________ 88

Index to streamflow data_______________________________ 358

Appendices _____________________________________________ 371

ILLUSTRATIONS

Plate	1. Map showing area of report and location of flood-data sites, Middle Atlantic States ___________________In pocket

Figure	1. Map showing storm track, June 14-23, 1972 ------------------------------------------------------------------ 6

2.	Composite satellite photographs showing development of Agnes near east coast of Yucatan on June

15 and June 16, 1972 ________________________________________________________________________________ 8

3.	Synoptic situation at 0700 EST, June 17, 1972 ------------------------------------------------------------ 10

4.	Synoptic	situation at 0700 EST, June 18, 1972 ______________________________________________________________ 11

5.	Synoptic	situation at 0700 EST, June 19, 1972 ______________________________________________________________ 12

6.	Synoptic	situation at 0700 EST, June 20, 1972 ______________________________________________________________ 13

7.	Synoptic	situation at 0700 EST, June 21, 1972 ______________________________________________________________ 14

8.	Synoptic	situation at 0700 EST, June 22, 1972 ______________________________________________________________ 15

9.	Synoptic	situation at 0700 EST, June 23, 1972 -------------------------------------------------------------- 16

10.	Synoptic	situation at 0700 EST, June 24, 1972 ______________________________________________________________ 17

11.	Pressure variation at selected stations along storm track----------------------------------------------------- 21

12.	Upper-air soundings at Cape Hatteras, N.C., June 19-22, 1972 _________________________________________________ 22

13.	Upper-air soundings at Sterling, Va. (near Washington, D.C.), June 20-23, 1972 _______________________________ 23

14.	Upper-air soundings at New York, N.Y., June 20-23, 1972 ______________________________________________________ 24

15-31. Maps showing:

15. Precipitation for May 1972 in percent of normal _________________________________________________ 25

16. Precipitation for June 1-15, 1972, in percent of normal _________________________________________ 25

17.	Rainfall, in inches over northern section for 24-hour period ending 0700 EST, June 16,	1972	26

18.	Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 17,	1972	27

19.	Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 17, 1972.	28

20.	Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 18,	1972	29

21.	Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 18,	1972	30

22.	Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 19,	1972	31

v﻿VI

CONTENTS

Figuers 15-31. Maps showing—Continued.	Page

23. Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 19, 1972	32

24. Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 20, 1972	33

25.	Rainfall,	in	inches, over southern section for 24-hour period ending 0700 EST, June 20, 1972	34

26.	Rainfall,	in	inches, over northern section for 24-hour period ending 0700 EST, June 21, 1972	35

27.	Rainfall,	in	inches, over southern section for 24-hour period ending 0700 EST, June 21, 1972	37

28.	Rainfall,	in	inches, over northern section for 24-hour period ending 0700 EST, June 22, 1972	38

29.	Rainfall,	in	inches, over northern section for 24-hour period ending 0700 EST, June 23, 1972	39

30.	Rainfall,	in	inches, over northern section for 24-hour period ending 0700 EST, June 24, 1972	40

31.	Rainfall,	in	inches, over northern section for 24-hour period ending 0700 EST, June 25, 1972	41

32.	Mass rainfall curves for three stations in Pennsylvania and one in Virginia for the period June 20-

23, 1972 ________________________________________________________________________________________ 42

33.	Mass rainfall curves for two stations in New York and two in Pennsylvania for the period June 20-

23, 1972.	  43

34.	Map showing total storm precipitation for the period 6 p.m., June 19, through 6 p.m., June 23, 1972	46

35. Maximum discharge versus drainage area for known floods___________________________________________ 57

36. Discharge hydrographs, Schuylkill River, June 21-28, 1972 ________________________________________ 58

37.	Discharge hydrographs, Susquehanna River, June 21-28, 1972 -------------------------------------- 59

38-44.Photographs showing:

38.	Susquehanna River at Wyoming, Pa ___________________________________________________________ 60

39.	Susquehanna	River at Kingston, Pa___________________________________________________________ 61

40.	Susquehanna River at Wilkes-Barre, Pa_______________________________________________________ 62

41.	Susquehanna River at Enola, Pa _____________________________________________________________ 63

42.	Susquehanna River at City Island at Harrisburg, Pa	-------------------------------------- 64

43.	Susquehanna River at Harrisburg, Pa ________________________________________________________ 65

44.	Susquehanna River at Steelton, Pa __________________________________________________________ 66

45.	Discharge hydrographs, Susquehanna River basin, June 21-28, 1972 ----------------------------------- 67

46.	Discharge hydrographs, Potomac River, June 21-28, 1972---------------------------------------------- 67

47-48. Photographs showing:

47.	Occoquan River at Virginia State Highway 123 bridge	at	Occoquan, Va ---------------------- 68

48.	Occoquan River at Occoquan Dam at Occoquan, Va _____________________________________________ 69

49.	Discharge hydrographs, Potomac River basin in Maryland, June	21-28,	1972 ---------------------- 70

50.	Discharge hydrographs, Potomac River basin in Virginia, June	21-24,	1972 _________________________ 70

51-52. Photographs showing:

51.	James River at U.S. Highway 522 at Maiden, Va----------------------------------------------- 71

52.	James River at Mayos Bridge at Richmond, Va_________________________________________________ 71

53.	Discharge hydrographs, James River, June 21-28, 1972________________________________________________ 72

54.	Discharge hydrographs, Ohio River basin, June 21-30, 1972 __________________________________________ 73

55.	Discharge hydrographs, Genesee River, June 21-28, 1972______________________________________________ 75

56-58. Photographs showing:

56.	Erosion on flood plain of Susquehanna River at Old Fort,	Pa_________________________________ 76

57.	Road washout in Shickshinny, Pa_____________________________________________________________ 77

58.	Deposition on farmland bordering Susquehanna River	near Exeter, Pa _________________________ 78

59.	Graph of water and sediment discharge, Susquehanna River at Harrisburg, Pa., June 21-30, 1972—	79

TABLES

Page

Table	1. Minimum sea-level pressure and maximum surface wind speeds at selected stations, June 18-25, 1972	18

2.	High tides attributed to Agnes, June 18-22, 1972 ___________________________________________________________ 19

3.	Maximum 6-, 12-, 24-, and 48-hour rainfall amounts at selected stations recording 24-hour amounts

of 10 or more inches during the period June 21-22, 1972 ____________________________________________ 44

4.	Maximum depth-area-duration data for major tropical storm rainfall	in the	Eastern United States-----	44

5.	Supplementary rainfall data for Northeastern United	States for June 18-26,	1972 ----------------------- 47

6.	The 10 most destructive tropical cyclones in the United	States since	1930 ____________________________ 83

7.	U.S. deaths and damages attributed to Agnes_________________________________________________________________ 83

8.	Classification of property damage __________________________________________________________________________ 84

Appendix A tables:

A-l. Summary of peak stages and discharges_______________________________________________________ 372

A-2. Flood-crest elevations, June 19, 1972, for streams in Westchester County, N.Y. and

southeast Connecticut________________________________________________________________ 389

A-3. Flood-crest elevations, June 1972 __________________________________________________________ 390

A-4. Flood-crest elevations, floods of 1936, 1969, and 1972, James River in Virginia_____________ 396﻿CONTENTS

VII

Page

Table	A-5. Reservoir storage and peak flow reduction, June-July 1972, in the Susquehanna River

basin in New York and Pennsylvania -------------------------------------------------- 397

A-6. Reservoir storage and peak-flow reduction, June-July 1972, in Roanoke River basin in

Virginia and North Carolina__________________________________________________________ 398

A-7. Reservoir storage and peak flow reduction, June-July 1972, in the Ohio River basin in

New York, Pennsylvania, and West Virginia____________________________________________ 399

A-8. Summary of historical and 1972 water and sediment discharge________________________________ 400﻿﻿HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

By J. F. Bailey and J. L. Patterson , U.S. Geological Survey, and J. L. H. PAULHUS, National Weather Service, National Oceanic and Atmospheric Administration

ABSTRACT

Hurricane Agnes originated in the Caribbean Sea region in mid-June. Circulation barely reached hurricane intensity for a brief period in the Gulf of Mexico. The storm crossed the Florida Panhandle coastline on June 19, 1972, and followed an unusually extended overland trajectory combining with an extratropical system to bring very heavy rain from the Caro-linas northward to New York. This torrential rain followed the abnormally wet May weather in the Middle Atlantic States and set the stage for the subsequent major flooding.

The record-breaking floods occurred in the Middle Atlantic States in late June and early July 1972. Many streams in the affected area experienced peak discharges several times the previous maxima of record. Estimated recurrence intervals of peak flows at many gaging stations on major rivers and their tributaries exceeded 100 years. The suspended-sediment concentration and load of most flooded streams were also unusually high. The widespread flooding from this storm caused Agnes to be called the most destructive hurricane in United States history, claiming 117 lives and causing damage estimated at $3.1 billion in 12 States. Damage was particularly high in New York, Pennsylvania, Maryland, and Virginia.

The detailed life history of Hurricane Agnes, including the tropical depression and tropical storm stages, is traced. Associated rainfalls are analyzed and compared with climatologic recurrence values. These are followed by a detailed description of the flood and streamflows of each affected basin. A summary of peak stages and discharges and comparison data for previous floods at 989 stations are presented. Deaths and flood damage estimates are compiled.

INTRODUCTION

A major flood caused by the exceptional rainfall associated with Hurricane Agnes ravaged the Middle Atlantic States in late June and early July 1972. The origin of Agnes can be traced back to a weak tropical disturbance first detectable over the Yucatan Peninsula on June 14. An interesting hypothesis advanced by Namias (1973a) regarding the antecedent meteorologic events that could have triggered its birth is presented. The depression intensified rapidly and moved eastward into the Caribbean Sea. Fed by the sensible and latent heat energy provided by the warm sea surface, its circulation developed further. It reached tropical storm intensity on June 16 and started to curve northward heading straight toward the Florida Panhandle. Its maximum sur-

face wind near the center reached a speed of over 63 knots on June 18, while it was still in transit in the Gulf of Mexico. Agnes moved into the Florida Panhandle on June 19, with reduced maximum wind speeds. By the morning of the 20th the storm had weakened to tropical storm intensity. It never again reached the hurricane stage. Agnes would rank among the weakest hurricanes in intensity, but it had a relatively large diameter of 1,000 miles (1600 km). Also unusual was its extended overland trajectory after making landfall and the large amount of rainfall it brought over an extended area. Agnes’ “tropical” center was over water when the heaviest rains fell. Its long overland track extended through the relatively populous and industrially developed coastal regions of the Atlantic States. Furthermore, during the waning stage of its life cycle, the weakened Agnes merged with an extratropical cyclone circulation centered over Northeastern United States. This reinforced low then stagnated over western Pennsylvania for about 24 hours, yielding additional rain over the northeastern section of the Nation.

The rainfall over Eastern United States from Agnes and other weather systems during June 16-25 produced record floods. Greatest point rainfall occurred in Pennsylvania and New York. The greatest 24-hour amount measured was 14.8 inches in southeastern Pennsylvania at Gage R44 in the Ma-hantango Creek basin. This amount well exceeds the value for the 100-year recurrence interval. A series of daily isohyetal maps and mass curves of rainfall for selected stations show the progression of the rainfall associated with Agnes from Southeastern United States toward the northeast. A rainfall map for Northeastern United States for the total storm period shows the magnitude of precipitation. Total precipitation at several locations from New York to Virginia was in excess of 15 inches. A comparison between Agnes and other tropical storms over the same region indicated that, for areas greater than 10,000 square miles and durations longer than 24 hours, Agnes rainfall set a record.

1﻿2

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

This complete description of the rainfall associated with this storm utilized considerable supplementary data as well as the regular reporting network. These supplementary data came from sources other than official gages and are included in tables of this report.

The flooding caused by the exceptional precipitation ravaged parts of 12 States. Peak stages and discharges established new records on many streams, and many reservoirs in New York and Pennsylvania were at their highest levels since construction. In the Susquehanna River basin, peak flows at many locations exceeded the maximum of record. Along the main stem of the Susquehanna from the New York-Pennsylvania border to its mouth on the Chesapeake Bay, this was the greatest flood since at least 1784. Peak flows from Harrisburg downstream to the bay were in excess of 1 million cubic feet per second (cfs). Although flooding on the main stem of the Potomac River was not exceptional, many of its tributaries downstream from the Shenandoah River experienced record flows. Peak flows on the Conococheague Creek at Fairview, Md., and on the Monocacy River near Frederick, Md., were greater than the flood of 1889, and the peak discharge of Difficult Run near Great Falls, Va., was 5 times the previous maximum for the period of record beginning in 1935. On the James River from Lynchburg to Richmond in Virginia, peak flows exceeded those resulting from the passage of Hurricane Camille in 1969 to become the highest since at least 1870. A maximum flow of 313,000 cfs occurred at Richmond. Detailed description of the flood for each affected drainage basin together with significant discharge hydrographs for affected major rivers are presented in the text.

The suspended-sediment concentration and load of most streams were unusually high. Sediment loads during the flood period on the Susquehanna and Schuylkill Rivers in Pennsylvania were three times their average annual loads.

The effectiveness of reservoir-storage regulation in controlling the magnitude of peak flows for the Susquehanna, Roanoke, and Ohio River basins, and for some streams tributary to Chesapeake Bay and to Lake Ontario was examined on the basis of data supplied by the U.S. Army Corps of Engineers.

Total damage from Hurricane Agnes was estimated to be $3.1 billion, or over twice that produced by Camille, the second most destructive hurricane to strike the United States. Most of the damage resulted from flooding in the Middle Atlantic States. Damage reached $2.12 billion in Pennsylvania alone, making this the worst natural disaster in the history

of that State. Damage included destruction of homes and other structures, flooding of public water and sewage facilities, inundation of industrial and public utility plants, loss of crops, and disruption of normal activities. Owing to the timely warning issued to the public, the total death toll of 117 persons was comparatively light considering the severity of the flooding.

Data for 989 gaging sites are furnished in this report. These data should provide a valuable reference for future investigations. All sites, for which data on discharge, stage, and sediment are given, are numbered consecutively in downstream order and in the same sequence as is used in parts 1-4 in water-supply papers of the U.S. Geological Survey containing records of streamflow. Included in the numbering are gaging stations, reservoir stations, partial record stations, and miscellaneous sites. The location of each site is shown by report number on the map (pi. 1). The report number appears in parentheses preceding the site title in the section on streamflow data and in the tables in Appendix A. The permanent station number assigned by the

U.S. Geological Survey is also shown in the stream-flow data. Peak stage and discharge at gaging stations, flood-crest elevations for selected stream reaches, and reservoir-storage data are given in Appendix A.

This report was prepared jointly by the U.S. Geological Survey and the National Weather Service. Additional sources for both meteorologic and hydrologic data are included in Appendix B.

ACKNOWLEDGMENTS

The meteorologic and rainfall analyses in this report are based upon the efforts of many individuals within the National Weather Service. These people make and record thousands of observations and analyze countless charts in supporting an effort such as this. Hundreds of precipitation observations are made by unpaid volunteers in the cooperative observing program of National Oceanic and Atmospheric Administration. The supplementary rainfall data included in this report were collected under the supervision of John Thomas, Regional Hydrologist, National Weather Service, Eastern Region. The hurricane track shown in figure 1 was obtained from the National Hurricane Center, Robert H. Simpson, Director. John F. Miller, Chief, Water Management Information Division, and Dr. Edwin Chin of that Division have reviewed the manuscript.

Discharge records and other flood data in this report were collected as part of cooperative pro-﻿INTRODUCTION

3

grams between the U.S. Geological Survey and the States of North Carolina, Virginia, Maryland, West Virginia, Pennsylvania, New York, and Connecticut; county and municipal agencies within these States; and agencies of the Federal Government. Other Federal and State agencies, municipalities, universities, corporations, and individuals gave assistance, financial or otherwise, in the data-collection effort. Credit for this assistance is given in the appropriate place in the text. During the flood emergency, engineers and technicians of the U.S. Geological Survey from 23 States were detailed into the Northeastern area to assist in the collection of flood data. Their assistance is gratefully acknowledged.

Photographs in this report were obtained from Federal and State agencies, newspapers, and individuals. Where appropriate, photograph sources are given.

The U.S. Army Corps of Engineers provided the information on damage.

GLOSSARY

Acre-foot (acre-ft).—The quantity of water required to cover 1 acre to a depth of 1 foot and is equal to 43,560 cubic feet, 325,851 gallons, or 1,223 cubic metres.

Contents.—The volume of water in a reservoir or lake. Content is computed on the basis of a level pool and does not include bank storage. Convective clouds.—A cloud which owes its vertical development and possibly its origin to convection.

Cubic feet per second (cfs).—The rate of discharge. One cubic foot per second is equal to the discharge of a stream of rectangular cross section 1 foot wide and 1 foot deep, flowing at an average velocity of 1 foot per second. It equals 28.32 litres per second or 0.02832 cubic metres per second.

cfs-day.—The volume of water represented by a flow of 1 cubic foot per second for 24 hours. It equals 86,400 cubic feet, 1.98 acre-feet, or 2,447 cubic metres.

cfsm (cubic feet per second per square mile).—The average number of cubic feet of water per second flowing from each square mile of area drained by a stream, with the assumption that the runoff is distributed uniformly in time and area. One cfsm is equivalent to 0.0733 cubic metres per second per square kilometre. Crest-stage station.—A particular site where only information on crest stage and peak discharge is collected systematically.

Depression.—An area of low atmospheric pressure.

Drainage area of a stream at a specific location.— The area, measured in a horizontal plane, which is enclosed by a topographic divide. Drainage area is given in square miles. One square mile is equivalent to 2.590 square kilometres.

Extratropical low (extratropical cyclone).—Any cyclone-scale storm that is not a tropical cyclone, usually referring only to the migratory frontal cyclones of middle and high latitudes.

Flood-hydrograph station.—A particular site where a record of the flood hydrograph is collected systematically.

Gaging station.—A particular site on a stream, canal, lake, or reservoir where systematic observations of gage height or discharge are obtained.

Gust.—A sudden brief increase in the speed of the wind.

Hurricane.—A severe tropical cyclone (windspeed 64 knots or higher) in the North Atlantic Ocean, Caribbean Sea, Gulf of Mexico, and in the Eastern North Pacific of the west coast of Mexico.

Instability.—Areas of instability as referred to in this report are areas where the lifted index is less than four. The lifted index is the difference, in °C, between the observed 500-mb temperature and the computed temperature, which a parcel characterized by the mean temperature and dew point of the 50-mb-thick surface layer would have if it were lifted from 25 mb above the surface to 500 mb.

Mean low water.—The average level of low water at a place over a 19-year period.

Mean sea level.—The average height of the sea surface for all stages of the tide over a 19-year period.

Miscellaneous site.—A site where data pertaining only to a specific hydrologic event are obtained.

Precipitable water.—The total atmospheric water vapor contained in a vertical column of unit-cross-sectional area extending from the surface up to a certain pressure level, usually 500 mb.

Runoff.—That part of the precipitation that appears in streams. It is the same as streamflow that is unaffected by artificial diversions, storage, or other works of man in or on the stream channels. Runoff, given in inches (1 inch is 2.54 centimetres), is the depth to which the drainage area would be covered if the runoff for a given time period were uniformly distributed over the surface.

Sediment.—Fragmental material that originated from weathering of rocks and is transported by,﻿4

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

suspended in, or deposited by water or air or is accumulated in beds by other natural agencies.

Sediment concentration.—The weight of dry solids divided by the weight of water-sediment mixture and is expressed in milligrams per litre (mg/1).

Sediment discharge.—The rate at which dry weight of sediment passes a section of a stream, or it is the quantity of sediment, as measured by dry weight or by volume, that is discharged in a given time.

Sediment load.—The sediment moved by a stream, whether in suspension or at the bottom. It is synonymous with “sediment discharge” in this report and is used to avoid possible confusion between stream discharge and sediment discharge.

Sediment station.—A river section where sedimentload samples are taken each day, or periodically.

Sounding.—A single complete radiosonde observation of the upper atmosphere.

Stage-discharge relation.—The relation between gage height and the amount of water flowing in a channel.

Suspended load.—Sediment that moves in suspension. It is transported at virtually the velocity of water.

Time of day is expressed in 24-hour time; for example, 12:30 a.m. is 0030 hours, 1:00 p.m. is 1300 hours. All time noted is eastern daylight time.

Tons per day.—The unit used to express the quantity of sediment that passes a particular site during a 24-hour period.

Tropical storm.—Tropical cyclone with winds 34 to 63 knots.

Trough.—An elongated area of relatively low atmospheric pressure.

CONVERSION FACTORS

Most units of measure used in this report are

English Units. The following factors can be used

to convert English Units to the International System of Units (SI).

Multiply English units

inches (in.)__________

feet (ft) ____________

miles (mi)____________

miles (nautical)______

acres ________________

square miles (mi2) —

By

25.4 ________

.0254 ______

.3048 ______

1.609 _______

1.853 _______

4047 ___________

.004047 ___

2.590 _______

To obtain SI units

millimetres (mm) metres (m) metres (m) kilometres (km) kilometres (km) square metres (m ~) square kilometres (km2)

square kilometres (km2)

Multiply English units

gallons (gal)_______

million gallons (10 0 gal).

cubic feet (ft “)____

cfs-day (ft;7s-day) _

acre-feet (acre-ft)___

feet per second ____

miles per hour (mph).

knot________________

cubic feet per second (ft3/s)

gallons per minute (gpm).

million gallons per day (mgd).

ton (short)

By

3.785	_______

3.785	_______

3.785xl0~3 __

3785 ___________

3.785xl()-3 __

28.32	________

.02832 _____

2447 ___________

2.447xl0"3 —

1233 ___________

1.233x10-“ —

1.233x10 " __

.3048 ______

1.609 _______

1.853 _______

28.32	________

28.32	________

.02832 _____

.06309 _____

.06309 _____

6.309xl0-3

43.81_________

.04381 _____

.9072 ______

To obtain SI units

litres (1) cubic decimetres (dm3)

cubic metres (m 3)

cubic metres (m3) cubic hectometres (hm3)

cubic decimetres (dm3)

cubic metres (m3) cubic metres (m3) cubic hectometres (hm3)

cubic metres (m3) cubic hectometres (hm3)

cubic kilometres (km 3)

metres per second m/s

kilometres per hour km /hr

kilometres per hour km/hr

litres per second (1/s)

cubic decimetres per second (dm3/s) cubic metres per second (m3/s)

litres per second (1/s)

cubic decimetres per second (dm3/s) cubic metres per second (m3/s)

cubic decimetres per second (dm3/s) cubic metres per second (mVs) tonne (t)

STORM HISTORY

The formation process for a tropical storm is not always clear, and that for Agnes is no exception. The first signs of an incipient hurricane usually appear on satellite photographs as a large cloud mass showing indications of tropical storm circulation, and this occurs when the storm is already well along in the development stage. The problem of early identification of tropical storm formation may lie in the fact that different and perhaps multiple causes may be involved in the formation processes of different storms.

Namias (1973a) has suggested that Agnes “may have resulted from a combination of events involving an antecedent massive cold air outbreak into the tropics and, perhaps crucially, the migration of a nucleating cloud cluster of intense convective cells from the Southern Hemisphere tropics into the Northern Hemisphere.” From satellite photographs, he hypothesized that the nucleus for Agnes first﻿STORM HISTORY

5

appeared on June 9 in an area of abnormally warm surface water off the Pacific coast of Colombia at about lat 5° S. This nucleating mass of convective clouds moved northward over surface water with temperatures exceeding 80°F (27°C), crossed the Isthmus of Panama on June 12, and then started to curve northwestward over the Caribbean Sea. On June 13-14 this mesoscale cloud mass met a large-scale cloud environment associated with an intense cold front moving southward from the United States, across the Gulf of Mexico, and over the Caribbean Sea. This cold-air outbreak established record low temperatures for this time of the year at many cities in the Eastern United States. Again, quoting Namias: “Apparently, the large-scale convective cloud system associated with the cold front, the general cyclonic vorticity field, and the implied high moisture content aloft provided a favorable large-scale environment for triggering the hurricane by the nucleating intense mesoscale cloud system arriving from the south over anomalously warm water.” These immediate causes, Namias (1973b) further suggested, may be linked to midtropospheric anomalies in the large-scale air-sea circulation systems generated during the preceding 3 or 4 months.

At about 0700 EST, June 14, a weak depression in the surface-pressure field observed at about lat 20.0° N.; long 89.0° W., near Cozumel, Yucatan, was actually the first indication of the tropical disturbance that would become Hurricane Agnes (fig. 1). The depression intensified rapidly and moved slowly eastward along the lat 20° N. parallel until about 0700 EST, June 16 and then began to curve northward (fig. 1) as it reached tropical storm intensity (wind speeds 39-73 mph, or 34-63 knots). The cloud systems associated with the storm while moving eastward from Yucatan on June 15 and 16 appear distinctly on the satellite photographs of figure 2.

The storm continued northward at about 10 mph (16 km/hr) and was about 120 miles southwest of the west tip of Cuba by Saturday morning, June 17. By Saturday afternoon it had reached the Yucatan Channel, just west of the west tip of Cuba, with a minimum pressure of 986 mb (fig. 1). By early morning of June 18, the storm center was some 250 miles (400 km) southwest of the Florida Keys, and surface winds near the center were of hurricane force (over 73 mph, or 63 knots).

The satellite photograph in figure 3 shows a second well-defined circulation system east of Agnes. This system, which persisted throughout the life of Agnes, enhanced the already enormous flow of moisture and nearly saturated air into Agnes as the

latter moved northward over land.

At 0700 EST on the 18th, Agnes was centered at lat 23.8° N., long 85.6° W., about 200 mi (320 km) west of Fort Myers, Fla. (fig. 4), and showers were occurring over most of Florida south of Orlando. The upper-air soundings at that time showed that the unstable air covering the Southeastern United States on the morning of the 17th (fig. 3) had spread slightly northward (fig. 4). A similar increase in precipita-ble water was noted. At about 0900 EST, the barometric pressure at Tallahassee, Fla., began to fall rapidly (fig. 11), and rain began about 1400 EST. Table 1 lists the minimum sea-level pressure and maximum wind speed at selected stations affected by Agnes during June 18-25.

Agnes became a hurricane on the 18th. During the afternoon, maximum sustained surface-wind speeds near the storm center reached 85 mph (74 knots). Maximum sustained surface-wind speeds over land, strengthening first in the Keys and by evening as far north as Orlando, were 25-45 mph (22-43 knots), with gusts from 40 to 50 mph (35-43 knots). Wind speeds along Florida’s east coast were often higher than those along the west coast because the storm’s unusually large circulation, roughly 1,000 miles (1,600 km) in diameter (fig. 4), resulted in easterly to southeasterly surface winds with little reduction from overland friction. As a result, the highest gust reported in Florida was 69 mph (60 knots) at Cape Kennedy early on the 19th (table 1).

By the afternoon of the 18th it was obvious that Agnes would cross the Florida Panhandle and that her most destructive weapon in Florida would be the storm tides along the west coast.

At 0100 EST, June 19, Agnes reached her lowest central pressure, 978 mb, while in the Gulf of Mexico (lat 27.2° N.; long 85.7° W.), but neither the eye nor the wall cloud ever became fully developed.

By 0700 EST the storm had moved to lat 28.5° N.; long 85.7° W., about 75 miles (120 km) south of Apalachicola, Fla. (figs. 1 and 5). Soundings showed an appreciable increase in precipitable water over the Eastern United States during the preceding 24 hours (figs. 4 and 5), with the maximum amounts in the extreme southeastern part well exceeding average values for June (Reitan 1960). The area of atmospheric instability had spread northward. With the exception of a stable area centered over Alabama, the degree of instability had increased also, with the greatest instability noted over the Florida Peninsula.

Rain was falling as far to the northeast as Augusta, Ga., where the pressure began to fall rapidly﻿6

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

0	300	600 KILOMETRES

Figure 1.—Storm track, June 14-23, 1972.﻿STORM HISTORY

7

about 0900 EST (fig. 11). Pressure at Charlotte, N.C., started to fall at about the same time, but rain did not begin until about 1400 EST.

Agnes moved ashore on the afternoon of the 19th, with the center crossing the Florida coastline near Port St. Joe (about halfway between Apalachicola and Panama City). Maximum sustained surface-wind speeds reported at observing stations nearest the center were 40-45 mph (35-39 knots), with gusts reaching 45-55 mph (39-48 knots). Lowest pressure (991.2 mb) at Tallahassee, roughly 70 miles east of the storm center, was recorded at 1709 EST, with south-southeast surface winds veering to southwest and west (fig. 11), as the storm moved northeastward into Georgia (fig. 1).

The high storm tides first occurred in the Florida Keys on the afternoon of the 18th, with Key West and Big Pine Key both reporting high tides of 1.2 feet above normal (table 2). The data reported in the first part of table 2 represent the actual storm surge, except as noted. The value given is the departure from the normal height of the hourly tide curve. Flamingo reported a high tide 2.0 feet above normal on the same date. Most of the high tides in Florida, however, occurred on the 19th (table 2), with the highest tide (7.0 ft above normal) being recorded by Cedar Key in the afternoon. The Corps of Engineers, in a survey after the storm, determined that tides along the west coast of Florida increased from Lee County northward. In Lee County, tides were about 2 feet above normal. In Charlotte and Sarasota Counties, they ranged between 2 and 3 feet above normal, while in Manatee and Pinellas Counties they ranged between 3 and 6 feet above normal. As Agnes neared the Panhandle, Apalachicola recorded a tide 6.4 feet above normal in the afternoon. The National Ocean Survey conducted a survey in early 1973 along the northwest Florida coast to determine high-water marks for use in National Oceanic and Atmospheric Administration (NOAA) studies for the Federal Insurance Administration. These data are given in table 2.

Agnes spawned 15 confirmed tornadoes in Florida, all occurred on the 18th and 19th and all were confined to the peninsula south of Daytona Beach. Three tornadoes struck the Keys. The first roared through Geiger and Big Coppitt Keys early on the 18th. Before daylight, the second struck Key West, and the third ripped through Key Colony Beach, Grass Key, Conch Key, and Key Largo. Nine more tornadoes were reported in the afternoon and evening, with four occurring near Fort Myers. Another tornado was reported 17 miles (27 km) north of Okeechobee.

Tornadoes also touched down west of Lakeland and in Palm Beach County. Early on the 19th, three tornadoes hit the Cape Kennedy-Cape Canaveral area. In Georgia, tornadoes on the afternoon of the 19th struck near Blackshear and near Douglas. Damage resulting from all these tornadoes is reported later in the section on deaths and damage.

After crossing the coastline, Agnes changed her course toward the northeast (fig. 1) and weakened to a tropical depression (surface wind speed under 39 mph, or 34 knots) by 0700 EST, June 20, when the center was at lat 32.2° N.; long 83.8° W., about 30 miles (48 km) south-southwest of Macon, Ga. (fig. 6). By this time rain directly associated with the circulation around Agnes was falling from the northern boundary of Florida to southern Virginia. With the exception of Alabama, Misissippi, and northern New England, most of the Eastern United States was covered by unstable air. Except for some decrease in Florida, precipitable water had increased over the Southeastern States and was generally above June averages.

The radiosonde observations at Cape Hatteras, N.C., for the 19th and 20th (fig. 12) show a slight warming but a large increase in moisture during the 24-hour interval between the two soundings, although the storm center was still some 500 miles (800 km) away. A shift of winds at intermediate levels from southeasterly to southwesterly brought in a flow of moist air from the gulf, increasing the precipitable water in the layer of air from the surface to 500 mb from 1.20 to 1.84 inches in the 24-hour period. This shift of winds resulted from the approach of the 700-mb Low, which was centered over southwestern Georgia at 0700 EST on the 20th (fig. 6).

Later on the 20th Agnes deepened, and her circulation accelerated as a result of the release of energy from baroclinic sources (Simpson and Hebert, 1973) associated with an extratropical trough approaching from the west (fig. 6). This stimulation, however, was not enough to raise Agnes to the tropical storm stage but very likely led to the development of a secondary Low early on the 21st.

Continuing northeastward as a tropical depression, Agnes crossed into South Carolina, and at 0100 EST on the 21st was centered at lat 33.8° N.; long 80.2° W., about 60 miles (96 km) north-northwest of Charleston (fig. 1). At this time a secondary Low center appeared at lat 35.0° N.; long 80.0° W., roughly 80 miles (129 km) north of the primary center (fig. 1). These two Low centers, which ap-﻿8

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 2.—Composite satellite photographs showing development of Agnes near East Coast of Yucatan on (A) June 15

and (B) June 16, 1972.

pear as one on the maps of figures 7 and 8, moved along fairly parallel tracks through the 22nd, when the original Agnes center was absorbed into the then dominant secondary center (Simpson and Hebert, 1973).

Travelling at a speed of 12-15 mph, the Agnes center had moved into southeastern North Carolina by 0700 EST on the 21st (fig. 7). Precipitable water amounts had increased during the preceding 24 hours to well above June averages (Reitan, 1960) ahead of the storm all the way to the Canadian border (fig. 7).

A comparison of the soundings at Sterling, Va., near Washington, D.C., for the 20th and 21st (fig. 13) shows a slight cooling in the lower layers, with some warming at upper levels. Dew-point temperatures, however, showed a great increase, with max-

imum gains being above the 550-mb level. Precipitable water increased from 1.19 to 1.43 inches. Winds above the 700-mb level had backed from southwest to southeast and were now southeasterly at all levels up to 400 mb. Wind speeds had also generally doubled.

The New York soundings for the 20th and 21st (fig. 14) showed temperature and dew point changes similar to those at Sterling, Va., with precipitable water increasing from 1.19 to 1.56 inches. However, northwesterly winds above the 700-mb level had backed to southwesterly on the 21st with little change in speed. At 0700 EST on the 21st, unstable air covered the Eastern United States from Florida to Canada, and rain was falling from the Carolinas to Canada as a result of Agnes and the northern low-pressure system.﻿STORM HISTORY

9

Figure 2.—Continued.

Continuing her northeastward movement, Agnes strengthened to a tropical storm during the afternoon of the 21st and crossed the North Carolina coastline about 1900 EST, the original center passing about 35 miles (56 km) north of Cape Hatteras (fig. 1). The pressure at Norfolk, Va., which had been falling rapidly since about 1100 EST on the 19th, reached its minimum of 985.4 mb at about 2000 EST, with the surface wind shifting from easterly to northwesterly about 2120 EST (fig. 11). At 0100 EST on the 22nd, the storm center was about 100 miles (160 km) east of Norfolk.

At 0700 EST on the 22nd, Agnes was centered at lat 38.2° N.; long 73.1° W., about 210 miles (338 km) east of Baltimore (figs. 1 and 8). It was at this time that Agnes reached the lowest recorded central pressure of her entire life, 977 mb, as deter-

mined by military reconnaissance flights. The sounding at J. F. Kennedy International Airport near New York City showed strong easterly to southeasterly winds at all levels (fig. 14), with pre-cipitable water having increased slightly from 1.56 to 1.73 inches during the preceding 24 hours.

The moist unstable air accompanying the storm as it crossed Southeastern United States (figs. 3-7) had been replaced by dry stable air (fig. 8), which had moved in behind the storm, except over the extreme southern portion, where another weather system was active. The Kennedy Airport sounding (fig. 14) was the only one indicating instability in the Northeastern United States. The high amounts of precipitable water associated with Agnes on the morning of the 22nd were limited to southern New England, southern New York, and New Jersey﻿10

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 3.—Synoptic situation at 0700 EST, June 17, 1972. Satellite photograph is a composite from several orbits. (700-m'b heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿STORM HISTORY

11

Figure 4.—Synoptic situation at 0700 EST, June 18, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿12

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

PRECIPITABLE WATER CHART

FIGURE 5.—Synoptic situation at 0700 EST, June 19, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿STORM HISTORY

13

SATELLITE PHOTOGRAPH

PRECIPITABLE WATER CHART

FIGURE 6.—Synoptic situation at 0700 EST, June 20, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water, in inches.)﻿14

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 7.—Synoptic situation at 0700 EST, June 21, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿STORM HISTORY

15

Figure 8.—Synoptic situation at 0700 EST, June 22, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿16

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

SATELLITE PHOTOGRAPH

PRECIPITABLE WATER CHART

Figure 9.—Synoptic situation at 0700 EST, June 23, 1972. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿STORM HISTORY

17

700-mb CHART

SATELLITE PHOTOGRAPH

Figure 10.—Synoptic situation at 0700 EST, June 24, 1972'. Satellite photograph is a composite from several orbits. (700-mb heights in tens of metres, surface pressure in millibars reduced to sea level, and precipitable water in inches.)﻿18

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 1.—Minimum sea-level pressure and maximum surface wind speeds at selected stations, June 18-25,1972

______Pressure (mb)__________ _____________________________ Wind (mph)

Station1	Date	Low	Time	Fastest	Time	r .	Time

(EST)	mile	(EST)	UUSCS	(EST)

Florida

Apalachicola__________________ 19

Big Pine Key _________________ 18

Crestview FAA_________________ 19

Daytona Beach WSO_____________ 19

Flamingo______________________ 18

Fort Myers WSO________________ 17

Do _______________________ 18

Jacksonville WSO______________ 19

Kennedy SC____________________ 19

Key West WSO__________________ 18

Lakeland WSO _________________ 19

Miami WSMO____________________ 18

Orlando_______________________ 18

Panama City___________________ 19

Panama City FAA ______________ 19

Pensacola FWF NAS__________	19

Pensacola WSO ________________ 19

St. Petersburg AP FAA______	19

Tallahassee WSO_______________ 19

Tampa WSO ____________________ 19

Tyndall AFB___________________ 19

West Palm Beach WSO________	18

Alabama

Dothan FAA ___________________ 20

Mobile WSO ___________________ 19

Montgomery WSO________________ 20

Georgia

Albany FAA ___________________ 20

Augusta WSO __________________ 20

Brunswick ____________________ 20

Macon WSO ____________________ 20

Savannah WSO__________________ 20

South Carolina

Beaufort MCAS ________________ 21

Charleston WSO________________ 21

Columbia WSO__________________ 21

Florence FAA _________________ 21

Greer WSO ____________________ 21

Myrtle Beach AFB _____________ 21

North Carolina

Cape Hatteras WSO_____________ 21

Charlotte WSO_________________ 21

Elizabeth City FAA____________ 21

Greensboro WSO________________ 21

New Bern FAA__________________ 21

Raleigh WSFO _________________ 21

Rocky Mount FAA_______________ 21

Wilmington WSO________________ 21

Virginia

Chesapeake L/V________________ 21

Dulles Int’l. AP______________ 21

Langley AFB __________________ 21

Norfolk WSO __________________ 21

Richmond WSO__________________ 21

Washington Nat’l. AP_______	21

Maryland

Andrews AFB __________________ 21

Assateague____________________ 22

Baltimore WSO_________________ 22

Kentmorr Marina_______________ 22

Ocean City CGS________________ 22

Patuxent NAS _________________ 21

Salisbury FAA_________________ 22

Delaware

Dover AFB ____________________ 22

Indiana River Inlet CGS____	22

Wilmington WSO _______________ 22

See footnotes at end of table.

987.1	1512	SSE 32
984.4	1556-1757	NE 39
1005.1	1656	E 29 3
		SSE 42 E 25 2
1004.1	1630	SE 25 2
		E 39
		SSE 52
1002.0	0310	SE 43
1004.4	0230	SE 33
		ESE 25
1005.1	1655	ESE 30 2 NNE 35
4 987.5	1600&1800	NE 40 2
997.0	1355-1655	NNE 35
997.3	1700	NNW 23 2
‘ 1001.7	0353-0552	S 29 2
991.2	1709	S 312
1002.0	0600	SE 27 2
985.8	1458	NE 40 2
1008.5	1632	E 32 2
990.9	2200	N 29 2
1002.0	1745	N 22 2
998.3	0200-0400	N 25
992.2	0555	ENE 17 2
992.9	1800-2000	E 24 2
998.0	1558	
995.6	1010	E 33
994.9	1800	E 37 2
992.6	0200	SE 29 2
992.2	0400	W 39
992.2	0300-0400	E 24
990.2	0400	WNW 23 2
994.9	0200	E 21
989.8	0700	WNW 29 2
986.5	1755	WNW 37 2
991.2	0400	NW 23
985.8	1758	SSE 23s
992.2	0700	NW 26
988.5	1450	SE 182
990.5	0956	N 24 2
988.2	1358	NNW 23 2
988.8	1055-1255	SE 26 W 26
986.1	2300	
991.9	1555	NNW 25 2
985.8	1855	NNW 35
985.4	2000	NW 42
986.8	1658	NW 31
989.8	1955	NW 43
990.9	1855	NNW 29 SW 20
990.2	0042	NW 37 NW 50 2
985.1	0400	W 52
986.1	2358	NNW 25 2
984.4	0256-0356	NNW 37
986.1	0355	NW 46
986.1	0500	NW 46
986.1	0807	NW 35

	E 55	0612
	SE 55	1423
1140  0958	SE 50	1200
18/2237	E 45	0312
0735  1328	SSE 56	0700
0955	SE 53	0955
0637	SE 56	0637
0330	SSE 69 3	0330
0519	E 52	0144
18/1828	SE 55	18/1816
2228	SE 36	1523
18/2013	E 41	18/1928
0200  0700-0750	NNE 44	0200
0737	NNE 49	0648
1556	NNW 43	1556
0850	S 48	1455
1757	SSE 46	1817
18/2057	SE 43	18/2048
	S 43	11/1109
0655	NE 52	0655
1632	E 46	1632
19/2157	N 43	19/2157
1457	N 35	1452
1421	N 37	19/1411
19/1156	NE 29	19/1115
19/2010	E 35	19/1957
	E 52	19/1056
19/1537	NE 35	19/1555
19/1349	E 48	19/1340
19/1941	ESE 46	19/1901
0644  22/1455	E 40	19/2234
19/2255	E 34	19/2254
1354	WNW 44	1354
20/0200	N 29	20/2156
1136	NW 46	1350
2158	WNW 62	2155
0617	NNW 26	0622
0600	SSW 35	1159
0804	NNW 30	0747
0255	W 32	1855
1256	WSW 31	22/1555
1555	NNW 35	1555
20/1038  20/1346	SE 37	20/1004

1855	N 50	1853
22/0055	NW 54	22/0058
22/0037	NW 54	22/0032
1905	NW 32	1858
2317	NW 49	2103
2230	NNW 46	0209
1100	SW 50	0800
0116	NW 39	0155
0224  0730  22/0158	NW 63	0212
	NNW 43	22/0257
0700	NW 57	0708
0928	NW 67	0918
1100	NW 50	1200
1055	WNW 51	1133﻿STORM HISTORY

19

Table 1.—Minimum sea-level pressure and maximum surface wind speeds at selected stations, June 18-25, 1972—Continued

Station 1		Pressure (mb)			Wind (mph)		
	Date	Low	Time  (EST)	Fastest  mile	Time  (EST)	Gusts	Time  (EST)
New Jersey							
Atlantic City WSO _	22	982.4	0900-1115	WNW 312	1255	W 49	1227
Trenton WSO	22	982.1	1300	SW 292	2018		
Pennsylvania							
Allentown	22	983.5	1357	NE 25 2	0929		
Harrisburg	22	987.5	1950	NW 30	1048		
Philadelphia WSFO	22	984.1	0955	W 34	1318		
New York							
J. F. Kennedy Int’l. AP WSO-	22	981.4	1451	WSW 32 2	1651	WSW 47	1712
LaGuardia Field WSO	22	981.4	1454	NE 41	0848	WSW 44	1747
New York City WSO	22	981.7	1450	NE 36	0843	NE 55	0839
Connecticut							
Hartford WSO		22	982.1	1730	S 29	1931	S 46	1923
New Haven FAA -	22	982.1	1712	SSW 29	2047	SW 40	1945
Rhode Island							
Providence	22	985.5	1559	S 26 2	1928	S 38	1923
1 Abbreviations after station name are:	AFB, Air	Force Base;	AP, Air Port;	CGS, Coast Guard	Station ; FAA, Federal	Aviation Administration ;	

FWF; Fleet Weather Facility; L/V, Light Vessel: MCAS, Marine Corps Air Station; NAS, Naval Air Station; SC, Space Center; WSFO, Weather Service Forecast Office; WSMO, Weather Service Meterological Office; WSO, Weather Service Office.	______

2	Fastest 1-minute wind speed.

3	Upper limit of recorder.

4	Altimeter setting.

Table 2.—High tides attributed to Agnes, June 18-22, 1972 1

Station name 2

_______Location____________ Tide height {ft

Lat N.	Long W. above normal)

Time (EST)/Date

Florida

Apalachicola WSO	29°45'	85-00'	6.4	1512/19
Big Pine Key	24°43'	81°23'	1.2		/18
Cedar Key __ _ . . - -	. . 29°08'	83-02'	7.0		/19
Daytona Beach WSO	29°14'	81°00'	31.7	0057/19
Flamingo	. _ . 25°50'	80°38'	2.0		/18
Fort Myers WSO	. - - 26°39'	81°52'	3.0	0830/19
Jacksonville WSO	30-24'	81°26'	2.8		/19
Key West WSO 		24°33'	81°48'	1.2	1430/18
Panama City		 30“04'	85-35'	3.4		/19
Pensacola WSO	30°24'	87°13'	1.7	0658/19
St. Petersburg FAA	. . 27“46'	82°37'	4.1		/19
Tampa	27-46'	82°37'	5.0	1115/19
Alabama				
Mobile WSO			 30°42'	88°02'	1.3	0330/19
South Carolina				
Charleston		 32°47'	79°55'	47.0		/21
Virginia				
Norfolk WSO (Sewells Point) 			36°57'	76°20'	1.2	1730/21
Maryland				
Assateague	. 	 37 57'	75 06'	4.0		/22
Ocean City CGS	38°20'	75°05'	3.0	1500/22
Delaware				
Indian River Inlet CGS		 38°37'	75°04'	1.5		/22
New Jersey				
Atlantic City WSO	39°21'	74°25'	2-3		/22
New York				
LaGuardia Field	40°48'	73°47'	32.9	1300/22
New York (Battery Park)	40°42'	74°11'	3.1	1107/22
Rhode Island				
Providence WSO	. _ 41°48'	71°24'	3.2	1700/22

1	Parts of these data were obtained from the National Hurricane Center (Simpson and Hebert, 1978) and the Environmental Data Service (De Angel is and Hodge, 1972).

2	CGS, Coast Guard Station; FAA, Federal Aviation Administration; WSO, Weather Service Office.

3	Tide above mean sea level.

4	Tide above mean low water.

A﻿20

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 2.—High tides attributed to Agnes, June 18-22, 1972 —Continued

	Location		Elevation of mark (ft above mean sea level)	Average ground elevation of site (ft above mean sea level)	Remarks
Station	LatN.	Long W.			
	High-water mark data, Florida				
Alligator Point 		 - 		29"52'	84°25'	8.3	5.0	Water mark on door at Alligator Point Marina noted 5 hours after storm passage.
Apalachicola	 	 — _ _ _	29”44'	84°59'	5.4	0.5	Water at top of curb.
Carrabelle	29°51'	84°40'	8.3	15.0	Water level on piling.
Carrabelle - - -	29°51'	84°39'	9.5	12.0	Water at top of piling.
East Point, 6 mi NE _  Florida State Route 65 and US 98, 1.4 mi	29“49'	84°51'	6.4	5.5	Water elevation about 1 ft above cattle guard.
W of junction.	29°50'	84°52'	7.4	9.0	State Trooper stated water was covering berm of Highway 98 in front of Florida Highway Patrol Station.
Panacea, 4 mi S _	29"59'	84°22'	8.4	8.0	Water reached seam on pavement of driveway entrance to motel. Verified by photograph.
St. George Island	29°42'	84°50'	7.5	7.3	Water reached bottom of beams supporting floor of building.
St. George Island	29"42'	84°50'	4.4	4.0	Water reached top first layer of concrete blocks above floor level of building. Some conflicting testimony by witness.

(fig. 8). Rain was falling over the eastern Great Lakes region, Maryland, Delaware, New Jersey, and the New England coastal areas (figs. 28 and 29). Maximum sustained surface-wind speeds along the coast from Norfolk, Va., to Providence, R.I., ranged from 25 to 45 mph (22-39 knots) with guests up to 55 mph (48 knots).

At about 0700 EST on the 22nd, Agnes began to curve toward the northwest. The storm center just tipped the west end of Long Island and moved inland in the vicinity of New York City (fig. 1). The pressure at LaGuardia Airport reached its minimum of 981.4 mb at 1454 EST (table 1), and the northeasterly surface winds veered to southwesterly about 1700 EST. At about the same time, the surface wind at Wilkes-Barre, Pa., shifted from northerly to southerly. Lowest pressure at Wilkes-Barre was 981.5 mb at about 2000 EST (fig. 11).

Sometime during the afternoon of June 22, the original weakened Agnes center was absorbed into the circulation of the now dominant extratropical Low center, which was located in western Pennsylvania at 0700 EST, the 23rd (fig. 9). This Low stagnated for some 24 hours (fig. 10) before slowly drifting northeastward. It dominated the weather in the northeastern United States for several days before passing out into the North Atlantic. Most of the heavy rain in the Middle Atlantic region attributable to Agnes, however, fell on June 21-22.

RAINFALL

The severity of the flooding associated with Agnes may be attributable in part to the wet weather that prevailed over a period of several weeks preceding the storm. Figure 15 shows that May precipitation was abnormally heavy over New York, eastern Pennsylvania, Maryland, New Jersey, and, especially Virginia, the southeastern part of which experienced monthly totals exceeding twice normal.

Precipitation for the first half of June was generally above normal in eastern New York, western and extreme eastern Pennsylvania, northern New Jersey, and southeastern Maryland (fig. 16). In Virginia, precipitation was generally below normal.

A frontal system sweeping across Eastern United States on June 15-17 brought heavy rains to parts of the northeastern region and to scattered areas of the southern Appalachian Mountain region. The satellite photographs in figures 2 and 3 show that these heavy rains were associated with the cloudiness accompanying the frontal system and were not attributable to Agnes. The surface-weather map in figure 3 shows the northern part of the front passing out to sea at 0700 EST, June 17, with the southern part and associated cloud system, as shown by the satellite photograph, trailing southwestward from southern New England to Alabama and Mississippi. At this time Agnes had not yet reached the﻿RAINFALL

21

Figure 11.—Pressure variation at selected stations along the storm track. Arrows and numbers show surface wind direction and speed in knots.

west tip of Cuba (fig. 1), and her cloud pattern was well separated from that of the frontal system.

The isohyetal chart for the 24-hour period ending at 0700 EST, June 16 (fig. 17), shows an elongated area of heavy rainfall with centers of 2 to 4 inches extending southwestward from Lake Champlain in northeastern New York to northwestern Pennsylvania. During the following 24 hours, rainfalls exceeding 1 inch were measured in an area extending southwestward from eastern Massachusetts to south-central Pennsylvania and also in southwestern Virginia, southern West Virginia, and southeastern Kentucky (fig. 18). One-inch rainfalls were measured also at scattered places near the Tennes-

see-North Carolina border (fig. 19). The only mainland rainfall attributable to Agnes up to this time occurred in extreme southern Florida, where 24-hour amounts were less than an inch.

The rains associated with the frontal system continued into the 18th. At 0700 EST of that date the dissipating stationary front extended across southeastern Virginia, the western Carolinas, and the extreme northern parts of Georgia and Alabama (fig. 4). The rainfall for the 24-hour period ending at that time extended southwestward from southern New Jersey to the southern Appalachian Mountain region (figs. 20 and 21), with maximum amounts being generally less than 1% inches.﻿22

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TEMPERATURE |°C]

TEMPERATURE |°d

Figure 12.—Upper-air soundings at Cape Hatteras, N.C., June 19-22, 1972. Arrows and numbers show wind direction and speed in knots at various heights. (T = temperature; DP = dew point; precipitahle water evaluated for layer from surface to 500 mb.)

The first heavy rainfall on the mainland produced directly by Agnes occurred on June 17-18. By 0700 EST, June 18, rain of up to about 4 inches had fallen during the preceding 24 hours over Florida south of a line between St. Petersburg and Vero Beach (fig. 21). During this day, the Agnes cloud

shield advanced so as to cover most of Florida (fig- 4).

By 0700 EST, June 19, the front had passed almost completely out to sea, except for the tail end, which dragged across New Jersey into eastern Pennsylvania (fig. 5). Precipitable water and at-

PRESSURE (MB)	PRESSURE (MB)﻿RAINFALL

23

TEMPERATURE [°C]	TEMPERATURE |°C|

Figure 13.—Upper-air soundings at Sterling, Va. (near Washington, D.C.), June 20-23, 1972. Arrows and numbers show wind direction and speed in knots at various heights. (T = temperature; DP = dew point; precipitable water evaluated for layer from surface to 500 mb.)

mospheric instability had increased generally over the Eastern United States during the preceding 24 hours. The heavy rainfall associated with this system stretched from Cape Cod, Mass., to northern New Jersey, then in a more southerly direction to southern Virginia. Twenty-four-hour rainfall amounts exceeding 4 inches were measured in south-

western Connecticut and southern Virginia (fig.

22).

Almost all this rainfall occurred during the evening of the 18th and the morning hours of the 19th and resulted from renewed activity in the frontal system. The overland part of the original front had dissipated, and a new front had formed along a﻿24

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TEMPERATURE |»C)	TEMPERATURE [°C|

Figure 14.—Upper-air soundings at New York, N.Y., June 20-23, 1972. Arrows and numbers show wind direction and speed in knots at various heights. (T = temperature; DP = dew point; precipitable water evaluated for layer from surface to 500 mb.)

squall line behind and parallel to the old one. This squall line is not shown in figure 4, but, at that time, it extended from Connecticut southwestward to extreme southeastern Kentucky. The new front had a short life, and only a remnant shows up on the surface map of figure 5.

By 0700 EST on the 19th, rainfall directly attrib-

utable to Agnes, which was still in the Gulf of Mexico (fig. 5), had spread northward into southern Georgia and southeastern Alabama. Rainfall amounts for the preceding 24-hour period ranged up to about 7 inches in the Florida Peninsula (fig. 23).

Rainfall in extreme southern New England and﻿RAINFALL

25

0	150	300 KILOMETRES

Figure 15.—Precipitation for May 1972 in percent of normal.

southeastern Pennsylvania continued, with breaks, into the 20th. At 0700 EST on that date, 24-hour amounts up to about 2 inches were measured on Cape Cod, Mass., and Long Island, N.Y. (fig. 24). At this time, Agnes was centered in Georgia (fig.^ 6) and was producing rainfall as far north as southwestern Virginia and southeastern Kentucky (fig. 24). Rainfall was heaviest along the eastern slopes of the Appalachians in these two States and in Georgia and southeastern Alabama, with 24-hour amounts up to about 6 inches in these two States (fig. 25). Except for light instability showers, rain had generally ceased over all of Florida by 0700 EST on the 20th.

The 700-millibar chart for 0700 EST, June 20 (fig. 6), showed a deep Low over the Hudson Bay region, with a trough extending southwestward across the western Great Lakes into Illinois, with a secondary Low over Lake Superior. The high pressure ridge that had extended between this low-pressure system and Agnes on preceding days (figs. 3-5) had disintegrated by this time, and the northern low-pressure system and the tropical storm now

O	150	300KIL0METRES

Figure 16.—Precipitation for June 1-15. 1972, in percent of

normal.

lay in a common, though still somewhat discontinuous, pressure trough. The surface front associated with the Canadian Low and trough extended from Canada, across eastern Wisconsin, and into central Missouri (fig. 6).

The Canadian trough continued to move eastward on the 20th, producing heavy rains over the Allegheny River basin and along the main stem of the Ohio River down to its confluence with the Kanawha River. At 0700 EST on the 21st, with Agnes centered over North Carolina, the secondary Low in the Canadian 700-mb trough was located over Michigan (fig. 7). The isohyetal chart for that same time (fig. 26) shows the extent of the 24-hour rainfall associated with this system, the greatest amount being about 8 inches on the central Pennsylvania-New York border. This rainfall is considered to be attributable to the Canadian pressure trough and associated surface-weather system because of (1) the elongated area of light rainfall between it and the heavy-rainfall area extending into south-central Pennsylvania from Agnes in North Carolina, (2) its location west of the Allgheny Mountains, and﻿26

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 17.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 16, 1972.﻿RAINFALL

27

Figure 18.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 17, 1972.﻿28

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 19.—Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 17,1972.﻿RAINFALL

29

Figure 20.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 18, 1972.﻿30

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 21.—Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 18, 1972.﻿RAINFALL

31

Figure 22.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 19, 1972.﻿32

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 23.—Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 19, 1972.﻿RAINFALL

33

Figure 24.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 20, 1972.﻿34

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 25.—Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 20,1972.﻿RAINFALL

85

Figure 26.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 21,1972.﻿36

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

(3)	the prevailing southwesterly winds at Buffalo and Pittsburgh during this period of rainfall. Agnes, however, may have been an important factor contributing to the unusual intensities associated with the Canadian system because of the circulation bringing into that system more moisture (figs. 7, 13, and 14) than might have been realized without the tropical storm. The satellite photograph of figure 7 appears to lend support to this view. It should be kept in mind, however, that the photographs are composites from several orbits during the daylight hours. The cloudiness conditions shown for the 21st in figure 7 are somewhat different from those that prevailed during the heavy rainfall that occurred during the night of the 20th to the 21st.

Figure 26 shows that Agnes rainfall was also heavy during the 24-hour period ending at 0700 EST on the 21st. Amounts exceeding 6 inches were observed in northern and southwestern Virginia and in western North Carolina. Other heavy amounts were measured in South Carolina (fig. 27), although, except for scattered instability showers, it had already stopped raining there and in the other Southeastern States.

The greatest rainfall intensities associated with Agness occurred on the 21st and 22nd, while she was moving from southeastern North Carolina to a point some 140 miles east of the Maryland coast (figs. 1 and 8), where she reached the lowest central pressure of her entire life—977 mb. The isohyetal chart for 0700 EST, June 22 (fig. 28), shows 24-hour rainfall centers exceeding 10 inches in southeastern Pennsylvania, Maryland, and northern Virginia, with some amounts exceeding 12 inches. True 24-hour maximum amounts exceeded many of the values shown on this isohyetal chart, however, because the heaviest intensities generally extended into two observational periods. The mass rainfall curves of figures 32 and 33 show the extraordinary intensities observed at selected recording-gage stations, with maximum amounts for 6, 12, 24, and 48 hours being indicated on the charts. The greatest 24-hour amount measured was the 14.8 inches in southeastern Pennsylvania at Gage RR44 in the Mahantango Creek basin (fig. 33), which is located approximately in the farthest north 10-inch center shown in figure 28. The 24-hour amount of 14.8 inches is over twice the 100-year value indicated for that location (table 3).

Maximum 6-, 12-, 24-, and 48-hour rainfall amounts are summarized in table 3 for some stations recording 24-hour amounts of 10 or more inches during the period June 21-22, when the greatest inten-

sities were experienced. For comparative purposes, the table also includes generalized point rainfall values for the 100-year return period, as read from rainfall frequency atlases (Hershfield, 1963 and Miller, 1964). Comparison of the observed amounts with the 100-year values indicates that, for the listed stations, the 6-hour amounts ranged from 97 to 128 percent of the 100-year values; the 12-hour amounts, from 125 to 192 percent; the 24-hour amounts, from 132 to 228 percent; and the 48-hour amounts, from 127 to 239 percent. Several other stations experienced 24-hour amounts equaling or exceeding 10 inches during June 21-22. These unusually heavy rainfalls may be attributed to high precipitable-water amounts and atmospheric instability, together with the approach of Agnes on the morning of the 21st (figs. 7 and 13), as rainfall tends to be heaviest in the forward part of a tropical storm. During the following 24 hours, precipitable water decreased and the atmosphere became stable (figs. 8 and 13).

By 0700 EST, June 22, it had stopped raining over the Southeastern United States south of lat 38° N., except for scattered light showers. To the north, however, rain continued into the 23rd as a result of Agnes having reentered the coast near New York City and moved into Pennsylvania (fig. 1), where she was absorbed into the extratropical Low. This resulted in a greatly deepened 700-millibar Low centered over wester Pennsylvania, which, by 0700 EST, June 23, had brought in much drier and more stable air into the flood-plagued area (figs. 9 and 13). Rainfall, however, continued to be heavy during the transition period, 0700 EST, June 22, to 0700 EST, June 23, and 24-hour amounts of 4 inches or more were experienced in southern New York, Pennsylvania, southern New Jersey, northern Delaware, and northern Maryland (fig. 29).

By 0700 EST, June 24, the low-pressure system had filled considerably (fig. 10), and drier and more stable air covered the flood area, but some instability was still evident in the vicinity of New York City (fig. 14). One- to 2-inch 24-hour rainfalls were measured in West Virginia, southwestern and northeastern Pennsylvania, New York, and southern New England, where amounts exceeded 2 inches in western Massachusetts and northwestern Connecticut (fig. 30).

The low-pressure system shown in figure 10 moved very little during the 24 hours after the morning of the 24th, but it did fill somewhat. The largest 24-hour rainfall amounts during this period occurred in southwestern and southeastern Pennsylvania, and these did not exceed 1.5 inches (fig. 31).﻿RAINFALL

37

Figure 27.—Rainfall, in inches, over southern section for 24-hour period ending 0700 EST, June 21, 1972.﻿38

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 28.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 22,1972.﻿RAINFALL

39

Figure 29.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 23, 1972.﻿40

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 30.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 24, 1972.﻿RAINFALL

41

Figure 31.—Rainfall, in inches, over northern section for 24-hour period ending 0700 EST, June 25, 1972.﻿42

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972


DATE

DATE

Figure 32.—Mass rainfall curves for three stations in Pennsylvania and one in Virginia for the period June 20-23,

1972.﻿RAINFALL

43

Figure 33. Mass rainfall curves for two stations in New York and two in Pennsylvania for the period June 20-23, 1972.﻿44

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 3.—Maximum 6-, 12-, 24-, and 48-hour rainfall amounts for some stations recording 24-hour amounts of 10 or more

inches during June 21-22, 19721

Station	Lat N.		Elevation (in feet)		Maximum	amount 2	
		Long W.		6	(Duration  12	in hours) 24	48
Maryland  Aberdeen Phillins Field (NR)3.	39°28'	76° 10'	37			10.11(7.2)	10.81(8.5)
Parkton 2SW (R)	-	39°38'	76°42'	600	6.2 (5.1)	7.7 (6.0)	10.3 (7.1)	11.9 (8.2)
Pretty Boy Dam (NR)		39°37'	76°42'	520			12.25(7.1)	
Wheaton Regional Park (NR).	39°04’	77°02'	330			10.00(7.4)	11.25(8.5)
Woodstock (NR) _ _ _		39°20'	76°52'	460				11.47(7.3)	12.67(8.4)
Pennsylvania  Harrisburg (R)	40°13'	76°51'	338	5.93(4.7)	8.37(5.6)	12.53(6.6)	15.04(7.4)
Mahantango Creek Basin,	40"36'	76°32'	1050	5.9 (4.6)	10.6 (5.5)	14.8 (6.5)	17.4 (7.3)
RR44 (R).  Mahantango Creek Basin,	40°39'	76°31'	680	5.5 (4.6)	9.5 (5.5)	13.6 (6.5)	16.0 (7.3)
RL45 (R).  Sunbury (R) _ _	40"51'	76°48'	440	5.13(4.5)	6.75(5.4)	10.30(6.3)	12.30(6.9)
York 3SSW Pumping Sta-	39°55'	76°45'	390				13.50(6.8)	14.60(7.8)
tion (NR).  Zerbey Airport (R)	40°42'	76°23'	1700	4.45(4.6)	7.40(5.6)	10.35(6.5)	12.15(7.3)
Virginia  Dulles Int’l. Airport (NR)4-	38°27’	77°57'	291	5.74(5.6)	10.32(6.6)	11.88(7.5)	12.63(8.7)
The Plains (R)	38“54'	77°45'	530	7.3 (5.8)	9.2 (6.8)	10.3 (7.8)	11.4 (8.9)

1	Other nonrecording stations very likely experienced 24-hour amounts of 10 or more inches but the heavy rainfall may have extended into two observational periods, so that the once-daily measurements were less than 10 inches. There may also have been other qualifying: recording-gage stations.

2	Amounts in parentheses are 100-year values as read from rainfall frequency atlases (Hershfield, 1963 and Miller, 1964).

3	R = recording gage. NR = nonrecording gage; true maxima probably g. eater than indicated.

4	Amounts based on 6 hourly measurements; true maxima probably greater than indicated.

The total storm rainfall over the region extending from North Carolina to New England for the period June 18-25 is shown in figure 34, with the center of maximum rainfall located near Valley View, Pa. A depth-area-duration analysis of this rainfall yielded the maximum average depths for 6 to 72 hours over areas from 100 to 20,000 square miles (51,800 km2) given in the last column of table 4. For comparative purposes this table also presents similar data for nine other tropical storms producing outstanding rainfalls over the United States east of the Mississippi River. The two Florida hurricanes of July 5-10, 1916, and September 3-7, 1950, produced the largest values shown in the table. However, if these Florida storms and that of September 10-13, 1878, in Ohio are eliminated so as to restrict the comparison to tropical storm rainfalls north of Florida and from the Appalachians to the Atlantic coast, the Agnes rainfall exceeds all others for all durations over areas of 10,000 square miles (25,000 km2) and over. This comparison serves to explain in part why the

Agnes floods were so outstanding over an extensive region.

Supplementary storm-rainfall data for New York and Pennsylvania during June 18-26, 1972, are presented in table 5. These data were obtained from field surveys by the National Weather Service, Corps of Engineers, and U.S. Geological Survey. Such surveys, often called “bucket surveys,” consist of scouring the areas suspected of having experienced unusually heavy storm rainfalls to find and check rainfall amounts caught in buckets, tubs, barrels, and so forth. Many of these observations are reported by citizens who maintain various forms of regularly available rain gages for their own interest but who do not regularly report their observations. The results are usually published by the NO A A Environmental Data Service; however, the data of table 5 were processed too late to meet the scheduled publication deadline and are presented here as a matter of record since they do not appear in any other publication.﻿RAINFALL

45

Table 4.—Maximum depth-area-duration data for major tropical storm rainfalls in theEastem United States

[Rainfall depths in inches]

			Period of heaviest rainfall (See footnote for location of rainfall centers)							
duration  (hours)	Sept.  10-13,  1878	Aug.  23-28,  1908	July  5-10,  1916	July  13-17,  1916	Sept.  13-17,  1924	Sept.  17-22,  1938	Sept.  3-7,  1950	Aug.  17-20,  1955	Aug.  19-20,  1969	June  18-25,  1972
100 square miles (259 km 2)										
6	5.8	6.4	12.8	7.2	7.7	5.0	14.0	7.6	12.9	7.1
12	10.9	8.3	15.6	12.0	11.2	6.8	26.3	10.5	21.7	10.9
24	12.1	10.8	17.3	19.3	12.9	9.5	35.2	14.6	21.7	13.7
48	14.1	13.8	19.5	21.7	13.7	13.0	38.9	18.8	21.7	16.7
72	—	15.1	20.8	22.1	14.4	15.1	40.6	19.0	—	17.4
200 square miles (518 km2)										
6	5.8	5.9		6.9	7.1	4.6	13.4	7.4	11.7	6.6
12	10.8	7.8			11.7	11.0	6.3	25.6	10.2	19.6	10.4
24	11.9	10.4			18.3	12.6	9.0	34.2	14.2	19.6	13.4
48	13.9	13.6			20.9	13.5	12.4	37.7	18.2	19.6	16.3
72		14.8	___	21.4	14.2	14.8	39.2	18.4	—	16.9
500 square miles (1,295 km2)										
6	5.6	5.3	10.5	6.4	6.2	4.1	12.5	6.8	9.8	5.9
12	10.5	7.0	13.9	11.1	10.5	5.6	24.6	9.7	16.3	9.6
24	11.5	9.9	16.6	16.6	12.1	8.3	32.7	13.4	16.3	12.8
48	13.4	13.2	18.8	19.5	12.9	11.6	36.0	17.2	16.3	15.6
72	—	14.2	19.5	20.1	13.8	14.2	37.3	17.3	—	16.1
1,000 square miles (2,590 km 2)										
6	5.3	4.7	9.6	5.9	5.5	3.7	11.4	6.2	8.1	5.3
12	10.1	6.3	13.0	10.4	9.5	5.1	22.6	9.2	13.5	8.9
24	11.0	9.5	15.9	15.0	11.5	7.7	30.2	12.4	13.5	12.3
48	12.9	12.9	18.3	18.1	12.4	11.0	33.7	16.2	13.5	14.9
72	---	13.8	18.8	18.6	13.4	13.8	34.9	16.4	—	15.3
2,000 square miles (5,180 km 2)										
6	4.9	4.2	8.4	5.1	4.8	3.3	9.4	5.4	6.3	7.6
12	9.4	5.6	11.8	9.3	8,2	4.6	17.7	8.0	10.7	8.1
24	10.4	8.8	14.6	13.3	10.7	7.2	24.8	11.2	10.9	11.5
48	12.2	12.4	17.1	16.3	11.7	10.4	28.4	14.9	10.9	14.1
72	—	13.1	17.9	16.8	12.7	13.2	29.7	15.2	— -	14.4
5,000 square miles (12,950 km 2)										
6	4.1	3.6	6.8	3.9	3.7	2.7	5.4	4.0	4.4	3.8
12	8.0	4.7	9.7	7.4	6.4	3.9	9.7	6.3	7.5	6.8
24	9.2	7.7	12.0	10.9	9.4	6.3	15.5	9.5	8.0	10.0
48	10.9	11.1	15.0	13.4	10.6	9.5	19.7	12.6	8.0	12.6
72	—	12.1	16.5	13.8	11.6	12.0	21.0	13.0	— -	13.0

10,000 square miles (25,900 km2)

6	3.5	3.0	5.2	3.0	2.8	2.3	3.3	3.1	3.3	3.2
12	6.8	4.0	7.7	5.5	5.0	3.3	6.6	5.0	5.8	5.7
24	8.1	6.6	9.8	8.6	8.1	5.7	10.6	8.0	6.3	8.7
48	9.7	9.7	13.2	10.6	9.6	8.6	14.7	10.6	6.3	11.3
72	—	11.0	15.4	11.0	10.6	10.9	16.4	10.8	—	11.8

20,000 square miles (51,800 km 2)

6	2.8	2.3	3.3	2.1	2.0	1.9		2.3 2.1		2.5
12	5.4	3.2	5.5	3.8	3.8	2.8		4.3 3.6		4.4
24	6.7	5.4	7.4	5.9	6.3	4.9		7.5 6.3		7.3
48	8.1	8.0	11.3	8.0	8.3	7.5		11.2 8.3		9.9
72	—	9.7	14.0	8.4	9.4	9.6		13.5 8.5	—	10.5
				50,000	square miles (129,500 km 2)					
6	1.9	1.4	1.9		1.2	1.4				1.6
12	3.5	2.1	2.3		2.3	2.1				2.8
24	4.6	3.7	4.7		4.0	3.7				5.1
48	5.8	5.6	8.7		6.1	5.8				7.7
72	___	7.5	11.5	—	7.5	7.3			 		—	8.6
Storm dates		Name Location of rainfall center(s)			Storm dates		Name Location of rainfall center(s)			
Sept. 10-13,	1878	— Jefferson, Ohio			Sept. 17-22,	1938	—	Buck and Barre, Mass.		
Aug. 23-28,	1908	— Vade Mecum and Monroe, N.C.			•Sept. 3-7,	1950	Easy	Yankeetown, Fla.		
July 5-10,	1916	— Bonifay,	Fla.		Aug. 17-20,	1955	Diane	Westfield, Mass.		
July 13-17,	1916	— Altapass,	N.C.		Aug. 19-20,	1969	Camile	Near Tyro, Va.		
Sept. 13-17,	1924	— Beaufort,	, N.C.		June 18-25,	1972	Agnes	Near Valley View, Pa.		﻿46

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 34.—Total storm precipitation for the period 6 p.m., June 19 through 6 p.m., June 23, 1972.﻿RAINFALL

47

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972

Location 1

Lat N.

Long W.

Rain-

fall

amounts

(in.)2

Date

Time

a.m.

or

D.m.

(EST)

Type of rain gage

Accuracy 3

Remarks

NEW YORK Allegany Co.

Alfred___

Alma (1)

42"15'	77°47'	13.52			
42°01'	78°04'	11.0	21	6	a.m.
		7.0	22	6	a.m.
		.13	26	6	a.m.

8-in. standard

Alma (2)________ 42"02'

78°03'

9.6

Standard bucket or pail.

Fair

Andover Center. Belmont (1)

42°09'	77°48'	16.0 _____________________ 4-in. circular Good

glass.

42°13'	78°02'	7.95* 22	7:30 a.m. Govt, rain gage Good

7:30 p.m.______________________________

7.95*

1.85

1.16

.22

.10

22

22

23

24

26

Belmont (2)		42°15'	77°55'	12.5+ - -	12.5-in. cylindar.	Fair
Belmont (3)		42°16'	77°56'	10.0	Tube	Fair
Belmont (4)		42°15'	77°54'	14.3 ---	Agway tube	Good
Belmont (5)		42°15'	77°54'	12.0 	 		Pot	Fair
Belvedere _	42°15'	78°04'	9.0 		5-gal. bucket	Poor
Birdsall	42°24'	77°55'	11.0		5-gal. bucket	Fair
Canseraga		42°28'	77“47'	10.5 		Glass tube	Good
Centerville	42°01'	78°15'	10.0 +	Sap bucket	Poor
Ceres	42°01'	78°16'	9.0+		9-in. pot, 14-in.	Fair-:

diameter.

Cuba (1)	42“13'	78°17'	12.0 _			Round	Poor
Cuba (2)	42°14'	78°17'	10.0 +				
Fillmore (1)	42°28'	78-07'	4.0*	21		Agway rectan-	Fair
			4.25*	26	9 a.m.	gular	
			8.25				
Fillmore (2) __	42°28'	78°07'	7.25 .			Plastic triangle.	Good
Hume (1)	42°29'	78°08'	7.5				Fair
Hume (2) 		42°29'	78°08’	7.0 .			Glass tube	Fair
Independence	42°04'	77°48'	4.00	21	6 a.m.	6-in. Taylor	
Hill.			2.00	21	Afternoon	plastic tube,	
			5.00	22	10 p.m.	1.75 in. diam-	
			1.25*	26	8 a.m.	eter, gradu-	
			12.25			ated 0-5 in.	
Obi (1) 		42°04'	78°18’	9.3 .			Official 6-in.	Good
Obi (2) __	42°04'	78°18'	7.0*	24	9 a.m.	wedge, gradu-	-
			2.13*	26	9:30 a.m.	ated one-tenth	
			9.13 .			in.	

Rain heaviest on 21st. No record 23rd-25th. Observer evacuated home 4 a.m. on the 21st. Report supposed to agree closely with Wellsville’s but doesn’t.

Rain began 6 p.m. on the 20th. Bucket overflowed 9 a.m. on the 21st. No further readings. Heavy erosion of road and adjacent topsoil.

Emptied four times in open field.

Container overflowed 12.5 in. rain.

12 in. in pot in garden in open.

8 in. plus 1 in. evaporation.

Approximately 11 in.

10 in. from the evening of the 20th to the afternoon of the 23rd plus one-half in.

10 in. overflowed.

Rain began 5 p.m. on the 20th. Pot overflowed between 9-10 a.m. on 22nd. Not reset so further precipitation lost. Pot was setting about 10 ft W of house.

On post in field.

Neighbors had gages with 10-11 in.

Observer said neighbor had garbage can in open with 8.25 in. too.

6 in. plus 1 in. (shaded by tree; possible evaporation).

Visual measurement. Exposure good.

Gage obstructed E-NE side by trees and N side by poultry house; most precipitation on open side to W.

1 Location of the nearest town, etc., by State and county.

- Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿48

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26,1972—Continued

Location 1

LatN.

Long W.

Rain-

fall

amounts

(in.)2

Date

Time

a.m.

or

p.m.

(EST)

Type of rain gage

Accuracy 8

Remarks

NEW YORK—Continued Allegany Co.—Continued

Petrolia	___ 42"05’	78°01'	7.40  3.95  4.20	21  22  23	8:05 a.m. 8 a.m. 4:45 a.m.	4-in. Agway tube, graduated one-tenth
			15.55			in.

u

Rain began 6 p.m. on the 20th. Also, plastic ice chest (11.25 in. deep, 16.5 in. long, 12 in. wide) on open porch overflowed. Time not noted.

Rts. 14 and 70___

Rt. 19A between Fillmore and Rushford.

Rts. 26 and 408_ Scio (1)________

Scio (2)

42°26'	77°44'	11.0 .			•5-gal. bucket	Fair
42”25'	78°10'	7.8 .			Gage	Poor
42°18'	78°04'	9.1 .				.Good
42°10’	77°59'	5.0	21	5:30 a.m.	5-in. Agway tube	_
		3.9	22	5 a.m.	tube one-tenth	
		5.6	23	5:30	in.	
		0.5	24	7:30 p.m.		

15.0

11.12-in. deep and 11-in. wide at top of container. 1.12 in. evaporated.

Rain began just after midnight on the 21st. Heaviest precipitation on the 21st. Fields flooded and erosion of roads. Observation point good.

42°11'

77°59' 4.36	21	6:30 a.m.	8-in. standard	E-15 form lost in flood.
5.35	22	6 a.m.		Gagehouse washed
1.40	23	6 a.m.		away. Heavy damage to
.40  11.51	24	6 a.m.		fields and crops. Observer had some entries on paper but relied on

memory for others. Actual rainfall may have been greater as observer may have forgotten to make entry.

Swain	42°29'	77°51'	10.0 .			ICA	Good	8.5 plus 1.5 in., about 10 in. total. Heaviest
								rain on the 22nd.
	42°20'	77°55'	11.5			Agway 5-in. Agway	Good	
(1).  West Almond	42°20'	77°53'	11.25 .				Good	4.5 in. 9 a.m. on the 21st.
(2).								
Cattaraugus Co.								
Portville (1) __	42-03'	78°20'	4.7	21	7 p.m.	6-in. conical	Good	Rain began 7 p.m. on the
			3.1	22	7 p.m.	shaped, grad-		20th. Heavy rain be-
			1.3	23	7 p.m.	uated one-tenth		tween 7 p.m. on the 20th
			0.3	24	7 p.m.	in.		and noon on 21st. Crop
			0.2	25	7 p.m.			loss and loss of gravel.
			0.2	26	8:30 a.m.			Fields flooded.
Portville (2) __	42°03'	78°19'	9.8  10.0			10-in. round		_ Rain began 7 p.m. on the
						plastic, grad-		20th. Measurement made
						uated one-tenth		at 8:45 a.m. on the
						in. to 2 in.,		26th. Heaviest rain be-
						five-tenths in.		tween midnight on the
						to 10 in.		20th and 5 p.m. on the 22nd. Observer had
								fields flooded, fences downed, and topsoil washed away.
Portville (3)	42°04'	78°18'	7.0*	23		6-in. Victor tube,	Poor-fair	Rain began 7 p.m. on the
			1.3	24		graduated on-		20th to the 23rd. Little
			.5*	26	7 a.m.	tenth in.		damage to obsrever.
			8.8					Gage obstructed by trees and shrubs.

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3	Accuracy is listed as reported by field surveyor.﻿FLOOD FREQUENCY

49

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

			Rain-		Time		
Location 1	Lat N.	Long W.	fall  amounts	Date	or	Type of Accuracy rain gage Accuiacy	3 Remarks
			(in.)2		(EST)		
NEW YORK—Continued							
Cayuga Co.							
Auburn	42°51'	76°35'	6.2			5-in. rectangular, Good	Exposure good.
						2-25 in. by three-fourths	
Moravis	42"44'	76°27'	6.0 .			in.  5-in. glass tube, Fair	Did not remember dis-
						graduated one-tenth in.	tribution.
New Hope	  Niles	42°48'	76°21'	6.0 .			Wedge Fair	
	42“50'	76°24'	3.0 .			Tube Poor	Does not fit in the pat-
							tern, but observer seems to keep track of rain.
Union Springs-	42°51'	76°37'	5.0 +			5-25-in. coffee Fair	Rain began on the 20th.
						can	Measurement made on the 25th.Gage may have splashed over.
Weedsport		43°07'	76a33'	5.0 _			_ 5-in. wedge Good	Rain began the evening
						1 in. by 3 in.	of the 20th. Measurement made on the evening of the 23rd.
Chemung Co.							
Elmira (1)		42°15’	76°45'	7.2 ..			4.5-in, glass tube, Fair	Lost paper on which
						graduated one-tenth in.	breakdown was written.
Elmira (2)		42°05'	76°49'	T	21	7 a.m.		
			3.30	22	7 a.m.		
			3.02	22	8 p.m.		
			6.32				
Cortland Co.							
Scott	42°45'	76°15'	5.6 .			5-in. glass tube, Poor	Did not remember dis-
						flared top and expanded scale	tribution.
Erie Co.							
East Aurora	32“46'	78°37'	4.0			Fair	
North Collins _	42°36'	78°57’	6.0 .			Plastic test Good	Rain began 2 p.m. on the
						tube	21st. On the morning of the 23rd, 5.34 was measured. Storm total
							measured on the 24th.
Genesse Co.							
Bergen	43°05'	77=57,	.15	20	7 a.m. ,	6-in wedge, Good	Open exposure.
			1.25	21	7 a.m.	graduated one-	
			1.60	22	7 a.m.	tenth in.	
			.45	23	7 a.m.		
			.15	24	7 a.m.		
			3.60				
Oakfield	43°04'	78°17'	1.4	21	7 a.m.	6-in. wedge, Good	Open exposure.
			1.5	22	7 a.m.	graduated one-	
			.3	23	7 a.m.	tenth in.	
			.2	24	7 a.m.		
			3.4				
Livingston Co.							
Avon (1) _ . _	42°55'	77045-	.02	20 _		_ 6-in. wedge, Good	Heaviest rainfall 2:30-4
			.34	21		graduated one-	p.m. on the 22nd. Ex-
			1.25	22		tenth in.	cellent exposure.
			2.60	23			
			.37	24			
			.08	25			
			4.66				
Avon (2)	42°53'	77°46'	4.5			6-in. wedge	

graduated one-tenth in.

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿50

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

Location 1	Lat N.	Long W.	Rain-  fall  amounts  (in.)2	Date	Time  a.m.  or  p.m.  (EST)	Type of rain gage	Accuracy 3	Remarks
NEW YORK—Continued								
Livingston Co.—Continued								
Conesus (1) 		42°45'	77-40'	2.5	21	7 a.m.	5-in. cone,		50 nercent loss in grape
			2.5	22	7 a.m.	graduated one-		crop due to rainfall.
			3.0	23	7 a.m.	tenth in.		
			T	24	7 a.m.			
			8.0					
Conesus (2) 		42°43'	77°40'	4.0*	22	5 a.m.	4-in. Agway,		-Rain began at 9 p.m. or
			4.5	23			graduated one-		later on the 20th. Ex-
			8.5			tenth in.		posure fair.
Cuylerville		42-47'	77°52'	1.20	10	6 a.m.	6-in. wedge,		.Exnosure good.
			.52	20	6 a.m.	graduated one-		
			1.50	21	6 a.m.	tenth in.		
			3.00	22	6 a.m.			
			.11	23	6 a.m.			
			.14	24	6 a.m.			
			6.47					
Dalton	42°33'	77°58'	9.5			Agway tube	Good	Greatest rain on the
Geneseo	42“46'	77°50'	.40	19 .		6-in. wedge,		evening of the 22nd.
			5.00*	23 .		graduated one-		
			5.40			tenth in.		
Hunt (1)		42°32'	78°00'	4.1	21	11 p.m.	4-in circular	Good	
			3.7	22	11 p.m.	tube		
			.3	23	11 p.m.			
			.2	24	11 p.m.			
			8.3					
Hunt (2)	42°33'	78°01'	8.0 i			Tube	Fair	8 in. at bottom of valley.
Leicester	42°47'	77°53'	6.5			Agway tube,		Rain began about 9 p.m.
						graduated one-		on the 20th and ended
						tenth in.		close to midnight on
								the 22nd. 700 acres of
								1,500 were under water
								from Little Beards
								Creek.
Livonia (1)	42°48'	77°40'	3.00	21		5-in. rectan-		■Station doubled some sur-
			5.00	22		gular Agway,		rounding rainfall re-
			3.00	25		graduated one-		ports. Amount possible.
						tenth in.		Creek flooded flats. Sta-
								tion located between two
								hills.
Livonia (2)	42"49'	77-40'	.20	19 .		. -5-in. Agway,		Exposure fair.
			.85	20		graduated one-		
			.00	21		tenth in.		
			1.50	22				
			2.80	23				
			.40	24				
			.15	25				
			5.90					
	42°50'	77°40'	1.00	22		5-in. rectan-	Good	
			1.30	23		gular Agway,		
			3.55	24		graduated one-		
			5.85			tenth in.		
Mt. Morris (1)-	42°42'	77°52'	.70	19	7 a.m.	6-in. wedge,		-From Dansville to Hen-
			.65	20	7 a.m.	graduated one-		rietta, 2,000 acres of
			1.50	21	7 a.m.	tenth in.		contracted crops suf-
			1.95	22	7 a.m.			fered.
			.25	23	7 a.m.			
			T	24	7 a.m.			
			5.05					
Mt. Morris (2)_	42°39'	77°52'	3.5*	21	6 p.m.	4-in. Dlastic	Poor	
			3.0*	23	6 p.m.	tube.		
			6.5					
Mt. Morris (3)_	42°38'	77°48'	3.5*	22	6 a.m.	5-in. glass	Fair	
			3.2	23	6 p.m.	tuba		
			6.7					

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿FLOOD FREQUENCY

51

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

Location 1

LatN.

Long W.

Rain-

fall

amounts

(in.)2

Date

Time

a.m.

or

p.m.

(EST)

Type of rain gage

Accuracy 3

Remarks

NEW YORK—Continued Livingston Co.—Continued

Mt. Morris (4) _	42°43'

Nunda___________ 42°34'

Portageville____	42° 34'

Springwater  42°32'

Livingston-	42° 45'

Wyoming Co. line.

Onandaga Co.

Apulia _______ 42 “52'

Camillus_______	43°02'

Fabius ________ 42°49'

Navarino (1) _	42"56'

Navarino (2) _	42°56'

Ontario Co.

Burbee Hollow _	42°43'

Canandaigua____	42° 53'

Canadice_______	42"44'

Canadice Lake _	42°43'

Gorham______ 42" 48'

77°54'	.1	20	- _ 5-in. tube	Good
	1.4	21		
	2.3	22		
	3.0	23		
	.2	24		
	•1	25		
	7.1			
77°57'	8.0 -			Fair-good

78°03'	9.0 .			4.5-in. Agway	Fair-good
				tube.	
77°35'	2.96	21	4 p.m.	Standard	Good
	2.10	22	3 p.m.	Weather	
	2.98	23	3 p.m.	Bureau	
	.08	24	4 p.m.	gage.	
	8.12				
77°57'	6.25 .			Triangle	Good

76°01'	.01	21 .		Wedge	Good
	2.70	22			
	1.20	23			
	.32	24			
	4.23				
76°21'	3.1	21 .		2.5 by 4-in. can.	Fair
	1.5	22			
	1.5	23			
	6.1				
76°02'	.01	21	7 a.m.	Tru Check	Good
	2.70	22	7 a.m.	plastic wedge	
	1.20	23	7 a.m.		
	.32	24	7 a.m.		
	4.23				
76°16'	5.2			5-in. glass tube.	Poor
76°15'	6.0			4.5-in. glass	Fair
				tube.	
77°25'	3.50	21	7 a.m.	Tru Check	
	5.00	22	7 a.m.	plastic wedge.	
	2.50	23	7 a.m.		
	1.00	24	7 a.m.		
	12.00				
77°12'	3.0*			4-in. Agway, graduated one-	
	2.3*	26			
	5.3			tenth in.	
77°32'	4.0*			4-in. Agway, graduated one-	
	2.0*				
	6.0			tenth in.	
77°34'	.07	20 .			
	1.31	21			
	2.25	22			
	3.34	23			
	.40	24			
	.10	25			
	7.47				
77°10'	3.3*				4-in. glass tube.	Fair
	2.0*				
	2.0*					

7.3

Rain began about 7-8 p.m. on the 20th and ended about midnight on the 26th.

Rain began about 7-9 p.m. on the 20th and ended about 6 p.m.-midnight on the 26th.

Exposure good.

Exposure good.

Poor exposure, tall trees nearby.

Did not remember distribution.

Exposure good.

Took two readings during storm.

Emptied once.

Did not remember dates.

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿52

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

			Rain-	Time  a.m.  or  p.m.  (EST)			
Location 1	LatN.	Long W.	. Date amounts (in.)2		Type of rain gage	Accuracy 3	Remarks

NEW YORK—Continued Ontario Co.—Continued

Granger Point _	42°40'	76°21'	2.80	21	7 a.m.	11-in. plastic	.	.Exposure good.
			2.25	22	7 a.m.	Taylor tube,		
			2.84	23	7 a.m.	4-in. diameter.		
			.54	24	7 a.m.			
			8.43					
Naples	42“35'	77°27'	11.0 .			5-in. rectan-	Fair	Rain began night of 20th.
						gular Agway.		Heaviest rain on the
								21st and 22nd.
Wine Cellar	42"37'	77°26'	4.00	21	7 a.m.	12-in. plastic		Exposure good.
Hill.			3.20	22	7 a.m.	Taylor tube		
			3.00	23	7 a.m.	4-in. diameter.		
			10.20					
Orleans Co.								
Medina	43°13'	78°24'	.0	20 .		Weather Bureau	Good	Records sent to Dr. Pack,
			T	21		gage.		Cornell Univ.
			.95	22				
			1.40	23				
			.24	24				
			.02	25				

2.56

Schuyler Co.  Mecklenburg Seneca Co.  Covert	. 42°24’ _ 42°34' 42"47'	76°45'  76-42'  76°50'  77°15'	8.2			4-in. glass tube Wedge 0.5-in. tube	Fair  Fair	
			7.5 _  2.0*  3.0*  2.0*  7.0  .09					Did not remember distribution.  Did not remember dates.
Steuben Co.	42°07'			21	7 a.m.			
			1.81	22	7 a.m.			
			1.90					
Arkport (1)	_ 42“24'	77°42'	10.5 +			5-in. Agway	Poor	5.5+ overflowed.
						tube.		
Arkport (2)	_ 42“24'	77°43'	5.54-	21	8 a.m.	5-in. Agway	Good	5.5+ in. overflowed on
			1.5	21	10:30 a.m.	tube.		the 21st. 14 in. on an-
			2.4	22	7 a.m.			other gage at airport.
			3.6	23	6:45 a.m.			
			.9	24	7 a.m.			
			13.5 +					
Arkport (3)	_ 42°24'	77°42'	10.2 ..			•5-in. Agway	Good	Rain began the night of
								the 20th and ended the
								night of the 23rd.
ArkDort (4)	. 42°24'	77°41'	11.9			Wedge	Fair	
Atlanta	_ 42°31'	77°29'	5.05	21	10 p.m.	Weather Bureau	Good	Rain began 10 p.m. on
			4.15	22	10 p.m.	gage and		the 20th and ended 6
			2.00	23	6 a.m.	USD A gage.		a.m. on the 23rd. 39-
			11.20					hr period.
Dansville _	_ 42°27'	77°35'	10.5			5-gal. bucket	Fair	Rain began 10 p.m. on
						and glass		the 20th. Measurement
						tube.		made at 7 a.m. on the
								23rd.
Ingleside	. 42“34'	77°24'	2.45	21	7 a.m.	12-in. plastic		Exposure good.
			2.90	22	7 a.m.	Taylor tube,		
			4.70	23	7 a.m.	4-in. diameter.		
			.39	24	7 a.m.			
			10.44					
Kirkwood	. 42°31'	77°28'	5.05	21	10 p.m.	8-in. standard		Exposure good.
			4.15	22	10 p.m.			
			2.00	23	10 p.m.			
			.19	24	10 p.m.			

11.39

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3	Accuracy is listed as reported by field surveyor.﻿FLOOD FREQUENCY

53

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

Location 1	Lat N.

NEW YORK—Continued Steuben Co.—Continued

Lindley ________ 42°02'

Stephens Mill _	42°24'

Wheeler ________ 42° 26'

Tompkins Co.

Fenner _________ 42°37'

North Lansing 42°37’ Howser.

Wyoming Co.

Bennington _____ 42°50'

Castile ________ 42°38'

Hermitage ______ 42°39'

Java (1) _______ 42°39'

Java (2) _______ 42°38'

Orangeville_____	42°45'

East Perry	42°45'

Center.

Pike ___________ 42° 34'

Portageville____	42°34'

Warsaw (1)____	42°47'

Warsaw (2)____	42°44'

Warsaw (3)	42°45'

Warsaw (4)____	42°44'

Yates Co.

Branehport____	42°37'

Dundee________ 42°31'

Keuka (1) ___	42°30’

Keuka (2)	42°30'

Middlesex ______ 42°43'

Long W.

Rain-

fall

amounts

(in.)2

Date

Time

a.m.

or

p.m.

(EST)

Type of rain gage

Accuracy 3

Remarks

77° 08'	2.30	22	7 a.m.

77°37'  77°20'	14.00	. .  11.00	_	Agway tube	Fair  Fair	3-day period.
76°36'	7.8 		4-in. Agway tube, 0.63-in. diameter.	Poor	3-day period. Exposure good.
76°30'	6.5 	 .	6-in. wedge	Good	From the 20th to the 251

78'° 25'	2.5*			Circular can	Fair	Time of observations un-
	1.0* .					known.
	3.5					
78°03'	7.0			Plastic gage	Good	
78°13'	6.5 _			4-in. Agway	Good	From the 20th to the 23rd.
				tube.		
78°23'	6.2			5-in. Agway	Good	Rain heaviest the evening
				tube.		of the 21st.
78° 23'	5.75			5-in. Agway	Good	
				tube.		
78°16’	9.5				Poor	Seem to high.
78°00'	6.7			5-in. Agway	Good	
				tube.		
78°09'	7.5 +			4-in. Agway	Fair	7.5+ , not more than one-
				tube.		half in. ran over.
78°04'	7.1 -			4-in. Agway	Good	7.1 in. west of Portage-
				tube.		ville; 8.1 in. in Portageville; 7.1 in. in Hunt
						lower elevation—neighbors.
78°07'	4.5			Agway tube	Good	Rain began the night of
						the 20th. Measurement made on the 23rd.
						
78°09'	5.25			Tube	Poor	Poor location of gage.
78°07'	6.0 .			6-in. tube	Good	Exposure good.
78 08'	7.00			4-in. Agway	Fair	7 in. at least.
				tube.		
77°48'	3.5*			4.5-in. gage, graduated one-	Fair	Did not remember dates.
	4.0*					
	7.5			fourth in.		
76°59'	3.8*			4-in. Agway tube, gradu-		
	3.7*					on some days during
				ated one-tenth		this period. Storm total
				in.		given as 10.6 in.
77°08'	3.0 +	21	9 a.m.	3-in. glass		Gage may have splashed
	3.0	21	8 p.m.	tube.		over.
	3.0	22	6 a.m.			
	1.5	22	6 a.m.			
	10.5 +					
77°06'	3.1*			4-in. Agway		Did not remember dates.
	3.4*			tube.		
	1.0*					
	7.5					
77°16'	4.0	21		4-in. Agway		
	3.0	22		tube.		

1.2	23

.8	24

9.0

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿54

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

			Rain- Time	
Location a	Lat. N.	Long W.	fal1 . Date or amounts „  /. p.m. Un-J (EST)	Type of rain gage
PENNSYLVANIA Bradford Co.				
Troy (1)	41°43'	76°39'	11.4 	 _	Plastic gage
Troy (2) 		41°48'	76°50'	10.2	Plastic gage
Wyalusing	41°40'	76°13’	7.5 		Straight-sided
(1).				concrete mixing vat.
Wyalusing	41°44’	76°17'	6.6 _ -	5-in. plastic
(2).				Taylor tube.
Wysox _	41°48'	76°24’	8.1 		Milk can, 12-in.

Accuracy 3

Remarks

Elk Co.

Johnsonburg

41°31'

Lake City_______	41°21'

Fayette Co. Uniontown

Lackawanna Co. Interstate 81 and Rt. 632 intersection. Luzerne Co.

Nescopec ______

39”53'

McKean Co.

Eldred (1) _

Eldred (2)

Port Allegany _	41° 47'

Northumberland Co.

Mt. Carmel___	40°48'

78°40'

78°54'

79°43'

3.05	21	6	a.m.
1.06	22	6	a.m.
3.77	23	6	a.m.
.17	24	6	a.m.
.67	25	6	a.m.
.37	26	6	a.m.

diameter, 9-in. opening.

8-in. standard

9.09 9.0 .

Straight pot

.24 .63 4.34 .90 ■ 19

21

22

23

24

25

6.30

. Gage in open area. Emptied by observer a few times.

_ Homes flooded W of town. 44 in. of water on first floors. Boy drowned on the 26th 1.5 mi below dam at Bending State Park 4 mi up Clarion River from Johnsburg.

.Readings from the 20th to the evening of the 26th. Ruler used.

41°33'	75-44'	14.2 .			Milk can, 17-in. diameter, 14-	In open undisturbed area.
					in. opening.	
41“03'	76°17'	13.8			Oval metal con-	Observer assumed this
					tainer, 8 ft by	amount covered more
					3 ft.	than 2 days.
41°58'	78°22'	5.3	21	11 a.m.	Wedge	Town suffered extensive
		3.1	22	4 p.m.		damage to business and
		0.5	23				residences. Exposure
		0.6	24				poor.
		0.5	25	11 a.m.		
		10.0				
41°58'	78°21'	3.03	21	7 a.m.	8-in. standard	
		2.19	22	7 a.m.		
		3.29	23	7 a.m.		
		.05	24	7 a.m.		
		.38	25	7 a.m.		
		.16	26	7 a.m.		
		9.10				
41°47'	78°14'	6.0			6-in. Victor tube, Fair	Rain began 6-7 D.m. on
		6.6*	21	11 a.m.	graduated one-	the 20th and ended
		12.6			tenth in.	about midnight on the 26th. Heaviest precipi-

tation between 7 p.m. on the 20th and 11 a.m. on the 21st.

76°26'

12.06 ___________________ -Standard

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.﻿FLOOD FREQUENCY

55

Table 5.—Supplementary rainfall data for Northeastern United States for June 18—26, 1972—Continued

Location 1

Lat. N. Long W.

Rain-

fal1 . Date amounts

(in.)2

Time

a.m.

or

p.m.

(EST)

Type of rain gage

Accuracy 3

Remarks

PENNSYLVANIA-	-Continued	
Schuylkill Co.		
Eisenhuth	40“48'	76°07'
Reservoir.		
New Ringold __	40°40'	75°58'
Tamaqua	40°48'	76°02'
Tioga Co.		
Gaines	41°45'	77°33'
Maimesburg	41"46'	76°58'
(1).		
Maimesburg	41°48'	76°54
(2).		
Mansfield	41°48’	77°07'
Wellsboro	41“47'	77°11'
Westmoreland Co.		
Donegal	40°07'	79°22'
Greensburg		40“14'	79°28'

Kingston

40°18’	79°21'

Latrobe (1) ..	40°18'	79°23'

Latrobe (2)	40°19'	79°23'

Mt. Pleasant

(1).

40°07'	79°30'

9.24

11.25

9.2 .

.Schuylkill Co. Water Authority

. Can in clear area.

5.18 ______________

9.4 _______________

6.5+	22 11p.m.

7.80

8.00

.16	20	11 p.m.
.96	21	11 p.m.
2.10	22	11 p.m.
4.17	23	11 p.m.
.74	24	11 p.m.
.12	25	11 p.m.
.00	26	11 p.m.
8.25		
.24	20	
.45	21	
2.00	22	
3.73	23	
.27	24	
.29	25	
6.98		
.27	20	11 p.m.
1.50	21	11 p.m.
2.00	22	11 p.m.
2.56	23	11 p.m.
.60	24	11 p.m.
.12	25	11 p.m.
.00	26	11 p.m.
7.05		
2.00	22	
3.50	23	
2.00	24	
7.50		
.50	19	6:30 a.m.
.00	20	6:30 a.m.
.40	21	6:30 a.m.
1.30	22	6:30 a.m.
4.03	23	6:30 a.m.
2.30*	26	6:30 a.m.
8.53		
.00	20	
2.00	21	
2.00	22	
5.00	23	
3.00	24	
1.50	25	
.00	26	

Glass tube, 8-in. diameter, 0.38-in. opening.

Straight-sided metal can, 15.75-in. diameter.

Wedge	____________Tall trees around gage

but open over top.

Plastic	____________Gage in clear area.

Plastic	____________Rain began 5 a.m. on the

22nd. Gage in clear area.

Plastic	____________Gage in clear area.

9-in. calibrated ________________________________________

glass gage.

________________________________3.34 in. at 11 a.m. on the

23rd.

8-in. standard

.Exposure good.

8-in. standard

.Exposure good.

5-in. Agway, graduated one-tenth in.

8-in. standard

.Exposure fair.

.Exposure poor to fair.

10-in. metal Taylor, 3-in. diameter.

. Exposure fair to good.

13.50

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3	Accuracy is listed as reported by field surveyor.﻿56

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Table 5.—Supplementary rainfall data for Northeastern United States for June 18-26, 1972—Continued

Location 1	Lat. N.	Long W.	Rain-  fall  amounts  (in.)2	Date	Time  a.m.  or  p.m.  (EST)	Type of rain gage	Accuracy3 Remarks
PENNSYLVANIA-	—Continued						
Westmoreland Co.—	-Continued						
Mt. Pleasant	40°11'	79°28'	12.+ .			13-in. 5.gal.	May have been measured
(2).						oil can, 11.13-	on the 21st. Rain con-
						in. diameter.	tinued after can em-
							ptied.
Perryopolis __	. 40“05'	79°48'	1.5*	22 .		15.5-in. can, 11-	Rain began on the 20th.
			5.0*	24		in. diameter.	Exposure good. An-
			6.5				other farmer a half mile
							down road had identi-
							cal reading.
Rector (1) __	. 40°11'	79°15'	.00	20 .		_ 8-in. standard	Exposure good.
			.21	21			
			1.11	22			
			3.85	23			
			1.25	24			
			.20	25			
			.02	26			
			6.64				
Rector (2)		_ 40°11'	79°15'	.00	20	7 a.m.	8-in. standard	. _ Exposure good.
			.20	21	7 a.m.		
			1.10	22	7 a.m.		
			4.00	23	1 p.m.		
			.63	24	7 a.m.		
			.18	25	7 a.m.		
			.00	26	7 a.m.		
			6.11				
Smock	. 39°57'	79°48'	1.0	22		4-in. Agway	On the 23rd, overflowed
			4.5 +	23		tube, 0.75-in.	at 7 a.m.
			1.0	24		diameter.	
			6.5 +				
Stahlstown		. 40°10'	79°21'	.00	20		Wedge	_ .Exposure good.
			.38	21			
			1.04	22			
			4.05	23			
			2.20	24			
			.40	25			
			.03	26			
			8.10				
Wyoming Co.							
	41°34'	76°03'	7.4			Plastic gage	
Meshoppen		41°37'	76°02'	6.1			Straight-sided	Can in open area.
						metal can, 6-	
						in. diameter.	
Mill City	41°30'	75°52'	5.7 _			Straight-sided	Bucket in oven area.
						plastic bucket,	
						10.5-in. diam-	
						eter.	
Rts. 6 and 92	41°29'	75°52'	6.0 _			1 gal. can	Road washed out a few
intersection.							miles south of here.

1	Location of the nearest town, etc., by State and county.

2	Daily amounts are generally listed. The total of these amounts at each location is omitted when one or more days of record are missing. Where

a	appears after an amount, it indicates accumulation since beginning of storm or prior measurement. In some cases, only storm totals are known.

3 Accuracy is listed as reported by field surveyor.

FLOOD FREQUENCY

Information on flood frequency is useful in the design of bridges, culverts, highways, flood-control structures, industrial plants or other buildings lying on flood plains, and in the development of criteria for land management.

Recurrence interval in this report is defined as the average number of years within which a given flood peak will be exceeded once. The recurrence

intervals are average figures based on historical data; consequently, a flood of a given recurrence interval may occur in any year, in successive years, or may not occur for a period much greater than the designated recurrence interval. Probability terms may be used to avoid any inference of regularity of occurrence. A flood with a 50-year recurrence interval would have 1 chance in 50 or a 2-percent chance of being exceeded in any given year; cor-﻿THE FLOODS

57

respondingly, a 25-year flood would have 1 chance in 25 or a 4-percent chance of being exceeded in any given year.

Flood-frequency information at gaging sites are shown in this report in table A-l. The flood frequency data shown were prepared using the methodology described by the U.S. Water Resources Council (1967). Peak flow data through 1971 were used in the frequency analysis. Flood-frequency information shown for some stations is based on regional flood-frequency analysis owing to insufficient length of record at the site. At sites where flood peaks are materially affected by regulation or diversion, flood frequency is shown only if 25 or more years of record are available during which effects of regulation or diversion on peak flows has remained virtually unchanged. Many stations experienced flood peaks whose recurrence interval was greater than 100 years. Owing to the short length of available record, frequency curves could not be reliably defined beyond the 100-year recurrence interval, therefore, stations whose peak flow exceeded the 100-year recurrence interval are shown in table A-l as >100.

The outstanding aspect of the 1972 floods was their great areal extent, resulting in record-breaking extremely rare floods on major streams. Peak flows

at some stations approached the highest ever recorded (fig. 35).

Several major streams, the Schuylkill River, the Susquehanna River and its major tributaries, the Chemung and West Branch Susquehanna Rivers, and the James River experienced peak flows having recurrence intervals in excess of 100 years throughout most of their lengths. New record highs would have been recorded throughout the length of the Allegheny River had it not been for flood storage in reservoirs.

Peak flows on many tributary streams had recurrence intervals greater than 100 years. Most gaged streams tributary to the Susquehanna River from Waverly, N.Y., to the Chesapeake Bay experienced peak flows having recurrence intervals near or greater than 100 years. This was also true of most Potomac River tributaries downstream from Point of Rocks, Md.

THE FLOODS

In this section the magnitude of floodflows in the report area is discussed. Storm precipitation and property damage are covered in other parts of the report and are not discussed here. The floods in the various river basins in the flood area are dis-

Figure 35.—Maximum discharge versus drainage area for known floods.﻿58

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

cussed briefly in the downstream order used in water-supply papers of the U.S. Geological Survey. Peak flows are described with reference to their recurrence intervals (the average number of years during which the peak discharge will be exceeded once) and by comparison with previous floods. A summary of data on flood stages and discharges is given in table A-l.

STREAMS TRIBUTARY TO LONG ISLAND SOUND

Unusually high floodflows were experienced on streams in Manchester County, N.Y., and the southeast corner of Connecticut on June 19. These high flows were caused by an intense frontal storm before the advent of Hurricane Agnes in other parts of the report area. Maximum peak flows for periods of record were recorded at most stream-gaging sites. Some of the peak discharges had recurrence intervals estimated to be greater than 100 years. Four gaging stations, with records dating back to about 1940, Blind Brook at Rye, N.Y. (site 11) ; Beaver Swamp Brook at Mamaroneck, N.Y. (site 13) ; Mamaroneck River at Mamaroneck, N.Y. (site 17) ; and Bronx River at Bronxville, N.Y. (site 19), had peak flows almost two times the magnitudes of the previously recorded maximums. Flood profile data for several streams are shown in table A-2.

DELAWARE RIVER BASIN

Severe flooding occurred in the Schuylkill River basin from the headwaters to its confluence with the Delaware River at Philadelphia. Flooding in the Delaware River basin upstream from the Schuylkill River was not unusual, and only the Schuylkill River and other right- (west-) bank tributaries to the Delaware River downstream from Philadelphia are included in the report area. Peak discharges recorded at several gaging stations indicate that recurrence intervals greater than 100 years were fairly common. The peak discharge for Schuylkill River at Berne, Pa. (site 23), was the greatest since records began in 1948, and the peak of 95,900 cfs at Pottstown, Pa. (site 28), was almost two times the maximum previously known since at least 1902. The peak stage of 29.97 feet at that site is about 9 feet higher than the previous maximum during the same period. At the gaging station at Philadelphia, Pa. (site 39), the peak discharge of

103,000	cfs was the greatest since at least 1902 but was exceeded by the historic flood of 1869. Information on flood-crest elevations along the Schuylkill River are shown in table A-3. Discharge hydrographs for the period of extreme flooding for Schuylkill River at Pottstown and Philadelphia, are shown in figure 36.

Outstanding floods also occurred on Schuylkill River tributaries, Tulpehockan Creek, French Creek, and Perkiomen Creek. There was some reduction of peak flow of Perkiomen Creek owing to flood storage in Green Lane Reservoir; however, the peak discharge at Graterford, Pa. (site 32), downstream from the reservoir was 35,800 cfs, only slightly less than the maximum for the period of record beginning in 1915.

There was no flooding of consequence on small tributary streams between the Schuylkill River and Christina River; however, record-breaking floods occurred on streams in the Christina basin (includes Brandywine Creek) in southeast Pennsylvania and Delaware. Peak discharge of White Clay Creek above Newark, Del. (site 50), was more than two times the previous maximum for the period 1953-59, 1963-72, and that of White Clay Creek near Newark, Del. (site 52), was the greatest since at

Figure 36.—Discharge hydrographs at selected gaging stations on Schuylkill River, June 21-28, 1972.﻿THE FLOODS

59

least 1932. Peaks at both sites had recurrence intervals estimated to be greater than 100 years. New maximums of record were recorded at most gaging stations in Brandywine Creek basin. The peak discharge of Brandywine Creek at Chadds Ford, Pa. (site 64), was the greatest known since at least 1912, and that for Brandywine Creek at Wilmington, Del. (site 67), was the greatest since at least 1947. Recurrence intervals at these and several other sites in the basin exceeded 100 years.

SUSQUEHANNA RIVER BASIN

The 1972 flood in the Susquehanna River basin is the greatest known as regards both areal extent and magnitude of flood flow. Only the upper reaches of the basin escaped the disasterous effects of Agnes. Flood-crest-profile data for more than 1,000 river miles in the basin are tabulated in table A-3.

SUSQUEHANNA RIVER MAIN STEM

Flooding along the Susquehanna River and its tributaries upstream from Binghamton, N.Y., was not significant. The peak discharge of 58,000 cfs recorded for the Susquehanna River at Vestal, N.Y. (site 102), has a recurrence interval of only 2 years. However, flood flows increased rapidly downstream from Vestal owing to high rates of runoff from tributary streams; the peak discharge at a gaging station near Waverly, N.Y. (site 107), was about two times that at Vestal and has a recurrence interval of 40 years.

The Susquehanna River, from the mouth of Chemung River, just upstream from the New York-Pennsylvania line, to the Chesapeake Bay in Maryland, experienced the greatest flood known since as far back as 1784. Peak flows along the entire reach have recurrence intervals greater than 100 years. Some reduction of peak flows resulted from flood storage in reservoirs on tributary streams. The estimated reduction of peak stages upstream from West Branch Susquehanna River was less than 1 foot and was between 1 and 2 feet downstream from that point. (See table A-5). For the reach between Chemung and West Branch Susquehanna Rivers, peak discharges were about 1.5 times the previous known maximums, and peak stages exceeded previous maximums by 8.4 feet at Towanda (since at least 1865), by 7.8 feet at Wilkes-Barre (since at least 1784), and by 4.8 feet at Danville (since at least 1865).

Flooding was especially severe on the Susquehanna River from Wilkes-Barre to Harrisburg. The peak flow of West Branch Susquehanna River at its confluence with Susquehanna River near Sunbury, Pa., was about 300,000 cfs, thus sustaining record

peak flows in the river downstream. At Sunbury, Pa. (site 247), the peak discharge of 620,000 cfs on the Susquehanna was 64,000 cfs more than that for the great flood of 1936, the greatest previously known since at least 1819, and the stage was 1.2 feet higher. Flood flows increased rapidly downstream as all tributary streams experienced extremely high rates of runoff. The peak discharge of 1,020,000 cfs at Harrisburg, Pa. (site 283), was 1.4 times that of 1936, which was the previous maximum since at least 1786, and the stage was 3.4 feet higher. At Marietta, Pa. (site 296), the peak stage was 3.8 feet higher than that of the 1936 flood. The greatest peak discharge determined for the Susquehanna River was 1,130,000 cfs at the short-term gaging station at Conowingo, Md. (site 302).

Discharge hydrographs at selected gaging stations on the Susquehanna River are shown in figure 37. Pictures of flooding along the Susquehanna are shown in figures 38-44.

Figure 37.—Discharge hydrographs at selected gaging stations on Susquehanna River, June 21-28, 1972.﻿60

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 38.—Susquehanna River at Wyoming, Pa. Photograph by Pennsylvania Army National Guard.

SUSQUEHANNA RIVER TRIBUTARIES

Some of the most destructive flooding occurred on the Chemung River and its principal tributaries, the Tioga, the Canisteo, and the Cohocton Rivers. Peak discharges having recurrence intervals greater than 100 years were recorded at most gaging stations in the basin, and only a few of the more unusual will be enumerated. On the main stem of the Tioga River, peak discharges were almost two times those previously known at the gaging station at Tioga, Pa. (site 113), Lindley, N.Y. (site 117), and Erwins, N.Y. (site 145), for periods of record 'beginning in 1939, 1930, and 1919, respectively, and the peak stage of Tioga was 2.3 times higher than that of the historic flood of 1889. High floodflows also occurred in the Canisteo River basin, but some reduction of peak flow was effected by flood storage

in Arkport Reservoir on Canisteo River and Almond Lake on Canaceda Creek. (See table A-5.) Even with flood storage, the peak flow of Canisteo River at West Cameron, N.Y. (site 140), exceeded the previous maximum for the period of record 1937-72 and also exceeded the historic peak of 1935.

Extreme flooding occurred throughout the Cohocton River basin. The peak discharge of Cohocton River at Avoca, N.Y. (site 150), was about four times that of the previous maximum since at least 1939, but the peak near Campbell, N.Y. (site 158), was slightly less than that of the flood of 1935. The peak flow of Mud Creek near Savana, N.Y. (site 157), a tributary to Cohocton River, was more than three times the previous maximum since at least 1939.

Flooding along the Chemung River downstream from the confluence of Tioga and Cohocton Rivers﻿THE FLOODS

61

Figure 39.—Susquehanna River at Kingston, Pa. Photograph by Pennsylvania Army National Guard.

greatly exceeded any previously known. Flood peaks moving down the two tributary streams arrived at their juncture at about the same time setting the stage for unprecedented high flows along the main stem of the Chemung River. A peak discharge of

235,000	cfs occurred near Big Flats, N.Y. (site 162). The peak discharge of 189,000 cfs recorded at Chemung, N.Y. (site 167), was about 1.5 times that of the previous maximum since at least 1904. The peak stage was about 8 feet higher than the previous maximum known.

Extreme flooding occurred on streams between Chemung and West Fork Susquehanna Rivers, except for tributary streams draining the area north of the Susquehanna River between Towanda and Wilkes-Barre, Pa., which experienced only moderate flooding. The flood peak of Towanda Creek near Monroeton, Pa. (site 170), was the greatest since at least 1914, and that for Fishing Creek near Bloomsburg, Pa. (site 189), was almost two times

the previous maximum since at least 1939. Peaks at both sites had recurrence intervals greater than 100 years.

Flooding in the West Branch Susquehanna River basin was reduced to some extent by storage in flood-control reservoirs, but the lower reaches of West Branch Susquehanna and some of its uncontrolled tributaries experienced peak flows greater than previously known. In the upper part of the basin, peak flows were generally slightly lower than those for the outstanding flood of 1936 but exceeded those of other known floods. Even with reservoir regulation, the peak discharges of West Branch Susquehanna River at Williamsport, Pa. (site 236), and Lewisburg, Pa. (site 245), exceeded those of the 1936 flood and were the greatest known since at least 1889. Without flood storage, it is estimated that peak stages would have been about 4 feet higher. (See table A-5.) The most outstanding peak flows on tributary streams occurred in the﻿62

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 40.—Susquehanna River at Wilkes-Barre, Pa. Photograph by Pennsylvania Army National Guard.

lower part of the basin. Flooding was particularly severe in the Pine Creek, Lycoming Creek, and Loyalsock Creek basins north of Williamsport, where peak flows far exceeded any previously known. At the most downstream gaging station on West Branch Susquehanna River at Lewisburg, Pa., the peak discharge of 300,000 cfs was only slightly less than that for the Susquehanna River j ust upstream from their confluence.

Extreme flooding occurred on all tributary streams between West Branch Susquehanna River and Juniata River. The peak discharge of Penns Creek, at Penns Creek, Pa. (site 249), was more than two times the previous maximum since at least 1930, and that for East Mahantango Creek near Dalmatio, Pa. (site 250), was almost seven times the previous maximum for the same period.

The stage at Dalmatio was 13 feet higher than that of the 1933 flood, the highest previously known. Wiconisco Creek at Lykens, Pa. (site 251), experienced a peak discharge of 18,700 cfs from a drainage area of 29.0 square miles, and the peak discharge of Rattling Creek near Lykens (site 252) was 13,500 cfs from 18.9 square miles.

Floodflows in the Juniata River basin, though outstanding, were generally less than those for the 1936 flood. The uncompleted dam on Raystown Branch near Huntingdon, Pa. impounded about 159,000 acre-feet of flood waters in Raystown Lake during the flood, thus reducing peak flows on Raystown Branch and on Juniata River downstream from Raystown Branch. Peak flows of the main stem of Juniata River were generally the greatest since the 1936 flood; at the most downstream gaging station at﻿THE FLOODS

63

Figure 41.—Susquehanna River at Enola, Pa. Photograph by Pennsylvania Army National Guard.

Newport, Pa. (site 274), discharge was almost as great as that of the 1936 flood and would have been greater had it not been for upstream flood storage.

There are no large streams tributary to Susquehanna River downstream from Juniata River, but extremely high rates of runoff occurred on most small tributary streams from Juniata River to Chesapeake Bay. In general, peak flows were the greatest known and have recurrence intervals greater than 100 years.

The peak discharge of Stony Creek near Dauphin, Pa. (site 278), was about five times the previous maximum known since at least 1939, and that of Yellow Breeches Creek near Camp Hill, Pa. (site 286), was about three times greater than the previously known maximum in 1915. The maximum discharge recorded for Swatara Creek at Harper Tavern, Pa. (site 288), was more than two times the previous maximum known since at least 1919,

but was exceeded by that of the historic flood of 1889. The maximum peak discharge for West Cone-wago Creek near Manchester, Pa. (site 290), was about two times that of the 1933 flood, and the maximum for Conestoga Creek at Lancaster, Pa. (site 298), was about four times greater. The 1933 flood was the greatest known since at least 1929. The 1972 peak stage for Conestoga Creek at Lancaster, Pa. was 10.5 feet higher than that in 1933.

Discharge hydrographs at selected gaging stations on Susquehanna River tributaries are shown in figure 45.

SMALL BASINS TRIBUTARY TO CHESAPEAKE BAY

Streams discussed in this section are west-bank tributaries to Chesapeake Bay in Maryland between the Susquehanna and Potomac Rivers. Consistently high rates of runoff were experienced throughout these basins with most peak flows at gaging stations﻿64

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 42.—Susquehanna River at City Island at Harrisburg, Pa. Photograph by Pennsylvania Army National Guard.

exceeding previously known maximums. Recurrence intervals for peak flow for many sites were around 100 years or more.

In the Gunpowder River basin the most outstanding flood occurred on Baisman Run. A peak discharge of 38,000 cfs was determined at the gaging station at Broodmoor, Md. (site 317), from a drainage area of 59.8 square miles. This was more than six times the maximum previously known during the period of record beginning in 1945.

Peak flows of streams in the Beck River basin were not unusual and were considerably less than those in 1971.

Record-breaking floods occurred throughout the Patapsco River basin. The peak flow of North Branch Patapsco River at Cedarhurst, Md. (site 325), was seven times the previous maximum since at least 1946, and the stage was 10.4 feet higher. A peak flow of 80,600 cfs was experienced on Patapsco River at Hollofleld, Md. (site 330). This discharge was more than four times the previous maximum

for the period of record beginning in 1949, and the peak stage was almost 12 feet higher than that of the outstanding flood of 1933. A peak discharge of 7,400 cfs from a drainage area of 5.52 square miles occurred on Dead Run at Franklintown, Md. (site 335).

Flooding in the small South River basin was insignificant.

In the Patuxent River basin flooding was quite severe upstream from the confluence of Patuxent and Little Patuxent Rivers and, to a lesser degree, along the main stem of the Patuxent River downstream to Chesapeake Bay. Flooding on tributary streams in the lower part of the basin was not unusual. The peak discharge of Patuxent River near Laurel (site 343) was more than two times the previous maximum since at least 1945, and the peak discharge of 35,400 cfs for Little Patuxent River at Savage was about six times that of the previous maximum since at least 1940. The stage was about 8 feet higher than that of the 1933 flood.﻿THE FLOODS

65

p	1 B a
	. TU7T *

	-		
	0	1NP	5P*
	EHH91		Mi
rrr r			
			
			x*lfj

Figure 43.—Susquehanna River at Harrisburg, Pa. Photograph by Pennsylvania Army National Guard.

POTOMAC RIVER BASIN

Flooding in the Potomac River basin upstream from Hancock, Md. was not unusual, and peak flows on the main stem of the Potomac River throughout its entire length were considerably less than those of previous floods. Floodflows in the lower reaches of the river were relatively greater than those upstream owing to extremely high rates of runoff from tributaries downstream from the Shenandoah River. Recurrence intervals of floods at the five gaging stations on the Potomac River, at Paw Paw, W. Va., at Hancock, Md., at Shepherdstown, W. Va., at Point of Rocks, Md., and near Washington, D.C., were determined as 5, 7, 18, 40, and 30 years, respectively, with the greater recurrence intervals in the lower reaches of the river reflecting high rates of runoff from tributaries downstream from Shenandoah River. The peak discharge of 347,000 cfs at Point of Rocks, Md. (site 437), was exceeded by the his-

toric floods of 1889 (460,000 cfs), 1936 (480,000 cfs), and 1943 (418,000 cfs). Although flooding on the main stein of the Potomac River and its principal tributary, the Shenandoah River, were not outstanding, peak flows on some of the smaller downstream tributaries were probably the most outstanding in the entire report area. Discharge hydrographs at selected gaging stations on the Potomac River are shown in figure 46.

Peak flows on the Shenandoah River were not exceptional except on a few small tributary streams. The peak discharge of 103,000 cfs at Millville, W. Va. (site 433), had a recurrence interval of 18 years and was only the fourth largest flood since 1924.

Peak flows on most north-bank Potomac River tributaries from Conococheague Creek at Fairview, Md. to Rock Creek at Washington, D.C., exceeded previously known maximums and had recurrence intervals estimated to be greater than 100 years. Conococheague Creek at Fairview, Md. (site 399),﻿66

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 44.—Susquehanna River at Steelton, Pa. Photograph by Pennsylvania Army National Guard.

experienced a peak discharge of 32,400 cfs. This is the greatest known discharge at the site and is about 1.5 times that of the flood of 1889, with a stage about 8 feet higher than the 1889 peak. In the Monocacy River basin in Maryland, the peak discharge of 22,800 cfs for Big Pipe Creek at Bruce-ville, Md. (site 441), was more than twice that of the previous maximum for the period of record beginning in 1948. The peak of 20,100 cfs for Liga-nore Creek near Frederick, Md. (site 448), was about five times the maximum for the period of record beginning in 1933. The Monocacy River at Jug Bridge near Frederick, Md. (site 449), had a peak discharge of 81,600 cfs, exceeding maximums of the floods of 1889 and 1933.

Some other long-term gaging station sites on north-bank Potomac River tributaries experiencing

outstanding peak flows were: Bennett Creek at Park Mills, Md. (site 450), about three times previous maximum since at least 1949; Seneca Creek at Dawsonville, Md. (site 963), greatest since at 1931; and Rock Creek at Sherrill Drive, Washington, D.C. (site 475), twice the previous maximum since at least 1930. The peak discharge for North Branch Rock Creek near Norbeck, Md. (site 473), was 10,100 cfs from a drainage area of only 9.73 square miles, and that for Northwest Branch Anacostia River at Norwood, Md. (site 478), was 3,750 cfs from a drainage area of 2.45 square miles. Peak discharges at other gaging stations on this stream were two to three times previous maximums for periods extending back to 1924.

Except for the Shenandoah River, extremely severe flooding occurred on most south-bank Po-﻿THE FLOODS

67

JUNE 1972

Figure 45.—Discharge hydrographs at selected gaging stations in the Susquehanna River basin, June 21-28, 1972.

Figure 46.—Discharge hydrographs at selected gaging stations on Potomac River, June 21-28, 1972.

tomac River tributaries in West Virginia and Virginia from just west of Winchester, Va., and Martinsburg, W. Va., to Alexandria and Quantico, Va., in the east. Flooding on some of the streams in this area was even more outstanding than on north-bank tributaries, with estimated recurrence intervals exceeding 100 years at many sites. The peak dis-change of 19,000 cfs on Opequon Creek near Martinsburg, W. Va. (site 402), exceeded the maximum for the period of record beginning in 1948 and was about the same as that of the 1936 flood. Flooding in the Leesburg, Herndon, Manassas, and Occoquan area west and south of Washington, D.C., was particularly severe. Peak discharge exceeding 1,000 cfs per square mile on small streams were common. Peak data for some streams in this category are tabulated below.

Report  No.		Drainage area (sq mi)	Maximum discharge  (cfs) (cfs per KCJ8) sq mi)	
455		-South Fork Broad Run near Areola, Va.	4.12	4,180	1,010
456—_	-Frying Pan Branch near Herndon, Va.	1.50	1,840	1,230
457--	-Horsepen Run at Sully Road, near Herndon, Va.	7.20	8,250	1,140
494—	-Long Beach at Vienna, Va.	1.18	1,280	1,080
505—	-Bull Run near Cathar-pin, Va.	25.8	39,400	1,530
506—	_Cub Run near Chantilly, Va.	7.13	8,300	1,160
507—	-Cain Branch near Chantilly, Va.	1.67	2,200	1,320
508—	-Flatlick Branch at Sully Road near Chantilly, Va.	5.92	6,600	1,120
510		_Big Rocky Run at Sully 6.10 Road near Centreville, Va.		7,100	1,160﻿68

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Peak flows for larger streams were equally outstanding. The peak discharge of 78,100 cfs at the gaging station on Goose Creek near Leesburg, Va. (site 452), was about twice those of the floods of 1899, 1937, and 1942. At Difficult Run near Great Falls, Va. (site 468), the peak discharge of 32,200 cfs was about five times the previous maximum for the period of record beginning in 1935. Cedar Run near Catlett, Va. (site 500), experienced a peak flow of 38,600 cfs, which is about 5.5 times the previous maximum for the period of record beginning in 1951. The stage was about 6 feet higher than that for the outstanding flood of 1942. The peak discharge of 36,000 cfs for Cub Run near Centreville, Va. (site 509), was about 16 times that experienced during 1961-72. Bull Run at Manassas, Va. (site 511), had a peak discharge of 76,100 cfs, about six times the maximum during 1951-72. The peak discharge of 56,400 cfs for Occoquan River near Manassas, Va. (site 504), greatly exceeded the maximum previously known. Figures 47 and 48 show pictures of Occoquan River at Virginia State Highway 123 bridge and at Occoquan Dam. Figures 49 and 50

show discharge hydrographs at selected gaging stations on Potomac River tributaries.

RAPPAHANNOCK RIVER AND YORK RIVER BASINS

Flooding in the Rappahannock and York River basins was less severe than in the Potomac River basin to the north or the James River basin to the south. However, peak discharges having recurrence intervals of 50 years or more did occur at some sites in the basins. Peak discharges on the main stem of the Rappahannock River were probably the third largest since at least 1908 and were exceeded only by the floods of 1937 and 1942. The Rapidan River near Culpeper, Va. (site 535), experienced a peak discharge of 55,600 cfs, the second highest since at least 1931, having a recurrence interval of about 50 years. The small stream of Harpers Run near Mor-risville, Va. (site 528), had a peak discharge of 1,900 cfs from 2.28 square miles. This peak was estimated to have a recurrence interval greater than 100 years.

In the York River basin, peak flows were generally slightly lower than those during the 1969

Figure 47.—Occoquan River at Virginia State Highway 123 bridge at Occoquan, Va., just prior to destruction of bridge.

Photographed by Paul Muse, Potomac News.﻿THE FLOODS

69

Figure 48.—Occoquan River at Occoquan Dam at Occoquan, Va. Washington Evening Star photograph.

flood. The peak flow of 23,300 cfs on North Anna River near Doswell, Va. (site 546), had a recurrence interval of about 75 years and was slightly less than that of the 1969 flood. It was the second highest since at least 1927. The flood peak of the Mattaponi River near Beulahville, Va. (site 556), exceeded that -of the 1969 flood and was the greatest since at least 1942. The peak discharge of 16,900 cfs is estimated to have a recurrence interval greater than 100 years, Outstanding peaks were also recorded for several small streams in the York River basin as follows: Bunch Creek near Boswells Tavern, Va. (site 548), 2,580 cfs, drainage area 4.37 square miles; Harris Creek near Trevilians, Va. (site 549), 2310 cfs, drainage area 3.31 square miles; and Po River near Spotsylvania, Va. (site 554), 10,900 cfs, drainage area 77.4 square miles. Recurrence interval at each of these small-stream sites is estimated to exceed 100 years.

JAMES RIVER BASIN

Some of the worst flooding in the report area was experienced in the James River basin, particularly on the main stem of the James River. Peak flows upstream from Lynchburg, Va., though outstanding, were not unprecedented. Flooding on the James River downstream from Lynchburg was the greatest known since at least 1870; peak flows were considerably greater than those for the flood of 1969, which at the time, was considered to be the flood of the century. Peak stages downstream from Lynchburg were from 3 to 4 feet higher than in 1969. Information on flood-crest elevations along the James River are shown in table A-4. The peak discharge determined at main stem gaging stations ranged from 66,300 cfs at Lick Run, Va. (site 564), drainage area 1,373 square miles, to 362,000 cfs at Car-tersville Va. (site 608), drainage area 6,257 square miles. The 1972 peak discharge at Cartersville was more than 100,000 cfs greater than that of 1969.﻿70

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 49.—Discharge hydrographs at selected gaging stations in the Potomac River basin in Maryland, June 21-28, 1972.

Although there was some attenuation of peak discharge downstream from Cartersville the maximum discharge determined at the gaging station near Richmond, Va. (site 612), was 313,000 cfs, almost

100,000	cfs more than that experienced during the 1969 flood. Figures 51 and 52 are pictures of the James River at Maiden, Va., and at Richmond near the peak of the flood showing part of the inundated area. Figure 53 shows a plot of discharge hydrographs for selected gaging stations on James River in Virginia. Estimated recurrence intervals of peak flows at gaging stations on the James River range from about 25 years at Lick Run to about 100 years at Buchanan, Va., and exceeded 100 years at sites downstream from Lynchburg, Va.

Severe flooding occurred on tributary streams in the James River headwaters in the vicinity of Covington, New Castle, and Catawba. The peak dis-

Figure 50.—Discharge hydrographs at selected gaging stations in the Potomac River basin in Virginia, June 21-24, 1972.

charge of Dunlap Creek near Covington, Va. (site 560), was the highest since at least 1929 as was that for Potts Creek near Covington, Va. (site 561). At New Castle, Va., the peak discharge for Johns Creek (site 567) was about the same as that experienced in 1935, which was the greatest since at least 1927. Peak flow for Craig Creek near Parr, Va. (site 569), was the highest since at least 1926; that for Catawba Creek at Catawba, Va. (site 570), was the greatest since at least 1944, but it was exceeded by an outstanding flood in 1936. Recurrence intervals of peak flows in this area ranged from about 50 years to more than 100 years.

Flooding on tributary streams between Buchanan and Scottsville, although extensive, were not record breaking. In contrast, floods in the Hardware, Slate, Rivanna, and Willis River basins entering James River between Scottsville and Cartersville were very﻿THE FLOODS

71

Figure 51.—James River at U.S. Highway 522 at Maiden, Va. Photograph by Virginia Dept, of Highways.

Figure 52.—James River at Mayos Bridge at Richmond, Va. Photograph by Virginia Dept, of Highways.﻿72

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Figure 53.—Discharge hydrographs at selected gaging stations on James River, June 21-28, 1972.

outstanding and were generally the greatest known. The peak discharge of 42,200 cfs for Slate River near Arvonia, Va. (site 592), is 1.5 times the previous known maximum since at least 1927 and has a recurrence interval greater than 100 years. Severe flooding was experienced throughout the Rivanna River basin with peak discharges at several sites having recurrence intervals greater than 100 years. A peak discharge of 18,000 cfs from a drainage area of only 13.6 square miles was experienced on Lynch River near Nortonsville, Va. (site 600), a tributary to Rivanna River. On Rivanna River at Palmyra, Va. (site 605), the peak discharge of 73,400 cfs was second only to that of the 1969 flood, which was the highest during the period of record beginning in 1934. The maximum stage of Willis River at Flanagan Mills, Va. (site 607), was about 6 feet higher than the previous high since at least 1927.

The Appomattox River basin upstream from Mattax, Va., experienced record breaking floods with recurrence intervals of peak flows exceeding 100 years at most gaged sites. The peak discharge of Holiday Creek near Andersonville, Va. (site 615), was 9,640 cfs from a drainage area of 8.53 square miles, more than 1,000 cfs per square mile. On the Appomattox River at Farmville, Va. (site 617), the peak flow of 33,100 cfs was about 1.5 times that of the previous maximum for the period of record beginning in 1927. Downstream from Mattoax the peak rate of runoff from tributary streams was not outstanding, and there was attenuation of peak discharge along the lower reaches of the Appomattox River. The peak flow of Appomattox River at Ma-toaca (site 621) was only 22,800 cfs or about two thirds that experienced at gaging station at Farmville.

CHOWAN RIVER AND ROANOKE RIVER BASINS

Flooding in the Chowan River basin was outstanding only in the upper Nottoway and Meherrin River basins in the vicinity of Keysville, Victoria, and Blackstone. The peak flows of Nottoway River near Burkeville, Va. (site 623), and Nottoway River near Rawlings, Va. (site 626), were slightly less than those for the 1971 flood, which were the greatest since at least 1947 and 1951, respectively. The peak discharge for North Meherrin River near Keysville, Va. (site 634), was the greatest since at least 1949. Flooding in other parts of the Chowan River basin was not significant.

Extremely high flows occurred on the Roanoke River and its tributaries upstream from Smith Mountain Lake. Record-breaking peaks were experienced at gaging stations; South Fork Roanoke River near Sbawsville, Va. (site 640), Roanoke River at Lafayette, Va. (site 641), Roanoke River at Roanoke, Va. (site 64?), Tinker Creek near Daleville, Va. (site 643), and Roanoke River at Niagara, Va. (site 644). Peak discharge at each of these sites had a recurrence interval estimated to be greater than 100 years. Records of peak flows on the three long-term gaging stations on Roanoke River above Smith Mountain Lake indicate that the 1972 flood was probably the greatest since at least 1899.

Flooding was alleviated in the Lower Roanoke River Basin below Leesville by operations of the flood-control reservoirs, Smith Mountain Lake and Leesville Lake. Operations of these two reservoirs are described in more detail in a later section entitled “Effect of Regulation.” As a result of flood storage in Smith Mountain and Leesville Lakes and﻿THE FLOODS

73

diminished tributary inflow downstream, peak flows of the Roanoke (Staunton) River were not outstanding. The peak discharge at the gaging station on. Roanoke (Staunton) River at Altavista, Va. (site 651), was reduced from 77,000 cfs to 37 300 cfs according to information furnished by U.S. Army Corps of Engineers (see table A-6). Peaks were reduced to a lesser extent downstream from this site.

Severe flooding occurred on tributary streams in an area just north of Brookneal, Va., at the gaging station on Falling River near Naruna, Va. (site 656). The peak discharge was the greatest for the period 1930-34, 1940-72 and is about 1.5 times that of the 1940 flood.

Unusually high rates of runoff also occurred in the Dan River basin upstream from Smith River. The peak flow at several gaging stations exceeded previously recorded maximums. The peak flow of 54,200 cfs on Dan River near Wentworth, N.C. (site 671), was about 1.5 times the previous maximum for the period of record beginning in 1940 but was exceeded by the flood of 1908. The peak discharge of Mayo River near Price, N.C. (site 669), was slightly less than that of the 1937 flood and was the second highest since at least 1930. Flood storage in Philpot Lake on Smith River reduced what would have been near record-breaking peaks on that stream to only moderate flooding. Some reduction of peak flows on Dan River downstream from Smith River was also affected. Even with flood storage in Philpot Lake, the peak discharge of 64,800 cfs for Dan River at Paces, Va. (site 682), was the greatest since at least 1951 and the peak stage exceeded that of the 1940 flood by about 1 foot.

Flood flows in the remainder of the Roanoke basin were not outstanding. Flood storage in John H. Kerr Reservoir effectively controlled flows in the Roanoke River downstream from the reservoir. A computed peak inflow of 141,000 cfs into the reservoir was reduced to 25,200 cfs peak outflow.

OHIO RIVER BASIN

Although considerable flooding occurred along the main stem of the Ohio River, peak flows were reduced considerably by flood storage in Allegheny Reservoir on the Allegheny River and many flood control reservoirs on tributary streams (see table A-7). At Sewickley, Pa. (site 842) , the peak stage was 10.3 lower than that of 1936, the previous maximum since at least 1934. At St. Marys, W. Va. (site 843), the peak stage was 8.2 feet lower than the 1943 flood (greatest since at least 1939) and 15.7

feet lower than the historic flood of 1913, which was the greatest since at least 1884. At Huntington, W. Va. (site 873), the most downstream point for which records are included in this report, the 1972 peak stage was 26.4 feet lower than that for the great flood of 1937.

In addition to the data shown for the main stem Ohio River, flood data for the Allegheny River basin, Monongahela River basin, and the Kanawha River basin are contained in this report. Discharge hydrographs at selected gaging stations in the Ohio River basin are shown in figure 54.

ALLEGHENY RIVER BASIN

The upper Allegheny River and its tributary streams in New York and Pennsylvania experienced record breaking floods following the Hurricane Agnes storm. The peak discharge of 3,000 cfs for Newell Creek near Port Allegheny, Pa. (site 701), was about four times the previous maximum since at least 1960. At Allegheny River at Elrod, Pa. (site 704), the peak discharge of 65,400 cfs was the greatest since at least 1940, and the peak discharge of

JUNE 1972

Figure 54.—Discharge hydrographs at selected gaging stations in the Ohio River basin, June 21-30, 1972.﻿74

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

73,000	cfs recorded for Allegheny River at Salamanca, N.Y. (site 709), was about 1.5 times the previous maximum since at least 1904.

The Allegheny Reservoir greatly reduced peak flows downstream. At the gaging station on Allegheny River at Warren, Pa. (site 712), the U.S. Corps of Engineers estimated the peak flow under natural conditions would have been about 94,000 cfs, about 1.5 times the previous maximum since at least 1936. The regulated peak flow was only 25,000 cfs and occurred June 28, about 5 days after the peak reservoir inflow. Comparable reduction in peak flows were effected at other points along the Allegheny River between Allegheny Reservoir and its confluence with the Monongahela River. This reduction was caused by flood storage in numerous reservoirs on tributary streams as well as that in Allegheny Reservoir (see table A-7). Had it not 'been for flood storage in the basin during the storm, record peak flows would have been experienced throughout the length of the Allegheny River; however, with storage, only moderate flooding was experienced on the main stem downstream from Warren, Pa.

Outstanding and, in some cases, record-breaking floods occurred on unregulated tributary streams in the entire Allegheny River basin. Even with regulation by West Branch Clarion River Lake, the peak flow of 53,300 cfs for Clarion River at Cooksburg, Pa. (site 745), was only slightly less than the previous maximum since at least 1935, and the peak flow of 74,500 cfs for Clarion River near Piney, Pa. (site 746), was about 1.5 times the previous maximum for the same period. Record peaks were experienced at long-term gaging stations on Mahoning Creek at Punxsutawney, Pa. (site 751), and Little Mahoning Creek at McCormick, Pa. (site 752), with periods of record beginning in 1936 and 1940, respectively. The peak discharge of 13,200 cfs for Crooked Creek at Idaho, Pa. (site 756), was the greatest for the period of record beginning in 1937 and was only slightly less than that for the historic flood of 1936.

Outstanding flood flows occurred in the upper reaches of the Kiskiminetas River upstream from Conemaugh River Lake and Loyalhanna Lake. Peak discharges for Blacklick Creek at Josephine, Pa. (site 763), and Two Lick Creek at Graceton, Pa. (site 768), were about two times that for the previous maximums since at least 1952. Peak flows on the upper Loyalhanna Creek were also outstanding. On the lower Kiskiminetas River, peak flows were greatly reduced by flood storage in upstream reservoirs.

MONONGAHELA RIVER BASIN

In general the flooding in the Monongahela River basin was not as severe as that in the Allegheny River basin. In the upper reaches of the basin, flood flows were outstanding only in the Tygert Valley River drainage. The peak flow of 15,800 cfs recorded at gaging station on Tygert River at Belington, W. Va. (site 782), was slightly less than that of 1967, which was the greatest since the flood of 1912. The peak flow of Middle Fork River at Audra, W. Va. (site 783), was the greatest since at least 1943, and that for Tygert Valley River at Philippi, W. Va. (site 788), was only slightly less than the previous maximum for the period of record beginning in 1940. Flooding in the West Fork River basin was insignificant; that in the Cheat River basin, although severe in some areas, was not record breaking. High flows were experienced, however, on Deckers Creek (site 800) and Corbun Creek (site 799) at Morgantown, W. Va., with peak discharges having recurrence intervals of about 50 years.

Flooding along the main stem of the Monongahela River was severe but considerably reduced by flood storage in upstream reservoirs. Peaks were considerably less than those experienced in 1967.

Flooding in the Youghiogheny River basin, principal tributary to the Monongahela River was not noteworthy except in the lower reaches of the main stem, where peak flows approached those of previously experienced maximums. The peak discharge of Youghiogheny River at Suttersville, Pa. (site 838), was 83,000 cfs, as compared with the previous maximum of 108,000 cfs in 1954 for the period of record 1921-72.

KANAWA RIVER BASIN

Only about one thind of the Kanawha River basin is in the area covered by this report. The Greenbrier River, the Gauley River above Sommersville Dam, and the Elk River above Sutton Dam are included. This basin is in a fringe area in regards to high rates of runoff, and flooding was noteworthy only in scattered localities. The most outstanding floods in the basin occurred on east bank tributaries of the Greenbrier River in the vicinity of Anthony and White Sulphur Springs, W. Va. High peak flows were recorded on Anthony Creek near Anthony (site 853), Dry Fork at White Sulphur Springs (site 854), Howard Creek at Caldwell (site 855), and Second Creek near Second Creek (site 856). Peak discharge at each of these sites was a maximum for the period of record. Records for only site 856 extended back as far as 1946.﻿SEDIMENTATION

75

STREAMS TRIBUTARY TO LAKE ERIE AND LAKE ONTARIO

That part of the Lake Erie and Lake Ontario drainage systems in which significant flooding occurred lies between Buffalo, N.Y., in the west and Rome, N.Y., in the east and is entirely within the State of New York. Data for only a few Lake Erie tributaries south and east of Buffalo are included in the report. Within that general area, the most severe flooding occurred in the upper Chautauqua Creek basin. A peak flow of 7,730 cfs was measured for Chautauqua Creek at Barcelona, N.Y. (site 874), from a drainage area of 36.0 square miles, with an estimated recurrence interval greater than 100 years. Near record flows for period of record extending back to about 1940 were also experienced on Buffalo Creek at Gardenville, N.Y. (site 881), and Cazenovia Creek at Ebenezer, N.Y. (site 883). The peak flow of 8,800 cfs for Cayuga River near Lancaster, N.Y. (site 882), was the greatest since at least 1939.

There was no significant flooding on the Niagara River tributaries nor on Lake Ontario tributaries between the Niagara River and the Genesee River; data for this area is not included in this report. Flooding in the Genesee River basin upstream from Mount Morris Lake was extreme, and most peak flows had recurrence intervals estimated to be greater than 100 years. Peak flows on tributary streams were generally greater than any previously known. A few of the more outstanding peak flows determined are: Fullmer Valley Creek near Halls-port, N.Y. (site 889), 3,200 cfs (drainage area 11.8 square miles), Chenunda Creek at Stannards, N.Y. (site 891), 9,200 cfs (drainage area 30.6 square miles), and Indian Creek near Andover, N.Y. (site 896), 929 cfs (drainage area 1.07 square miles). At the long-term gaging station on the Genesee River at Scio, N.Y. (site 900), the recorded peak discharge of 41,000 cfs was almost two times the previous maximum for the period of record beginning in 1917, and the peak discharge of 90,000 cfs recorded on the Genesee River at Portageville, N.Y. (site 913), was about two times the previously experienced peak since at least 1909. The peak stage of 35.25 feet at Portageville was 12.3 feet higher than for the 1967 flood, which was the highest previously known. A discharge hydrograph for Genesee River at Portageville is shown in figure 55. Flood storage in Mount Morris Lake, (site 914) prevented what would have been a disastrous flood along the lower reaches of the Genesee River. Water stored in the lake increased from about 7 260 acre feet (elev. 603.1 feet) on June 20 to 322,600 acre feet

Figure 55.—Discharge hydrographs of Genesee River at Portageville, N.Y., June 21-28, 1972.

(elev. 755.46 ft) June 25, or an increase of about

315,000	acre feet and a rise in lake level of more than 152 feet. The peak lake level was about 36 feet higher than the previous maximum since the reservoir was completed in 1951. Flooding on Genesee River tributaries downstream from Mount Morris Lake, though not as extreme as that experienced on upstream tributaries, was still severe. Even though peak flows on the lower Genesee River were greatly reduced, the peak discharge of 29,600 cfs (gage height, 15.89 ft) at Rochester, N.Y. (site 933), is only slightly lower than that of the 1942 flood, 34,400 cfs (gage height, 17.08 ft), which was the maximum since the flood of 1927.

Flooding upstream from Cayuga Lake in the vicinity of Ithaca was noteworthy, and peak flows on streams were the greatest known, some having recurrence intervals estimated to be greater than 100 years. The peak discharge of 4,800 cfs for﻿76

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Cayuga Inlet near Ithaca, N.Y. (site 947), was the greatest since at least 1937, and the peak flow of 11,800 cfs at a downstream gaging station in Ithaca (site 949) was outstanding. Peak discharge of Canandaigua outlet at Chapin, N.Y. (site 963), was the greatest since at least 1940; that of Flint Creek at Potter, N.Y. (site 964), was more than five times the previous maximum since 1964. Outstanding flooding also occurred in the vicinity of Lake Owasco and Lake Skaneateles. The peak flow of Owasco outlet near Auburn, N.Y. (site 969), was the greatest since at least 1913, with a recurrence interval estimated to be greater than 100 years. Peak flows from Seneca River at Baldwinsville, N.Y. (site 971), and Onondaga Creek at Darwin, N.Y. (site 973), exceeded previously recorded maximums for periods beginning in 1950 and 1952, respectively. Severe flooding also occurred both upstream and downstream from Oneida Lake, with the peak flow of East Branch Fish Creek at Talberg, N.Y. (site 981), being the greatest since at least 1924.

Records of lake elevations have been collected for 10 natural lakes in that part of Lake Ontario drainage in the report area. During the 1972 flood, maximum elevations for periods of record were recorded at nine of these lakes, and the maximum elevation of the remaining lake, Owasco Lake near Auburn, was virtually the same as the previous maximum for the period of record beginning in 1912.

SEDIMENTATION

The extremely high floods on most streams caused widespread movement and deposition of sediment. Sediment yield, especially on the large streams, was unusually high owing to the widespread flooding.

Erosion and deposition, physical processes related to sedimentation, contributed significantly to the damage. Wyoming Valley near Wilkes-Barre and Harrisburg, both on the Susquehanna River, suffered heavy damage from sedimentation. Dramatic evidence of the erosive capability of a large stream is shown in figure 56.

Figure 56.—Erosion on flood plain of Susquehanna River at Old Fort, Pa. Photograph by Media Affiliates, Inc. Wilkes-

Barre, Pa.﻿FLOOD-CREST ELEVATIONS

77

Damage by erosion was not confined to natural or undeveloped areas. Developed areas were also ravaged by the high flows, as can be seen in figure 57.

Overbank areas, natural and developed, bordering on the major streams experienced deposition. Extensive amounts of sand, silt, and mud were deposited in these areas. A typical example of such a deposition can be seen in figure 58. The sediment particles deposited on the flood plains were generally sand-grain size or finer.

The Schuylkill River at Manayunk, Philadelphia, Pa., Susquehanna River at Harrisburg, Pa., and Potomac River near Point of Rocks, Md., for flood periods of June 22-27, 21-30, and 21-26, respectively, carried a combined total of 9,649,000 tons of sediment. This amount of sediment is equivalent to approximately 0.5 inch of soil from a 200-square-mile area. The Susquehanna River carried the most sediment—by virtue of having the largest drainage basin. During the specified flood periods, the Susquehanna and Schuylkill Rivers transported ap-

proximately three times their average annual sediment load, while the Potomac River transported 1.5 times its average annual load. The normal sediment load for a 3-year period at Harrisburg on the Susquehanna River and at Philadelphia on the Schuylkill River was exceeded in 10 days and 6 days, respectively, while 1.5 times the normal annual sediment load was carried past Point of Rocks in 6 days.

Conestoga Creek at Lancaster, Pa., experienced the highest runoff and sediment load per square mile of any other major stream, followed, in decreasing order, by the Schuylkill, Susquehanna, and Potomac Rivers. The extremely high sediment yield per square mile shown for Stave Run near Reston, Va., reflects the extensive urban development in progress in the basin immediately preceding the flood. The Schuylkill River was the muddiest, transporting, on the average, 3.10 tons/cfs-day, while the Susquehanna River transported 1.76 tons/cfs-day and the Potomac River, 1.46 tons/cfs-day.

Data on water and sediment discharge for the Susquehanna River at Harrisburg, Pa., during June

Figure 57.—Road washout in Shickshinny, Pa. Photograph by Media Affiliates, Inc., Wilkes-Barre, Pa.﻿78

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

21-30 are shown in figure 59. The data show that well-defined suspended-sediment-concentration peaks were experienced at Harrisburg, with the maximum peak concentration preceding the peak stage. The maximum suspended-sand concentration was well defined and preceded the maximum stage experience by more than 24 hours.

Sediment data collected during the flood period are summarized in table A-8.

FLOOD-CREST ELEVATIONS

Information on flood-crest elevations was obtained for about 1,290 stream miles in the flood area. About 1,030 miles of the profile data are for streams in the Susquehanna River basin.

These data include maximum stages recorded or observed at gaging stations, as well as many high-water elevations determined from field surveys made after the flood crest. The streams for which data were obtained are listed below in downstream order.

Streams tributary to Long Island Sound East Branch Byram River Blind Brook

Mamaroneck River Sheldrake River Hutchinson River Hudson River basin Sawmill River Delaware River basin Schuylkill River Susquehanna River basin Susquehanna River Tioga River (head of Chemung River) Canisteo River Cohocton River Chemung River Seeley Creek

West Branch Susquehanna River Penns Creek

Middle Creek Mahoney Creek East Mahantango Creek Pine Creek Wiconisco River Rattling Creek Juniata River Sherman Creek Conodoguinet Creek Paxton Creek Yellow Breeches Creek Mountain Creek Swatara Creek

Little Swatara Creek West Canewago Creek Codorus Creek Conestoga Creek Pequa Creek Muddy Creek

Figure

58.—Deposition on

farmland bordering Susquehanna River near Exeter, Pa. Photograph by Media Affiliates Inc Wilkes-Barre. Pa.	’	’’﻿EFFECT OF REGULATION

79

X

o

LxJ

X

LU

O

<

o

Figure 59.—Graph of water and sediment discharge, Susquehanna River at Harrisburg, Pa., June 21-30, 1972.

Potomac River basin

Conococheague Creek West Branch Monocacy River James River basin James River Allegheny River basin Allegheny River

Flood-crest elevations for streams tributary to Long Island Sound and for Sawmill Creek in the Hudson River basin are listed in table A-2. Flood crests in this area occurred June 19 and were caused by a frontal storm which struck just prior to Hurricane Agnes, which caused flooding in the rest of the area covered by this report.

Profile data for James River in Virginia are listed for the floods of 1936 and 1969, as well as for the 1972 flood. The 1972 flood was considerably higher than the earlier floods in the lower part of the basin. Profile data for James River are shown in table A-4.

Flood-crest data for streams other than those listed above are included in table A-3. Flood crests on streams listed in this table occurred during June 22-24, and the date of occurrence is shown when known, or it can be estimated from the time of occurrence recorded at gaging stations for other points along the streams.

EFFECT OF REGULATION

Reservoir storage during the flood period substantially reduced the magnitude of peak flows in some basins. In other basins the effect of regulation was not significant. Storage was supplied by reservoirs primarily designed for flood control as well as those constructed for water supply or hydroelectric-power generation. Some of the effects of regulation were briefly discussed in a previous section describing the floods. The effect of regulation on peak flow is discussed in the following sections for those basins where the effect is probably significant. Data presented in this report are adapted from information furnished by the U.S. Army Corps of Engineers.

SUSQUEHANNA RIVER BASIN

Peak flows of the Susquehanna River upstream from the Chemung River were only slightly reduced owing to the operation of flood-control structures on the Ouleout Creek and Otselic River. Natural runoff in the Susequehanna River basin above Wav-erly was relatively light, as compared to that downstream.﻿80

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Peak flows on the upper Canisteo River in the Chemung River basin, in the reach from Hornell to Canisteo, were materially reduced by storage in Arkport Reservoir and Almond Lake. However, the effect on peak reduction rapidly diminished downstream as a result of extremely high flows from unregulated tributary streams, and peak reduction was not significant downstream from the confluence of the Canisteo and Tioga Rivers.

Reservoir storage in the West Branch Susquehanna River basin significantly reduced peak flows on the main stem of the river from Curwensville Reservoir near Curwensville to its confluence with the Susquehanna River. Peak flows were also reduced on the following tributary streams: First Fork Sinnemahoning Creek and Sinnemahoning Creek (First Fork Sinnemahoning Creek Reservoir), Kettle Creek (Kettle Creek Lake), and Bald Eagle Creek (Foster Joseph Sayers Lake). The stage reduction on West Branch Susquehanna River ranged from about 7 feet just downstream from Curwensville Reservoir to about 4 feet near its confluence with Susquehanna River.

Construction of Raystown Dam on Raystown Branch Juniata River was not complete at the time Hurricane Agnes struck, but storage above the dam caused a considerable reduction in peak flows on Raystown Branch and on the Juniata River downstream from Raystown Branch. The estimated peak-stage reduction on Juniata River ranged from 4.6 feet at Mapelton Depot, Pa., to 3.3 feet at Newport, Pa.

Estimated stage reduction on the main-stem Susquehanna River was less than 1 foot upstream from West Branch Susquehanna and between 1 and 2 feet downstream.

Effects of reservoir storage in the Susquehanna River basin are summarized in table A-5. This table lists the major reservoirs in the basin, shows the available storage at the beginning of the storm, the amount of water stored during the storm, and peak inflow, if determined. The reduction of peak stage and discharge are shown for selected points downstream from the reservoirs. The report numbers listed are the same as those used to identify the site descriptions in a later section entitled “Streamflow Data.” These numbers are also used to identify the location of sites shown on plate 1.

SMALL BASINS TRIBUTARY TO CHESAPEAKE BAY

Reservoirs in the area, although designed for municipal water supply for Baltimore, Md., and suburban Washington, D.C., did store water during

the storm and consequently caused some reduction of peak flows on streams below these reservoirs. The storage space used during the flood in 5 water-supply reservoirs in the area are as follows.

Report

No.

Name and location of reservoir

Storage space used (acre-ft)

311_____Pretty Boy Reservoir on Gunpowder Falls 7,600

near Hereford, Md.

318_____Loch Raven Reservoir on Gunpowder Falls 21,900

near Carney, Md.

326_____Liberty Reservoir on North Branch Pa- 19,000

tapsco River near Marriottsville, Md.

341	___Triadelphia Lake on Patuxent River near 5,500

Laurel, Md.

342	___T. Howard Duckett Reservoir near Laurel, 4,600

Md.

ROANOKE RIVER BASIN

Storage of floodwaters in four major reservoirs in the Roanoke River basin in Virginia was effective in reducing peak flows for the June-July 1972 flood. Smith Mountain Lake and Leesville Lake on the Roanoke River reduced peak flows of the Roanoke River from Leesville Dam to John H. Kerr Reservoir. Reduction in stage in this reach ranged from about 9 feet at Altavista, Va., to about 4 feet at Randolph, Va.

Peak flows along the Smith River in Virginia and North Carolina were substantially reduced by flood storage in Philpott Lake on Smith River. The reduction in stage ranged from more than 9 feet at Bassett, Va., to about 3 feet at Eden, N.C. Flood flows on the Dan River downstream from Smith River were reduced to a lesser degree. Reduction in stage along the Dan River ranged from about 3 feet at its confluence with Smith River to less than a foot at the upper end of John H. Kerr Reservoir.

Floodflows from John H. Kerr Reservoir were completely controlled by storage in the reservoir. The peak inflow to the reservoir was computed as 141,-000 cfs. The maximum average daily reservoir release was 25,200 cfs and occurred after flood peaks from downstream tributary streams had passed.

The effect of reservoir storage in the basin is summarized in table A-6.

OHIO RIVER BASIN

Three subbasins of the Ohio River drainage system—the Allegheny River basin, the Monongahela River basin, and the Kanawha River basin—are within the report area. Reservoir storage in the Allegheny and Monongahela River basins caused considerable reduction of peak flows on these streams as well as on the main stem of the Ohio River downstream from their confluence.﻿STREAMFLOW DATA AT GAGING STATIONS AND MISCELLANEOUS SITES

81

The Allegheny Reservoir on the Allegheny River stored about 526,000 acre-ft of water during June 20-27 and completely controlled flood flows at that point. A maximum inflow to the reservoir of 88,000 cfs on June 23 was computed with the maximum outflow of 25,000 cfs occurring June 27.

Reservoir storage on tributary streams also contributed to the reduction of peak flows. In addition to the Allegheny Reservoir, there are seven other flood-control reservoirs in the Allegheny River basin that contributed significantly to peak-flow reduction. These reservoirs are listed in table A-7. At the beginning of the storm, space for storage of 1,292,-010 acre-ft of water was available in the Allegheny Reservoir and the 7 flood-control reservoirs on tributary streams. Of the available storage space, 1,051,-640 acre-ft, or about 81 percent of that available, was used to store floodwater. Peak flows on the Allegheny River were reduced from what would been record stages and discharges to moderate flooding.

Conemaugh River Lake, the second largest reservoir in the Allegheny River basin, stored 233,150 acre-ft of water and reduced the computed inflow of 99,100 cfs to an outflow of 25,900 cfs. Storage in this reservoir contributed significantly to peak reduction on the Allegheny and Ohio Rivers.

Flood storage in the Monongahela River basin contributed to a lesser degree to reduction of peak flows. Tygart Lake on Tygart Valley River and Youghiogheny River Lake on Youghiogheny River are the largest reservoirs in the basin, but only Tygart Lake had an appreciable effect on peak-flow reduction. The computed peak inflow to Tygart Lake was 52,000 cfs and the peak outflow was 16,800 cfs. The reduction of peak discharge on the Monongahela River at Greensboro, Pa., was estimated to be about 35,000 cfs, and that at Charleroi, Pa., to be about 42,000 cfs. Peak runoff from the area above Deep Creek Reservoir (hydro-electric storage) and Youghiogheny River Lake was not great; consequently, storage in these reservoirs did not significantly affect peak flows farther downstream.

Reservoir storage, mostly in the Alleghney River basin, reduced peak flows in the Ohio River main stem significantly. Peak-discharge reduction ranged from about 224,000 cfs at Sewickley, Pa., to about

155,000	cfs at Huntington W. Va. The peak stage was reduced by about 11 feet at Sewickley and about 10 feet at Huntington. Without reservoir storage the flood of 1972 at Sewickley would have been the greatest since at least 1934. With storage, the flood was only the third highest during this period.

The effect of reservoir storage in the Ohio River basin is summarized in table A-7.

STREAMS TRIBUTARY TO LAKE ONTARIO

Flood storage in Mount Morris Lake near Mount Morris, N.Y., virtually controlled flood flows at the reservoir outlet and prevented disastrous flooding on the Genesee River downstream from Mount Morris. The peak discharge of 90,000 cfs at a gaging station on the Genesee River at Portageville was about twice the previous maximium since at least 1909, whereas, downstream from the reservoir, the peak discharge of 17,800 cfs recorded at Avon, N.Y., was only about one-third of that of the flood of 1916. A large part of the 17,800 cfs was contributed by Canaseraga Creek which enters Genesee River downstream from Mount Morris Lake. The peak discharge of the Genesee River at Rochester, N.Y., was only about half the previous known maximum.

Natural storage in numerous lakes on streams tributary to Lake Ontario moderated the magnitude of peak flows downstream from these lakes.

DETERMINATION OF FLOOD DISCHARGE

The discharge at a gaging station is usually determined from a stage-discharge relation (rating curve) defined by current-meter measurements at various stages. The reliability of the stage-discharge relation is dependent on how well the experienced range in stage is covered by current-meter measurements. Fairly reliable extensions of rating curves to about twice the measured discharge can generally be made by logarithmic plotting, from velocity-area or slope-conveyance studies, or by use of other hydraulic principles.

The peak stages and discharges on many streams during the June 1972 flood greatly exceeded those previously known. Current-meter measurements were obtained where possible; however, the wide areal extent of the flood and the short period (June 22-24) during which the peak flows occurred made it impossible to obtain such measurements at many gaging stations. Measuring facilities were destroyed or overtopped, and access roads or bridges were inundated or washed out at many sites. Even if the site were accessible, reliable current-meter measurements could not have been made on many small streams owing to the short duration of the peak flow. Despite these difficulties, current-meter measurements were obtained at, or near, peak stage, and rating curves were reliably defined at many gaging stations.﻿82

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1&72

At those sites where available current-meter measurements were inadequate to define the stage-discharge relation for extreme flows, it was necessary to determine peak discharge by indirect measurements, such as slope area, contracted opening, flow through culvert, flow over highway embankment, flow over dam, and others. These indirect measurements are based on field surveys of high-water marks, channel geometry, and geometry of hydraulic structures, such as bridges, culverts, highway embankments, and dams. The measurements are indirect only in the sense that the data are collected after the passage of the peak discharge rather than by direct observation of the flow. Techniques used by the Geological Survey in determining peak discharge by indirect methods are described in selected chapters in the series Techniques of Water Resources Investigations of the United States Geological Survey.

STREAMFLOW DATA AT GAGING STATIONS AND MISCELLANEOUS MEASURING SITES

SUMMARY OF PEAK STAGES AND DISCHARGES

Maximum stage and discharge information (contents and pool elevations for reservoirs) for 989 sites in the flood area is summarized in table A-l. This summary includes peak data for daily discharge gaging stations, reservoir gaging stations, crest-stage gaging stations, flood-hydrograph gaging stations, and miscellaneous sites. Sites are listed in the downstream order used in U.S. Geological Survey Water-Supply Papers since 1951 and are identified by a report number (a sequential number assigned to each of the 989 sites) and by the permanent eight-digit number used in Geological Survey annual series of surface-water reports. Some miscellaneous sites are identified only by a report number. Numbers used in the table correspond to those used to identify the site descriptions in a later section entitled “Streamflow Data.” The report numbers are used to identify the locations of sites shown on plate 1.

In the table summarizing peak stages and discharges (table A-l), the first column under maximum flood previously known, the period of known floods, is not necessarily the same as the period for which the gaging stations have been operated. For instance, if a gaging station has been operated since 1942 but experienced a flood in 1936 for which the peak stage and discharge has been determined to be the greatest since at least 1891, the period of known

floods would be shown as 1891-1972, and the peak stage and discharge for the 1936 flood would be listed. If only the stage of the 1936 flood is known, two periods will be shown. The period 1891-1972 will be listed with only the stage of the 1936 flood given. The next line will show the period 1942-72, with the maximum stage and discharge for that period shown. If the 1936 peak was the greatest known for the period 1891 to the time the gage was installed in 1942 but was subsequently exceeded by a flood in 1969, the period of known floods would be 1891-1972, and the peak stage and discharge for the 1969 flood will be listed. If it is not known whether the 1936 flood is the greatest for a given period of time, the periods of known floods will be shown as 1942-72, and information for the 1936 flood will be shown on the next line.

The recurrence interval shown in the last column is the average interval of time in which the peak discharge during June-July 1972 can be expected to be exceeded once. Methods of determining the recurrence interval are explained in the section titled “Flood Frequency.” If the recurrence interval is estimated to be greater than 100 years, it is not listed, and the symbol indicating that the recurrence interval is greater than 100 years is shown.

STATION DESCRIPTION AND DISCHARGE TABLES

Information on stage and discharge (elevation and contents for reservoir stations) for 989 sites in the flood area is given. At some sites sediment data are also shown. The data generally consist of a station description, a table of daily mean discharges for June-July 1972, and a table of stages and discharges at indicated times during the period of severe flooding. Comparable sediment data are included where available. At miscellaneous sites and at crest-stage stations where only peak stage and discharge are known, only the station description is included. For some sites classified as continuous-record or flood-hydrograph gaging stations, malfunction of the recording gage during critically high flow periods did not permit inclusion of a table of stages and discharges at indicated times. This table was also omitted in some cases where the magnitude of the peak flow was relatively insignificant.

The station description gives information relative to the location of the site, size of drainage area upstream from the site, nature of gage-height record obtained during the period covered by this report, datum of the gage, definition of the stage-discharge relationship, maximum stage and dis-﻿DEATHS AND DAMAGE

83

charge during June-July 1972, maximum stage and discharge known prior to this flood, effect of regulation and diversion, and other pertinent information.

The table of daily mean discharge for continuous-record gaging stations or reservoir contents for June-July 1972 follows the station description. Daily mean suspended-sediment concentrations and loads are also given if these data are available. The table also shows monthly mean discharge, in cubic feet per second, and generally the monthly runoff, in inches and acre feet. If data are available, the monthly mean sediment load, in tons per day, and the monthly sediment load, in tons, are also shown. The 2 months for which data are included are adequate to show conditions for antecedent and recession periods. The table of stage and discharge at indicated times gives sufficient data to permit reproduction of stage and discharge hydrographs. Suspended-sediment concentration detailed in a similar manner is included in this table, where data are available. Only data for the period of severe flooding are included in this table.

DEATHS AND DAMAGE

Although Agnes barely reached the hurricane stage and then only for hours, she was the costliest hurricane in United States history (table 6). While it is true that gradually increasing population, industrialization, and property values tend to make the latest hurricane costlier than earlier hurricanes of equal or greater intensity, Agnes’ large size was an important factor in her setting a new record for damage. Agnes and the extratropical storm each brought heavy rains over large areas. These heavy rains continued after the two systems merged. The combined rainfall produced severe flooding over a large area. That it occurred following generally wet weather over the heavily populated and indus-

Table 6.— The 10 most destructive tropical cyclones in the United States since 1930 (De Angelis, 1972)

Damage

Storm	Year	(millions Deaths

of dollars)

Agnes _________________________ 1972	$3,102.6	117

Camille _______________________ 1969	1,420.7	258

Betsy _________________________ 1965	1,420.5	75

Diane _________________________ 1955	831.7	184

Carol _________________________ 1954	461.0	60

Celia _________________________ 1970	453.8	11

Carla _________________________ 1961	408.3	46

New England Huricane_______	1938	387.1	600

Donna _________________________ 1960	386.5	50

Hazel _________________________ 1954	251.6	95

trialized Mid-Atlantic States added to its effectiveness as a producer of costly floods. The fact that the extratropical Low into which the tropical storm was absorbed stalled for a few days in the Pennsylvania-New York area, thus adding to the tropical storm rainfall, was a contributing factor, even though the heaviest rainfall occurred before the two Lows joined.

The death toll of 117 was light considering the severity of the widespread floods. Total damage was estimated to be $3.1 billion, or over twice that produced by the very violent Camille in August 1969 and exceeded the combined total damage of the two next costliest hurricanes, Camille and Betsy (1965), by $257 million (table 6). Damage and deaths in each of the 12 States affected are summarized in table 7, and the number of families suffering property losses and the nature of these losses are given in table 8. The loss of life and damage to property would very likely have been much greater had it not been for the timely weather and flood forecasts (U.S. National Oceanic and Atmospheric Administration, 1973) issued in connection with this storm. Not included in the above estimates are the seven deaths and the damage resulting from the severe flooding in western Cuba. In Pinar Del Rio, 97 homes were destroyed and another 300 damaged.

Pennsylvania.—Agnes was the worst natural disaster ever to hit Pennsylvania. Damage was so extensive that the entire State was declared a disaster area. There were 48 deaths, and damages were estimated to be $2,119 billion, or about two-thirds of the total damage wrought by Agnes. Damage in the Schuylkill River Basin alone was estimated at over $330 million. In that part of the Ohio River Basin lying within the State, damage was roughly estimated at $92 million. In Wilkes-Barre, 100,000 persons evacuated, and 60 percent of the city was inundated. Altogether, some 250,000 persons were forced

Table 7.—U.S. deaths and damage attributed to Agnes (De Angelis, 1972)

State	Damage	Deaths
Pennsylvania	$2,119,269,000	48
New York	702,502,000	24
New Jersey		 15,000,000	1
Maryland	110,186,000	19
Ohio _	6,818,000	0
Delaware	Light	1
West Virginia _ _	7,753,000	0
Virginia		 125,987,000	13
North Carolina	6,558,380	2
South Carolina		 50,000	0
Georgia	205,000	0
Florida	8,243,000	9

Total _________________ $3,102,571,380	117﻿84

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

Table 8.—Classification of property damage (DeAngelis, 1972)

State	Families  suffer-  ing  loss	Dwell-  ings  destroyed	Dwell-  ings,  major  damage	Dwell-  ings,  minor  damage	Mobile  homes  destroyed	Mobile  Homes,  major  damage	Farm  build-  ings  destroyed	Farm  build-  ings,  major  damage	Small  busi-  nesses,  destroyed  or  major  damage
Virginia	7,063	95	1,307	3,086	125	450	u	27	205
Maryland	3,479	103	866	1,664	50	43	17	44	81
West Virginia	1,946	108	344	1.214	118	91	0	10	18
Washington, D.C.		506	0	0	350	0	0	0	0	0
New York	40,090	628	4,922	27,910	135	367	92	341	1,547
Pennsylvania-	69,860	2,321	33,412	29,455	1,266	1,908	435	1,249	3,003
New Jersey.1 Ohio	405	0	3	302	0	100	0	0	0
Florida	2,893	96	447	1,355	177	374	0	0	988
Georgia	1	0	0	0	0	1	0	0	0
North Carolina	7	0	1	0	0	6	0	0	0
Total	126,250	3,351	41,302	65.336	1,871	3,340	555	1,671	5,842

1 Almost all damage occurred in Pennsylvania.

to evacuate their homes, and many returned to find their homes gone.

Public water and sewage facilities were flooded out in many areas, and water had to be rationed in some communities. Fires that broke out in many places burned unchecked because flooding made them inaccessible.

Crop losses were estimated to have been $120 million. The floods washed out or closed 569 bridges, and total damage to roads and bridges was estimated at $300 million. Damage to industry amounted to $1 billion.

New York.—Second only to Pennsylvania in number of deaths and damage suffered was New York, with 24 deaths and $703 million damage, of which over $157 million was in the Susquehanna River basin. About 100,000 persons had to be evacuated from their homes. Almost the entire population of Corning was forced to flee, and about half the population of Elmira had to evacuate. Fear that dams would fail led many residing below the dams to flee. Lakeshore residents were forced to move to higher ground. The overflow of some of the Finger Lakes caused damage to boats, docks, marinas, and surrounding properties. Altogether, some 5,000 homes were destroyed or badly damaged, with the greatest loss being in the Corning-Elmira area. A tragic loss was the famous Glass Museum at the Corning Glassworks, where water rose almost to the ceiling of the museum rooms, with the result that many priceless ancient glass objects were lost. Other hard hit cities were Salamanca, Olean, Hornell, and Wellsville. At Wellsville, a hospital wing collapsed as a result of flooding.

Rains and floods caused extensive damage throughout the southwestern tier and Finger Lakes counties. Greatest damage was to potatoes, corn,

and hay. Dairy farmers suffered heavy losses also. Vineyards in the Naples area were inundated, and ruinous heavy rains occurred during the critical bloom stage.

The enormous damage resulting from all the above losses led to the following counties being declared disaster areas: Allegany, Cattaraugus, Cayuga, Chemung, Livingston, Ontario, Schuyler, Seneca, Steuben, Tompkins, Wyoming, and Yates.

New Jersey.—Total storm damage in New Jersey was estimated at $15 million, of which $10 million resulted from crop damage. One death was reported.

Ohio.—Northeasterly winds generated 15-foot waves and a 3.5-foot rise in the lake level along the south shore of Lake Erie, which caused damage to ships, boats, buildings, houses, docks, and cars. Other damage resulted from flooding along the Ohio River between East Liverpool and Hannibal, with Powhatan Point being hard hit. Total damage in the State was reported at slightly over $6 million. No deaths were reported.

Delaware.—One storm-connected death was reported, but damage was minor.

Maryland-District of Columbia.—The 19 deaths attributed to the storm ranked third among the death tolls in the States affected by Agnes. No deaths were reported in the District of Columbia. The $110 million in damages ranked fourth. About

1,000	homes were destroyed or suffered major damage. The following counties, including Baltimore City, were declared disaster areas: Anne Arundel, Baltimore, Carroll, Cecil, Charles, Frederick, Harford, Howard, Montgomery, Prince Georges, and Washington. Also included were the counties in the Chesapeake Bay area: Calvert, Dorchester, Kent, Queen’s, St. Mary’s, Somerset, Talbot, and Wicomico.﻿SELECTED REFERENCES

85

Disaster in the Chesapeake Bay counties was primarily in the form of losses to the shellfish industry, with resultant unemployment. Heavy rains cause excessive runoff into the bay, which reduces its salinity. The fresh water forms a layer on the surface of the bay. This surface layer gradually mixes with and dilutes the lower layer of salty water. Shellfish, particularly oysters, cannot survive prolonged exposure to low salinities. Also, a layer of fresh water overlying salt water with little mixing tends to reduce the amount of dissolved oxygen in the salt water. Damage to the industry was estimated to be somewhat less than that attributed to Camille in 1969.

Virginia.—In Virginia there were 13 deaths, and total damage was estimated at $126 million, the third largest loss of the States affected by Agnes. Destruction was widespread throughout the central part of the State, but was particularly heavy in the northern part, where Fairfax County reported damage estimated at $25 million, the greatest county loss by far. In the Fourmile Run drainage area, which includes parts of Arlington and Fairfax Counties, damage was estimated at $14 million.

Destruction ranged from agricultural damage on small streams to inundated cities and towns on the larger rivers, such as the Roanoke and the James, where total damage for these basins was estimated to be $20 million and $50 million, respectively. Richmond, the capital city, was hit hard. The water supply and sewage treatment plants were inundated, as were the electrical and gas plants, which were partly closed. Only one of the five bridges crossing the James River was usable. Downtown Richmond was closed for several days. Industry and business suffered much damage, and many residents were evacuated from their homes.

Other cities and towns suffering great damage included Alexandria, Buchanan, Charlottesville, Danville, Farmville, Fredericksburg, Glasgow, Lexington, Lynchburg, Manassas, Occoquan, Roanoke, Salem, Scottsville, and Waynesboro.

Altogether, through the State, some 1,400 homes were destroyed or suffered major damage. Much damage was done to highways. At the height of the flood, 600 miles (960 km) of road was under water, and 103 State highway bridges were destroyed or damaged. Most of the latter were small bridges on secondary highways.

Real tragedies occurred along the small tributaries. Most creeks and streams overflowed their banks and swept the adjacent land clean. Homes,

household goods, and other possessions were washed away. Losses were lessened somewhat by timely warnings, which also kept the death toll from being higher.

West Virginia.—Most of the damage, estimated to be $7,753 million, occurred along the Ohio River between Chester and New Martinsville, with Wheeling being hit particularly hard. No deaths were reported. Some 3,000 homes and 1,500 businesses were inundated along this reach of the river. In Green-briar County, which adjoins Virginia, Dry and Howard Creeks overflowed their banks and damaged 22 businesses and 56 homes. Five houses were destroyed. Damage there was estimated at $323,000.

North Carolina.—Two deaths were reported, and total damage in the State was estimated at $6,558 million. About two-thirds of the damage ($4.22 million) occurred in the Yadkin River basin, where

86,000	acres (about 135 mi2, or 350 km2) was inundated, and agricultural losses, mostly in growing crops, were estimated at $3.5 million. Flooding in Elkin, Yadkin College, and other river towns accounted for the remainder. One of the two deaths reported occurred in Surry County, when a canoe overturned, and the other, in Iredell County, when a man driving a tractor was swept away in the flood waters. In Catawba, Congaree, and Reedy River Basins, minor home and trailer damage and some crop losses were estimated at $32,000.

South Carolina.—Damage in this State was restricted to the Pee Wee River basin, where floods caused about $25,000 in crop losses.

Georgia.—Total damage was estimated at $205,-000, with no deaths reported. A tornado near Douglas, Coffee County, in the afternoon of June 19, was responsible, for damage estimated at $100,000. That same afternoon, another tornado near Blackshear, Pierre County, destroyed a mobile home for a loss of $5,000. Elsewhere in the State, total property damage was estimated at $80,000 and crop damage at $20,000.

Florida.—Nine deaths were reported, another 170 persons were injured, and total damage from tides, winds, and the 15 tornadoes reported on June 18-19 was estimated at $8,243 million. The tornadoes alone accounted for $4.5 million of the damage. The gulf coast counties from Monroe to Bay (Key West to Panama City) were declared disaster areas. Panama City, 18 feet (5.5 m) above mean sea level, in Bay County, suffered little damage, but low-lying coastal villages between Carrabelle and Apalachicola in Franklin County suffered great damage. Damage in Franklin County alone as a result of the﻿86

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

storm tides ran well over $1 million. These tides, the highest in many years, destroyed homes and businesses, washed out roads, and cut off access to many offshore islands. Pinellas County was also hit hard, particularly in the St. Petersburg area, with extensive beach erosion and shorefront property damage south to the Fort Myers area.

Inland, winds and tornadoes were responsible for the damage and most of the deaths. The following counties were declared disaster areas: Brevard, Hardee, Hendry, and Okeechobee. At Okeechobee City, a series of windstorms cut a swath 100 yards (90 m) wide through Treasure Island Park, a fishing lodge, and several other mobile home parks, killed six people, and injured another 40. Damage, including destruction of 50 mobile homes, was estimated at $500,000.

A windstorm near Ft. Denaud, Hendry County, destroyed a trailer, killing a woman and injuring her daughter. It then tore up some citrus groves and several other trailer parks near La Belle. Property damage was estimated at $200,000 and crop damage, $10,000. Other deaths included that of a child drowned in a rain-swollen stream and another caused by a heart attack attributed to the storm.

SELECTED REFERENCES

Benson, M. A., 1962, Evolution of methods for evaluating the occurrence of floods: U.S. Geol. Survey Water-Supply Paper 1580-A, p. A1-A29.

Benson, M. A., and Dalrymple, Tate, 1967, General field and office procedures for indirect discharge measurements: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. Al, 30 p.

Bodhaine, G. L., 1968, Measurement of peak discharge of culverts by indirect methods: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. A3, 60 p. Bogart, D. B., 1960, Floods of August-October 1955, New England to North Carolina: U.S. Geol. Survey Water-Supply Paper 1420, 854 p.

Camp, J. D., and Miller, E. M., 1970, Flood of August 1969 in Virginia: U.S. Geol. Survey open-file report, 120 p. Carpenter, D. H., and Simmons, R. H., 1969, Floods of August 1967 in Maryland and Delaware: U.S. Geol. Survey open-file report, 98 p.

Carter, R. W., and Davidian, Jacob, 1968, General procedures for gaging streams:	U.S. Geol. Survey Techniques.

Water-Resources Inv., book 3, chap. A6, 13 p.

Corbett, D. M., and others, 1943, reprinted 1957, Stream-gaging procedures, A manual describing methods and practices of the Geological Survey: U.S. Geol. Survey Water-Supply Paper 888, 245 p.

Dalrymple, Tate, 1960, Flood-frequency analyses: U.S. Geol. Survey Water-Supply Paper 1543-A, 80 p.

Dalrymple, Tate, and Benson, M. A., 1967, Measurement of peak discharge by the slope-area method: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. A2,

12 p.

DeAngelis, R. M., 1972, North Atlantic tropical cyclones, 1972: Natl. Oceanic and Atmospheric Climatological Data Natl. Summ., p. 62-69.

DeAngelis, R. M., and Hodge, W. T., 1972, Preliminary climatic data report, Hurricane Agnes, June 14-23, 1972: Natl. Oceanic and Atmospheric Adm. Tech. Memo. EDS NCC-1, 62 p.

Department of the Army, Corps of Engineers, 1956, New England floods of 1955: Part 1, Storm data; Part 2, Flood discharges; Part 3, Flood profiles; Part 4, Flood damages: Part 5, Effect of flood-control projects: Boston, Mass., New England Div.

Green, A. R., 1964, Magnitude and frequency of floods in the United States, Pt. 1-A, North Atlantic slope basins, Maine to Connecticut: U.S. Geol. Survey Water-Supply Paper 1671, 260 p.

Hershfield, D. M., 1963, Rainfall frequency atlas of the United States for durations from 30 minutes to 24 hours and return periods from 1 to 100 years: U.S. Weather Bur. Tech. Paper 40.

Hoyt, W. G., and Langbein, W. B., 1955, Floods: Princeton Univ. Press, p. 59, 60, 72-76.

Hulsing, Harry, 1967, Measurement of peak discharges at dams by indirect method: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. A5.

Langbein, W. B., and Iseri, K. T., 1960, General introduction and hydrologic definitions: U.S. Geol. Survey Water-Supply Paper 1941-A, 29 p.

Matthai, H. F., 1967, Measurement of peak discharge of width contractions by indirect methods: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. A4, 44 p.

Miller, E. M., 1969, Floods in Virginia, magnitude and frequency: U.S. Geol. Survey open-file report, 371 p.

Miller, E. M., and Kapinos, F. P., 1970, Floods of July 22, 1969 in the Northern Virginia area: U.S. Geol. Survey open-file report, 35 p.

Miller, J. F., 1964, Two-to-ten-day precipitation for return periods of 2 to 100 years in the contiguous United States: U.S. Weather Bur. Tech. Paper 49.

Namias, Jerome, 1973a, Birth of Hurricane Agnes—triggered by the transequatorial movement of a mesoscale system with a favorable large-scale environment:	Monthly

Weather Rev., v. 101, p. 177-179.

------- 1973b, Hurricane Agnes—an event shaped by large-

scale air-sea systems generated during antecedent months: Royal Meterol. Soc. Quart. Jour., v. 99, p. 506-519.

Porterfield, George, 1972, Computations of fluvial sediment discharges: U.S. Geol. Survey Techniques Water-Resources Inv., book 3, chap. C3, 66 p.

Reitan, C. H., 1960, Distribution of precipitable water over the continental United States: Am. Meterol. Soc. Bull., v. 41, p. 79-87.

Simpson, R. H., and Hebert, P. J., 1973, Atlantic hurricane season of 1972: Monthly Weather Rev., v. 101, p. 325-331.

Speer, P. R., and Gamble, C. R., 1964, Magnitude and frequency of floods in the United States, Pt. 2-A, South Atlantic slope basins, James River to Savannah River: U.S. Geol. Survey Water-Supply Paper 1673, 329 p.﻿SELECTED REFERENCES

87

------ 1965, Magnitude and frequency of floods in the United

States, Ohio River basin except Cumberland and Tennessee River basins: U.S. Geol. Survey Water-Supply Paper 1675, 630 p.

Tice, R. H., 1968, Magnitude and frequency of floods in the United States, Pt. 1-B, North Atlantic slope basins, New York to York River: U.S. Geol. Survey Water-Supply Paper 1672, 585 p.

U.S. National Oceanic and Atmospheric Administration, National Weather Service, 1973, Hurricane Agnes, June 14-23, 1972: Natl. Oceanic and Atmospheric Adm. Natl.

Weather Ser. Prelim. Rpts. on Hurricanes and Tropical Storms, p. 23-193.

Walker, P. N., 1971, Flow characteristics of Maryland streams: Maryland Geol. Survey Rpt. Inv., no. 16, 160 p. U.S. Water Resources Council, 1967, A uniform technique for determining flood flow frequencies, Bull. 15, Hydrol. Comm., Water Resources Council, 1925 Vermont Ave., N.W., Washington, D.C. 22205, 15 p.

Wiitala, S. W., 1965, Magnitude and frequency of floods in the United States, St. Lawrence River basin: U.S. Geol. Survey Water-Supply Paper 1677, 357 p.﻿88

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

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RUNOFF, IN INCHES..................................................... 2﻿GAGE HEIGHT, IN FEET, AND DISCHARGE, IN CUBIC FEET »ER SECOND, AT INDICATED TIME, 1972	GAGE HEIGHT* IN FEET, AND DISCHARGE, IN CUBIC FFET PER SFCOND, AT INDICATED TIME, 1972

114

HURRICANE AGNES RAINFALL AND FLOODS, JUNEXULY 1972

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120

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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REMARKS.--Flow affected by two reservoirs upstream; Needwood Lake on Rock Creek since Sept. 1966 and Bernard Frank Lake on North Branch Rock Creek since Feb. 1968. Total drainage area above lakes about 25 sq mi.﻿224

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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1966 to May 1972:	Discharge, 1,180 cfs Aug. 28, 1971 (gage height, 7.19 ft).	MAXIMUMS-June-July 1972:	Discharge, 7,840 cfs 1630 hours June 21 (gage height, 12.87 ft).

1951 to May 1972:	Discharge, 3,100 cfs June 8, 1955 (gage height, 9.59 ft).

MEAN DISCHARGE, IN CUBIC FEET PER SECOND, 1972	Flood in October 1942 reached a stage of about 13 ft, from information by local residents.﻿MONTHLY MEAN DISCHARGE,IN CUBIC FEET PER SECOND..................... 107

RUNOFF,IN INCHES.................................................... 9,

STREAMFLOW DATA

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AND FLOODS, JUNE-JULY 1972

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

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286

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RUNOFF,IN INCHES................................................. 7.38	1.82	MONTHLY MEAN DISCHARGE,IN CUBIC FEET PER SECOND,

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'E TIME GAGE DISCHARGE	DATE TIME GAGE DISCHAF.GE DATE TIME GAGE DISCHARGE	LCCATION.—Lat 40°35'27", long 79°03'11", Indiana County, in gatehouse at right end of Yellow

HEIGHT	HEIGHT	HEIGHT	Creek Dam on Yellow Creek, at Yellow Creek State Park, 3 miles southwest of Penn Run.

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RUNOFF,IN INCHES.................................................... 6﻿302

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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RUNOFF,IN INCHES......................................................

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RUNOFF,IN INCHES................................................... I-64	1-37	____ HEIGHT	HEIGHT	HEIGHT﻿(805) 03069500 CHEAT RIVER NEAR PARSONS

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(813) 03072590 GEORGES CREEK AT SMITHFIELD, PA.

iCATION.--Lat 39°47'44", long 79°47'47", Fayette County, on right bank at downstream side of bridge on Georges Township Road at Smithfield, 1.6 miles upstream from Mountain Creek, and 2.5 miles southwest of Fairchance.﻿0400	7.24	1,310	MONTHLY MFAN DI SC HA RGF,IN CUBIC FFFT PFR SECOMD

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DISCHARGE RECORD.--Stage-discharge relation defined by current-meter measurements below 60 cfs and by contracted-opening and slope-area measurement at 586 cfs.

MAXIMUMS.--June-July 1972:	Discharge, 586 cfs June 23 (gage height, 5.25 ft).

1959 to May 1972:	Discharge, 394 cfs Aug. 19, 1969 (gage height, 6.29 ft).﻿STREAMFLOW DATA

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MONTHLY MEAN 0ISCHARGE.IN CUBIC FFET PER SECOND....................... 68,900	50,800﻿GAGE HEIGHT, IN FEET, AND DISCHARGE, IN CUBIC FEET PER SECOND, AT INDICATED TIME, 1972	KINAWHA RIVER BASIN

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(860) 03184200﻿XIMUMS.—June-July 1972:	Discharge, 38,000 cfs 2000 hcurs June 21 (gage height, 15.24 ft);	------------------------------------------------

33,500 cfs 0200 hours July 6 (gage height, 13.94 ft).	MONTHLY MEAN DISCHARGE,IN CUBIC FEET PER SECOND,

1896 to May 1972 : Discharge, 77,500 cfs Mar. 14, 1918 (gage height, 22.0 ft, from	RUNOFF,IN INCHES................................

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GAGE-HEIGHT RECORD.--Crest stages only. Altitude of gage is 1,850 ft (from topographic map).	7,000 cfs and by slope-,﻿(864) 03189590 SUMMERSVILLE LAKE NEAR SUMMERSVILLE

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RUNOFF,IN INCHES...................................................... 4.09	3.﻿GAGE HEIGHT, IN FEET, AND DISCHARGE, IN CUBIC FEET CFR SECOND, AT INDICATED TIME, 1972	GAGE HEIGHT, IN FEET, AND DISCHARGE, IE CUBIC FEET PER SECOND, AT INDICATED TIME, 1972

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332

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

1,850 1 ,850 1,600	1 ,760 3,040 3,720 7,070 7,250	7,250  5,620  4,960	O O O o o O' vO cm r- m cm co m o r-  •t MCM NH	1,700  1,200  1,190	1,190  897  897	SS2  CO *c >o
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13.0 miles downstream from Kanawha River, 13.1 miles downstream from base gage, and at mile I0RD.—Water-stage-recorder graph. Datum of gage is at mean sea level.	278.5 (measured downstream from Pittsburgh, Pa.).

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MONTHLY MEAN DISCHARGE,IN CUBIC FEET PER SECOND.................. 1,990	1,230

RUNOFF,IN INCHES.................................................. A.09	2﻿GAGE-HEIGHT RECORD._Digital-recorder tape punched at 60-minute intervals. Datum of gage is	GAGE-HEIGHT RECORD-Crest stages only. Altitude of gage is 1,040 ft (from topographic map).

490.263 ft above mean sea level, Sandy Hook datum.

DISCHARGE RECORD.--Stage-discharge relation defined by current-meter measurements bel iw 320 cfs DISCHARGE R2CORD.—Stage-discharge relation is a constant-fall rating defined by current-	and extended above by logarithmic plotting.

334

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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GAGE-HEIGHT RECORD-Crest stages only. Altitude of gage is 896 ft (from topographic map).

DISCHARGE RECORD.--Stage-discharge relation defined by current-meter measurements below 3,000 cfs and by contracted-opening measurement at 9,260 cfs.﻿(886) 04220384 OREBED CREEK NEAR STANNARDS, N.Y.	(899) 04220500 DYKE CREEK AT WELLSVILLE, N.Y.

(Miscellaneous site)	(Gaging station, discontinued 1960)

LOCATION. -Lat 42°01'37", long 77°56,15", Allegany County, at upstream side of bridge on Graves	LOCATIONLat 42°07'14", long 77°56'13", Allegany County, at bridge on Miller Street in

Road, 0.7 mile upstream from mouth, and 4.2 miles southwest of Stannards.	Wellsville, 0.6 mile upstream from mouth, and 1.2 miles downstream from Trapping Brook.

336

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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LOCATIONLat 42°34'10", long 78°02'4S", Wyoming County, on left bank at Portageville, 300 ft

downstream from small tributary, 350 ft downstream from abandoned bridge piers, and 0.7 mile	LOCATIONLat 42°30'52", long 77°48'12", Livingston County, on right bank 300 ft downstream

upstream from Upper Falls.	from bridge on Linzy Road, 1.3 miles southwest of Ossian, and 5.1 miles upstream from mouth.

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RUNOFF,IN INCHES...................................................... 1«15	0﻿STREAMFLOW DATA

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HURRICANE AGNES RAINFALL AND FLOODS, JUNE-^IULY 1972

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LOCATION-Lat 42°36'19", long 77<:,24,47',, Ontario County, at bridge on State Highways 21 and 245, 0.1 mile southwest of Naples, and 0.15 mile upstream from mouth at Eelpot Creek.﻿STREAMFLOW DATA

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X >-• X 0) l-H T3 LU 3﻿358

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

INDEX TO STREAMFLOW DATA

A	Page

Abers Creek near Murrysville, Ba------------------------------323

Abrahams Creek at West Wyoming, Ba----------------------------13 5

Abram Creek at Oakmont, W.Va----------------------------------l8T

Accotink Creek at King Arthur Road, near Annandale, Va--------229

near Annandale, Va-----------------------------------------229

near Newington, Va-----------------------------------------  228

A ft on, Va., Stockton Creek near-----------------------------252

Akeley Run near Russell, Ba-----------------------------------286

Albright Creek at East Homer, N.Y-----------------------------117

Alderson, W.Va., Greenbriar River at--------------------------- 329

Griffith Creek near------------------------------------------329

Alexandria, Va., Cameron Run at---------------------------------227

Fourmile Run at--------------------------------------------226

Alfred, N.Y., Canacadea Creek near----------------------------123

Canacadea Creek tributary	No.	1	at----------------------- 123

Canacadea Creek tributary	No.	2	at-----------------------12 3

McHenry Valley Creek tributary	No.	1	near--------------12U

McHenry Valley Creek tributary	No.	2	near--------------12U

Railroad Brook near------------------------------------------337

Alfred Station, N.Y., Canacadea Creek at---------------------- 12U

East Branch Canacadea Creek at-----------------------------— 12 3

Allegheny Reservoir near Kinzua, Ba-----------------------------28U

Allegheny River at Coudersport, Ba----------------------------282

at Eldred, Ba-----------------------------------------------2 83

at Franklin, Ba----------------------------------------------290

at Kittanning, Ba--------------------------------------------297

at Natrona, Ba----------------------------------------------— 30U

at Barker, Ba----------------------------------------------29

at Salamanca, N.Y--------------------------------------------282

at Warren, Ba------------------------------------------------285

at West Hickory, Fh---------------------—------------------286

Allen Creek near Beydton, Va------------------------------------280

near Rochester, N.Y------------------------------------------3^3

Almond Lake near Almond, N.Y----------------------------------12l

Almond, N.Y., Almond Lake near--------------------------------12l

Canisteo River tributary near-------------------------------12 3

Canisteo River tributary No.	2 near-----------------------12 3

Karr Valley Creek near---------------------------------------12U

Altavista, Va.-, Roanoke (Staunton) River at--------------------269

Amelia, Va., Nibbs Creek tributary near-----------------------2 59

Amherst, Va., Buffalo River tributary near— ------—   —-- 250

Andersonville, Va., Holiday Creek near-------------------------2 56

Andover, N.Y., East Valley Creek tributary near— -------------337

Fullmer Valley Creek tributary near------------------------— 336

Indian Creek near--------------------------------------------337

Quig Hollow Brook near---------------------------------------337

Angelica Creek at Transit Bridge, N.Y-------------------------- 338

near Angelica, N.Y-------------------------------------------338

Angelica, N.Y., Angelica Creek near-----------------------------338

Baker Creek near-------------------------------------------  338

Annandale, Va., Accotink Creek at King Arthur Road at---------229

Accotink Creek near----------------------------------------  229

Holmes Run near----------------------------------------------226

Annapolis, Md., North River near--------------------------------182

Anthony Creek near Anthony, W.Va--------------------------------326

Anthony, W.Va., Anthony Creek near------------------------------326

Antietam Creek near Sharpsburg, Md------------------------------203

near Waynesboro, Ba------------------------------------------202

Appomattox River at Farmville, Va------------------------------2 58

at Matoaca, Va-----------------------------------------------258

at Mattoax, Va-----------------------------------------------258

near Appomattox, Va—-—--------------------------------------— 256

Appomattox, Va., Appomattox River near------------------------* 2 56

Right Hand Fork near-----------------------------------------271

A quia Creek near Garrisonville, Va-----------------------------233

Arbutus, Md., East Branch Herbert Run at----------------------180

Archbald, Pa., Lackawanna River at----------------------------- 133

Areola, Va., South Fork Broad Run near--------------------------2l6

Ark, Va., Beaverdam Swamp near—-------------------------------  2U0

Arkport, N.Y., Arkport Reservoir near---------------------------122

Canisteo River at-------------------------------------------— 122

Arkport Reservoir near Arkport, N.Y.----------------------------122

Arlington, Va., Doctors Run at----------------------------------226

Long Branch at-----------------------------------------------226

Lucky Run at-------------------------------------------------226

Bage

Arvonia, Va., Slate River near-------------------------------253

Ashland, Va., South Anna River near--------------------------21+1

South Anna River tributary near---------------------------2Ul

Ashville, Ba., Bradley Run near------------------------------139

Atlee, Va., Totopotomoy Creek near---------------------------—2k2

Auburn, N.Y., Owasco Lake near--------------------------------3U8

Owasco Outlet near-----------------------------------------3^8

Audra, W.Va., Middle Fork River at---------------------------306

Aughwick Creek near Three Springs, Fa------------------------159

Augusta, W.Va., Tearcoat Creek tributary near----------------198

Avoca, N.Y., Cohocton River at--------------------------------127

Goff Creek near--------------------------------------------128

Tenmile Creek at-------------------------------------------127

Avon, N.Y., Genesee River at---------------------------------3^1

Avondale, Md., Little Ripe Creek at--------------------------212

Axemann, Ba., Spring Creek near------------------------------lU5

Aylett Creek at Aylett, Va-----------------------------------2U3

B

Back Creek near Jones Springs, W.Va--------------------------200

near Mountain Grove, Va-----------------------------------2l3

Bacon Ridge Branch at Chesterfield, Md-----------------------182

Baisman Run at Broodmoor, Md----------------------------------177

Baker Creek near Angelica, N.Y--------------------------------338

Baker, W.Va., Lost River at McCauley near--------------------197

Bald Eagle Creek at Beech Creek Station, Ba------------------1^9

at Blanchard, Fa-------------------------------------------1^6

at Tyrone, Ba----------------------------------------------157

below Spring Creek at Milesburg, Fa-----------------------1^6

Baldwinsville, N.Y., Seneca River at-------------------------3^9

Banister River at Halifax, Va--------------------------------279

Barcelona, N.Y., Chautauqua Creek at--------------------------33^

Bard, Pa., Little Falls Creek at-----------------------------190

Barnesville, Md., Bucklodge Branch tributary near-----------—218

Barnum, W.Va., North Branch Potomac River at-----------------187

Barrackville, W.Va. Buffalo Creek at---------------------—310

Barton, Md., Savage River near--------------------------------188

Basin Run at Liberty Grove, Md-------------------------------172

at West Nottingham, Md-------------------------------------172

Bassett, Va., Smith River at-----------------------------------27

Batcheliars Run at Oakdale, Md--------------------------------225

Battle Run near Laurel Mills, Va-----------------------------235

Bear Creek at Friendsville, Md-------------------------------319

Bearskin Creek near Chatham, Va-------------------------------278

Beaverdam Swamp near Ark, Va----------------------------------2h0

Beaver Swamp Brook at Mama rone ck, N.Y---------------------- 90

at Rye, N.Y------------------------------------------------ 90

Beck Creek near Cleona, Pa-----------------------------------167

Beech Creek at Monument, Pa— --------------------------------lU 8

Beech Creek Station, Pa., Bald Eagle Creek at----------------1^9

Bel Air, Md., Bynum Run at------------------------------------17^

Bel Alton, Md., Clark Run near-------------------------------2 32

Belden, Ba., Dunning Creek at---------------------------------158

Be lews Creek near Kernersville, N.C-------------------------272

Belington, W.Va., Tygard Valley River at---------------------307

Be lie grove, Md., Sideling Hill Creek near------------------197

Be lie point,	W.Va., Big Creek	near-------------------------328

Be Ilona, N.Y., Kashong Creek	near--------------------------3^5

Bellwood, Pa., Sandy Run near--------------------------------156

Belmond, N.Y., Feathers Creek near----------------------------337

Bel Pre	Creek	at	Layhill, Md-------------------------------22U

Bennett	Creek	at	Fhrk Mills, Md----------------------------215

Bennetts Creek at Canisteo, N.Y-------------------------------126

Bennetts Creek tributary at Greenwood, N.Y-------------------126

Benson, Md., Winters Run near--------------------------------17^

Bent Creek,	Va., James River	at---------------------------250

Berne, Ba.,	Schuylkill River	at--------------------------- 92

Berryville, Va., Opequon Creek near--------------------------200

Bethesda, Md., Little Falls Branch near----------------------220

Beulahville, Va., Mattaponi River near-----------------------2U2

Big Creek near Be lie point, W.Va----------------------------328

near North Horne 11, N.Y----------------------------------123

Big Elk	Creek	at	Elk Mills, Md-----------------------------112

Big Flats, N.Y.,	Chemung River near-------------------------129﻿INDEX TO STREAMFLOW DATA

359

Big Flats, N. Y., Sing sing Creek near-------------------------

Big Lickinghole Creek tributary near Fern Cliff, Va------------

Big Otter River near Evington, Va------------------------------

Big Piney Run near Salisbury, Pa-------------------------------

Big Pipe Creek at Bruceville, Md-------------------------------

Big Rocky Run at Sully Road near Centreville, Va---------------

Big Run near Sprankle Mills, Pa--------------------------------

Big Sandy Creek at Rockville, W.Va-----------------------------

Birchardville, Pa., Middle Branch Wyalusing Creek

tributary near-------------------------------------------—

Birdsall, N.Y., Black Creek near-------------------------------

Bishopville, N.Y., Canisteo River at---------------------------

Bixler Run near Loysville, Pa----------------------------------

Blackbird Creek at Blackbird, Del------------------------------

Blackbird, Del., Blackbird Creek at----------------------------

Saw Mill Branch tributary near------------------------------

Black Brook at lyre, N.Y---------------------------------------

Black Creek at Churchvilie, N.Y--------------------------------

near Birdsall, N.Y------------------------------------------

Blacklick Creek at Josephine, Pa-------------------------------

Blacks Creek near Mt. Airy, Va---------------------------------

Blackstone, Va., Hurricane Branch near-------------------------

Blackwater River at Davis, W.Va--------------------------------

at Zuni, Va-------------------------------------------------

near Dendron, Va--------------------------------------------

near Franklin, Va-------------------------------------------

Blanchard, Pa., Bald Eagle Creek at----------------------------

Foster Joseph Sayers Lake near--------------------------------

Marsh Creek at----------------------------------------------

Blind Brook at Rye, N.Y----------------------------------------

near Purchase, N.Y------------------------------------------

Blind Brook tributary at Purchase, N.Y-------------------------

Bliss, N.Y., Wiscoy Creek at-----------------------------------

Blizzard Run at Danville, Pa-----------------------------------

Block House Creek near English Center, Pa----------------------

Bloomerville, N.Y., Neils Creek near---------------------------

Bloomington, Md., Savage River below Savage River Dam near-----

Savage River Reservoir near---------------------------------

Bloomsburg, Pa., Fishing Creek near----------------------------

Blue March damsite, near Reading, Pa., Tulpehocken Creek at—

Blue Mount, Md., Little Falls at-------------------------------

Bonica Run on U.S. Highway 250, near Philippi, W.Va------------

Boswells Tavern, Va., Bunch Creek near-------------------------

Bower, Pa., West Branch Susquehanna River at-------------------

Bowery Run near Quarryville, Pa--------------------------------

Bowling Green, Va., Mattaponi River near-----------------------

Boydton, Va., Allen Creek near---------------------------------

John H. Kerr Reservoir near---------------------------------

Braddock, Pa., Monongahela River at----------------------------

Bradford, N.Y., Mud Creek tributary near-----------------------

Bradley Run near Ashville, Pa----------------------------------

Brandywine Creek at Chadds Ford, Pa----------------------------

at Wilmington, Del------------------------------------------

Brandywine Creek tributary near Centerville, Del---------------

Brandywine, W.Va., South Fork South Branch Potomac

River at------------------------------------------------

Breesport, N.Y., Rorick Hollow Creek near----------------------

Brewerton, N.Y., Oneida Lake at--------------------------------

Bridgeport, Md., Monocacy River at-----------------------------

Bridge Run near Buckhannon, W.Va-------------------------------

Brien Run at Stemmers Run, Md----------------------------------

Briery, Va., North Meherrin River near-------------------------

Brighton, Md., Triadelphia Lake near---------------------------

Brink, Va., Fontaine Creek near--------------------------------

Broad Creek tributary at Whiteford, Md-------------------------

Broad Run at Buckland, Va--------------------------------------

near Warrenton, Va------------------------------------------

Broad Run tributary at Buckland, Va----------------------------

Brockway, Pa., Mill Creek near---------------------------------

Brokenstraw Creek at Youngsville, Pa---------------------------

Bronx River at Bronxville, N.Y---------------------------------

Bronxville, N.Y., Bronx River at-------------------------------

Broodmoor, Md., Baisman Run at---------------------------------

Brookneal, Va., Roanoke (Staunton) River at--------------------

Snake Creek near--------------------------------------------

Browns Branch tributary near Church Hill, Md-------------------

Browns Creek near Nineveh, Pa----------------------------------

Brownsville, W.Va., Skin Creek near----------------------------

West Fork River at------------------------------------------

Bruceville, Md., Big Pipe Creek at-----------------------------

Brushy Run near Petersburg, W.Va-------------------------------

Page

Buchanan, Va., James River at------------------------------- 2U7

Mill Creek near-------------------------------------------- 2U1

Buck, Pa ., Conowingo Creek near---------------------------- 171

Buckeye, W.Va., Greenbriar River at------------------------- 3'27

Buckhannon River at Hall, W.Va------------------------------ 307

Buckhannon, W.Va., Bridge Run near-------------------------- 306

Mud Lick Run near------------------------------------------ 306

Sand Run near---------------------------------------------- 307

Buckingham, Va., Frisby Branch near------------------------- 253

Buckland, Va., Broad Run at--------------------------------- 230

Broad Run tributary at----------------------------------- 2 31

Bucklodge Branch tributary near Barnesville, Md------------- 218

Buckstown, Pa., Clear Run near-------------------------------- 298

Buckton, Va., Passage Creek near------------------------------ 20°

Buena Vista, Va., Maury River near-------------------------- 2U8

Buffalo Creek at Barrackville, W.Va------------------------- 310

at Gardenville, N.Y---------------------------------------- 33U

near Freeport, Pa------------------------------------------ 305

near Hampden Sydney, Va------------------------------------ 257

near Romney, W.Va------------------------------------------ iqU

near Rowlesburg, W.Va-------------------------------------- 313

near Wales Hollow, N.Y------------------------------------- 335

Buffalo River near iye River, Va---------------------------- 250

Buffalo River tributary near Amherst, Va-------------------- 250

Buffalo Run tributary near Manns Choice, Pa----------------- 157

Bullpasture River at Williamsville, Va---------------------- 2bb

Bull Run near Catharpin, Va----------------------------------- 230

near Loganton, Pa----------------------------------------   1I9

near Manassas, Va---------------------------------------- 2 31

Bunch Creek near Boswells Tavern, Va------------------------ 2U0

Burdett, N.Y., Hector Falls Creek at------------------------ 3UU

Burketown, Va., North River near---------------------------- 20 5

Burke ville, Va., Nottoway River near----------------------- 260

Burton Creek tributary near Lynchburg, Va------------------- 2b 9

Bush Mill Stream near Heaths ville, Va---------------------- 235

Butcherville, W. Va., West Fork River at--------------------310

Butler Creek at Gibson, Pa------------------------------------ 132

Button Creek near Rustburg,	Va------------------------------- 270

Button Creek tributary near	Rustburg, Va---------------------- 270

Buttermilk Creek near Ithaca, N.Y--------------------------- 3UL

Butternut Creek at Morris> N»Y------------------------------ 115

near James ville, N.Y-------------------------------------- 35b

Bynum Run at Bel Air, Md------------------------------------ 17U

C

Cabins, W.Va., North Fork South Branch Potomac River at------- 503

Cabot, Pa., Little Buffalo Creek at------------------------- 305

Cacapon River above Wardensville, W.Va---------------------- -|_q8

near Great Ca capon, W.Va--------------------------------

Cain Branch near Chantilly, Va------------------------------ 230

Caldwell, W.Va., Howard Creek at---------------------------- 327

Calf pasture River above Mill Creek at Goshen, Va----------- 2U8

Camden-on-Gauley, W.Va., Gauley River at-------------------- 330

Cameron Run at Alexandria, Va------------------------------- 027

Camillus, N.Y., Ninemile Creek at--------------------------- 352

Campbell Creek near Kanona, N.Y----------------------------- 128

Campbell, N.Y., Cohocton River near------------------------- 128

Camp Hill, Pa., Yellow Breeches Creek near------------------ 167

Canacadea Creek at Alfred Station, N.Y---------------------- \2b

near Alfred, N.Y------------------------------------------- 123

near Horne 11, N.Y----------------------------------------- 125

Canacadea Creek tributary No. 1 at Alfred, N.Y-------------- 123

Canacadea Creek tributary No. 2 at Alfred, N.Y-------------- 123

Canadaraga Lake at Schuyler Lake, N.Y.---------------------- 113

Canandaigua Lake at Canandaigua, N.Y------------------------ 3U7

Canandaigua, N.Y., Canandaigua Lake at---------------------- 3U7

Canandaigua Outlet at Chapin, N.Y--------------------------- 3U7

Canasawaeta Creek near South Plymouth, N.Y------------------ 116

Canaseraga Creek at Canaseraga, N.Y------------------------- 338

near Dansville, N.Y---------------------------------------- 3U0

Canaseraga, N.Y., Canaseraga Creek	at----------------------- 338

Canisteo, N.Y., Bennetts Creek	at-------------------------- 126

Purdy Creek near------------------------------------------- 126

Canisteo River at Arkport, N.Y------------------------------ 122

at Bishopville, N.Y---------------------------------------- 123

at Erwins, N.Y----------------------............—........ 127

at West Cameron, N.Y--------------------------------------- 126

below Canacadea Creek at Horne11, N.Y-------------------- 12U

Canisteo River tributary near	Almond, N.Y--------------------- 123

Canisteo River tributary No. 2 near Almond, N.Y------------- 123

Page

129

256

268

321

212

231

295

31b

131

337

123

l6l

110

110

111

3^9

3b2

337

301

279

261

312

262

262

263

1U6

lU7

1U6

89

89

89

338

137

lb9

127

189

188

136

9b

17*»

309

2U0

137

172

2b2

280

280

323

129

139

107

109

109

19b

130

356

213

306

179

263

183

265

171

230

230

231

29b

287

91

91

177

269

271

112

316

309

309

212

19b﻿360

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Carney, MdLoch Raven Reservoir near----------------------

Carsonville, Pa., Clark Creek near-----------------------

Cartersville, Va., James River at----------------------—

CasseLman River at Grantsville, Md-----------------------

at Markleton, Pa--------------------------------------

Castle Fin, Pa., Muddy Creek at--------------------------

Catatonk Creek at Spencer, N.Y---------------------------

Catawba Creek near Catawba, Va---------------------------

Catawba, Va., Catawba Creek near-------------------------

Catharpin, Va., Bull Run near----------------------------

Catherine Creek near Montour Falls, N.Y------------------

Catherine Creek tributary No. k near Montour Falls, N.Y-

Catlett, Va., Cedar Run near-----------------------------

Catoctin Creek near Middletown, Md-----------------------

Cat Point Creek near Montross, Va------------------------

Cattail Creek at Roxbury Mills, Md-----------------------

Cattaraugus Creek at Gowanda, N.Y------------------------

Cattaraugus, N.Y., South Branch Cattaraugus Creek near—

Caughdenoy, N.Y., Oneida River at------------------------

Cayuga Creek near Lancaster, N.Y-------------------------

Cayuga Inlet at Ithaca, N.Y------------------------------

near .Ithaca, N.Y.------------------------------------

Cayuga Lake at Ithaca, N.Y-------------------------------

Cazenovia Creek at Ebenezer, N.Y-------------------------

Cedar Creek near Winchester, Va--------------------------

Cedarhurst, Md., North Branch Patapsco River at----------

Cedar Run near Catlett, Va-------------------------------

near Warrenton, Va------------------------------------

Cedar Run, Pa., Pine Creek at----------------------------

Cedar Run tributary near Culpeper, Va--------------------

Cedarville, Md., Wolf Den Branch near--------------------

Centerville, Del., Brandywine Creek tributary near-------

Centerville, Pa., Evitts Creek near----------------------

Centreville, Va., Big Rocky Run at Sully Road near-------

Cub Run near------------------------------------------

Chadakoin River at Falconer, N.Y-------------------------

Chadds Ford, Pa., Brandywine Creek at--------------------

Champlain, Va., Farmers Hall Creek near------------------

Chantilly, Va., Cain Branch near-------------------------

Cub Run near------------------------------------------

Flatlick Branch at Sully Road near--------------------

Chapin, N.Y., Canandaigua Outlet at----------------------

Chaptico Creek at Chaptico, Md---------------------------

Chaptico, Md., Chaptico Creek at-------------------------

Charleroi, Pa., Monongahela River at---------------------

Charlestown, Md., Northeast River tributary near---------

Charlotte Creek at West Davenport, N.Y-------------------

Charlottesville, Va., Moores Creek near------------------

Chatham, Va., Bearskin Creek near------------------------

Chautauqua Creek at Barcelona, N.Y-----------------------

Chautauqua Lake near Mayville, N.Y-----------------------

Cheat River at Rowlesburg, W.Va--------------------------

near Parsons, W.va------------------------------------

Chemung River at Chemung, N.Y----------------------------

near Big Flats, N.Y-----------------------------------

Chemung, N.Y., Chemung River «t--------------------------

Chenango Forks, N.Y., Chenango River near----------------

Chenango River at Eaton, N.Y-----------------------------

at Greene, N.Y----------------------------------------

at Sherburne, N.Y-------------------------------------

near Chenango Forks, N.Y------------------------------

Chenunda Creek at Stannards, N.Y-------------------------

Chenunda Creek tributary near Stannards, N.Y-------------

Cherry Tree, Pa., West Branch Susquehanna River at-------

Chester Creek near Chester, Pa---------------------------

Chesterfield, Md., Bacon Ridge Branch at-----------------

Chesterfield, Va., Falling Creek near--------------------

Chester, Pa., Chester Creek near-------------------------

Chester Springs, Fa., Pickering Creek near---------------

Cheswold, Del. Leipsic River near------------------------

Chickahominy River near Providence Forge, Va-------------

Christians Creek near Fishersville, Va-------------------

Christina River at Coochs Bridge, Del----------------------

Church Hill, Md., Browns Branch tributary near-----------

Church View, Va., Dragon Swamp near----------------------

Churchvilie, N.Y., Black Creek at------------------------

Cincinnatus, N.Y., Otselic River at----------------------

Clarion River at Cooksburg, Pa---------------------------

at Johnsonburg, Pa------------------------------------

at Ridgway, Pa----------------------------------------

Clarion River Dam, Pa., East Branch Clarion River at-----

Page

Clarion River Dam, Pa., East Branch Clarion River Lake at—	202

Clarion River near Piney, Pa--------------------------------- 29 5

Clark Creek near Carsonville, Pa----------------------------- 162

Clark Run near Bel Alton, Md--------------------------------- 232

Clarksburg, W.Va., West Fork River at------------------------ 310

Clarksville, Pa., Tenmile Creek near------------------------- 315

Clarkton, Va., Roanoke (Staunton) River at------------------- 270

Clayton, Del., Paw Raw Branch tributary near----------------- HI

Clear Creek near Sigel, Pa----------------------------------- 293

Clearfield Creek at Dimeling, Pa----------------------------- 139

at Irvona, Fa---------—----------------------------------- 13°

Clear Run near Buckstown, Pa-----------------— --------—— 298

Clements, Md., St. Clements Creek near----------------------- 233

Cleona, Pa., Beck Creek near--------------------------------- 167

Clifton Forge, Va., Cowpasture River near-------------------- 2UU

Cloverly, Md., Nursery Run at-------------------------------- 22U

Coate sville, Pa., Sucker Run near--------------------------- 1^6

West Branch Brandywine Creek at--------------------------- 105

Cobbs Creek at Darby, Pa------------------------------------- 100

at U.S. Highway No. 1 near Philadelphia, Pa--------------- 100

below Indian Creek, near Upper Darby, Pa------------------— 101

Cobun Creek at Morgantown, W.Va------------------------------ 310

Cochran, Va., Great Creek near------------------------------- ^63

Cocktown Creek near Huntingtown, Md-------------------------- 1®^

Codorus Creek at Spring Grove, Pa---------------------------- 1^9

near York, Pa--------------------------------------------- 1^9

Cogan House, Pa., Larrys Creek at---------------------------- 150

Cohocton, N.Y., Cohocton River at------------------

Cohocton River at Avoca, N.Y-----------------------

at Cohocton, N.Y----------------------------------

near Campbell, N.Y--------------------------------

Colesville, Md., Northwest Branch Anacostia River

near--------------------------------------------------------- 225

Colfax, W.Va., lygart Valley River at----------------------- 393

Colgrave, N.Y., Hunter Creek at----------------------------- 331*

College Park, Md., Paint Branch at Interstate

Highway 1+95 near------------------------------------- 222

Collegeville, Pa., Skippack Creek near------------------------ 97

Colonel Bill's Creek at South Canisteo, N.Y----------------- 126

Columbia Cross Roads, Pa., North Branch Sugar

Creek tributary near---------------------------------- 131

Columbia Furnace, Va., Pugh Run tributary near-------------- 209

Stony Creek at-------------------------------------------- 209

Comstock Brook at North Wilton, Conn------------------------ 89

Conemaugh River at Tunnel ton, Pa---------------------------- 303

at Seward, Pa--------------------------------------------- 300

Conemaugh River Dam, Fa., Conemaugh River Lake at----------- 303

Conemaugh River Lake at Conemaugh River Dam, Pa------------- 303

Conestoga Creek at Lancaster, Pa---------------------------- 171

Conesus Lake near Lakeville, N.Y----------------------------- 3L1

Conewango Creek at Russell, Pa------------------------------- 285

at Waterboro, N.Y----------------------------------------- 285

Confluence, Pa., Youghiogheny River below------------------- 320

Conicville, Va., Crooked Run tributary near----------------- 208

Conklin, N.Y., Susquehanna River at------------------------- 116

Connellsville, Pa., Youghiogheny River at-------------------- 322

Conococheague Creek at Fairview, Mi--------------------------- 201

near Fayetteville, Fa------------------------------------- 201

Conococheague Creek tributary at Kemps, Md------------------ 200

Conodoguinet	Creek near Hogestown,	Pa---------------------- 162

Conodoguinet	Creek tributary No. 1	near Enola, Pa---------16U

Conodoguinet	Creek tributary No. 3	at Enola, Fa----------16U

Conowingo Creek near Buck, Pa------------------------------- 171

Conowingo, Mi., Susquehanna River at------------------------- 171

Constantia, N.Y., Scriba Creek near------------------------- 356

Conway River near Stanardsville, Va------------------------- 236

Coochs Bridge, Del., Christina River at---------------------102

Cooksburg, Pa., Clarion River at----------------------------29U

Toms Run at------------------------------------------------293

Cooper Run near Green Bank,	W.Va-----------------------------235

Cootes Store, Va., North Fork	Shenandoah River at------------ 207

Corey Creek at Mansfield, Fa----------------------------------120

near Mainesburg, Fa----------------------------------------120

Corry, Pa., Hare Creek near-----------------------------------287

Corning, N.Y., Post Creek at--------------------------------128

Cortland, N.Y., Tioughnioga River at--------------------------117

Coudersport, Pa., Allegheny River at------------------------282

Mill Creek at-—------------------------------------------282

Covington, Va., Dunlap Creek near---------------------------21U

Potts Creek near-----------------------------------------21*5

Cowanesque River near Lawrenceville,	Pa----------------------121

Page

177

162

255

320

321

171

119

2U6

2U6

230

3U3

31*3

229

210

238

183

335

33^

357

33U

31*5

31*1*

31*6

335

208

179

229

228

1L 8

239

232

109

193

231

231

285

107

238

230

230

230

31*7

232

232

316

112

111*

255

278

331*

28U

313

312

130

129

130

119

117

117

117

119

336

336

137

102

182

256

102

95

111

259

20U

102

112

239

3l*2

118

29l*

292

293

292﻿INDEX TO STREAMFLOW DATA

361

Page

Page

Cowpasture River near Clifton Forge, Va-----------

Coy Glen Creek at Ithaca, N.Y---------------------

Crabtree Creek near Swanton, Mi-------------------

Craig Creek at Parr, Va---------------------------

near New Castle, Va----------------------------

Craig Creek tributary near New Castle, Va---------

Craigsville, W.Va., Gauley River near-------------

Cranberry Branch near Westminister, Md------------

Crooked Creek at Crooked Creek Dam, Pa------------

at Idaho, Pa-----------------------------------

at Tioga, ftt----------------------------------

Crooked Creek Dam, Pa., Crooked Creek at----------

Crooked Creek Lake at Crooked Creek Dam, Ra——■

Crooked Creek near Huntingdon, Ra-----------------

Crooked Run tributary near Conicville, Va---------

Cross Fork, Pa., Kettle Creek at------------------

Crozet, Va., Powells Creek near-------------------

Cryder Creek at Genesee, Pa-----------------------

Cuba, N.Y., Johnson's Creek at--------------------

Cub Creek at Rienix, Va---------------------------

Cub Run near Centreville, Va----------------------

near Chantilly, Va-----------------------------

Cub Run tributary near Montevideo, Va-------------

Culpeper, Va., Cedar Run tributary near-----------

Mountain Run near------------------------------

Rapidan River near-----------------------------

Cumberland, Md., North Branch Potomac River near-

Wills Creek near-------------------------------

Curwensville Lake near Curwensville, Pa-----------

Curwensville, Pa., Curwensville Lake near---------

West Branch Susquehanna River near-------------

-2UU -31+5 -189

_2 U T

-21+6 -2UT ,.331 -178 -299 -298 -121 -299 -299 -157 -208 -IU3 -252 -335 -282 -271 -231 -230 -207 -2 39 -237 -238 -191 -190 -138 -138 -138

D

Dailey, W.Va., lygart Valley River near-------------------

Daleville, Va., Tinker Creek near-------------------------

Dalmatia, Ra,, East Mahantango Creek near-----------------

Dan River at Danville, Va---------------------------------

at Paces, Va-------------------------------------------

near Francisco, N.C------------------------------------

near Wentworth, N.C------------------------------------

Dansville, N.Y., Canaseraga Creek near--------------------

Little Mill Creek near---------------------------------

Little Mill Creek tributary near-----------------------

Danville, Ra., Blizzard Run at----------------------------

Schler Run at------------------------------------------

Susquehanna River at-----------------------------------

Danville, Va., Dan River at-------------------------------

Sandy River near---------------------------------------

Darby Creek near Darby, Pa--------------------------------

near Waterloo Mills near Devon, Pa---------------------

Darby, Pa., Cobbs Creek at--------------------------------

Darby Creek near---------------------------------------

Darwin, N.Y., Onondaga Creek at---------------------------

Dauphin, Pa., Stony Creek near----------------------------

Davis, W.Va., Blackwater River at-------------------------

Dawsonville, Md., Seneca Creek at-------------------------

Dead Run at Franklintown, Md------------------------------

Deckers Creek at Morgantown, W.Va-------------------------

Deep Creek near Mannboro, Va------------------------------

Deep Creek Reservoir near Oakland, Md---------------------

Deer Creek at Rocks, Md-----------------------------------

near Kalmia, Md----------------------------------------

Deer Park, Md., Little Youghiogheny River tributary near-

Dendron, Va., Blackwater River near-----------------------

Denniston, Va., Hyco River near---------------------------

Devon, Ra., Darby Creek at--------------------------------

Difficult Run at Washington and Old Dominion

Railroad, near Vienna, Va--------------------------

near Great Falls, Va-----------------------------------

Dimeling, Ra., Clearfield Creek at------------------------

Dinwiddie, Va., Stony Creek near--------------------------

Ditch Run near Hancock, Md--------------------------------

Doctors Run at Arlington, Va------------------------------

Dodge Creek at Portville, N.Y-----------------------------

Dog Creek tributary near Locust Grove, Md-----------------

Doll Run at Red Lion, Del---------------------------------

Dollyhyce Creek at Libertytown, Md------------------------

Dorsey Run near Jessup, Md--------------------------------

Doswell, Va., Little River near---------------------------

North Anna River near----------------------------------

-306 -266 -15U -277 -277 -273 -27*+ -3U0 -339 -339 -137 -137 -136 -277 -276 -100 - 99 -100 .JL00

-163 -312 218 ’”l82 -311 -259 -318 -173 -173 -317 -262 -281 - 99

-220 -221 -139 -26l -199 -226 -282 -203 -110 -215 -18U —2Ul -21+1

Double Creek near Roseville, N.C-----------------------------278

Dover, Del., St. Jones River at------------------------------110

Downingtown, Pa., East Branch Brandywine Creek near----------106

Doyles River near Whitehall, Va------------------------------2 53

Dragon Swamp near Church View, Va----------------------------2 39

Dranesville, Va., Sugar land Run near------------------------219

Dresden, N.Y., Keuka Lake Outlet at--------------------------31+5

Driftwood Branch Sinnemahoning Creek at Emporium, Ra-----— ll+0

at Sterling Run, Pa---------------------------------------ll+O

Dry Fork at Hendricks, W.Va----------------------------------312

at White Sulphur Springs, W.Va----------------------------327

Dryden, N.Y., Virgil Creek at--------------------------------31+6

Dunbar, Pa., Gist Run near-----------------------------------322

Dunkard Creek at Shannopin, Ra-------------------------------315

Dunlap Creek near Covington, Va------------------------------21+1+

Dunning Creek at Belden, Pa-----------------------------------158

Durbin, W.Va., Greenbriar River at---------------------------32 5

Dyer, W.Va., Williams River at--------------------------------329

Dyke Creek at We 11svilie, N.Y-------------------------------336

near West Greenwood, N.Y-----------------------------------336

E

East Branch	Brandywine Creek near Down ingt own,	Pa---------106

East Branch	Byram River at Riversville, Conn---------------- $9

at Round Hill, Conn--------------------------------------- 88

East Branch	Canacadea Creek at Alfred Station,	N.Y--------123

East Branch	Chillisquaque Creek near Washingtonville, Ra---151+

East Branch Clarion River at East Branch Clarion

River	Dam, Pa-----------------------------------------292

East Branch Clarion River Lake at East Branch Clarion

River	Dam, Pa-----------------------------------------292

East Branch Codorus Creek tributary near

Winterstown, Pa-------------------------------------

East Branch Fish Creek at Taberg, N.Y-------------------

East Branch Herbert Run at Arbutus, Md------------------

East Conemaugh, Pa., Little Conemaugh River at----------

East Freedom, Ra., McDonald Run near--------------------

East Homer, N.Y., Albright Creek at---------------------

East Mahantango Creek near Dalmatia, Ra-----------------

Easton, Conn., Paterson Brook near----------------------

East Sidney Lake at East Sidney, N.Y--------------------

East Sidney, N.Y., East Sidney Lake at------------------

Ouleout Creek at-------------------------------------

East Valley Creek tributary near Andover, N.Y-----------

East Victor, N.Y., Mud Creek at-------------------------

East Waterford, Ra., Lick Run near----------------------

Eaton, N.Y., Chenango River at--------------------------

Eden, N.C., Smith River at------------------------------

Eighteenmile Creek at North Boston, N.Y-----------------

Ebenezer, N.Y., Cazenovia Creek at----------------------

Elders Branch near Hustontown, Ra-----------------------

Eldred, Pa., Allegheny River at-------------------------

Elimsport, Ra., White Deer Hole Creek near--------------

Elkins, W.Va., Tygart Valley River at-------------------

Elk Mills, Md., Big Elk Creek at------------------------

Elk River at Sutton, W.Va-------------------------------

below Webster Springs, W.Va--------------------------

Elk Run near Mainesburg, Ra-----------------------------

Elmira, N.Y., Newtown Creek at--------------------------

Seeley Creek near------------------------------------

Elmsford, N.Y., Rum Brook at----------------------------

Elm Valley Creek near Elm Valley, N.Y-------------------

Elm Valley, N.Y., Elm Valley Creek near-----------------

Elsmere, Del., Little Mill Creek at---------------------

Emlenton, Ra., Richey Run at----------------------------

Emporia, Va., Meherrin River at-------------------------

Emporium, Pa., Driftwood Branch Sinnemahoning Creek at-

Waldy Run near---------------------------------------

West Creek near--------------------------------------

English Center, Pa., Block House Creek near-------------

Enola, Pa., Conodguinet Creek tributary No. 1 near------

Conodoguinet Creek tributary No. 3 at----------------

Enterprise, W.Va., West Fork River at-------------------

Erwins, N.Y., Canisteo River at-------------------------

Mulholland Creek near--------------------------------

Tioga River near-------------------------------------

Etna, Pa., Little Pine Creek near-----------------------

Evingt on, Va., Big Otter River near--------------------

Evitts Creek near Centerville, Ra-----------------------

Ewart Creek at Swain, N.Y-------------------------------

,168

,35U

,180

,299

,155

,117

,15U

88

,115

,115

,115

,337

,31+6

,l6l

’ll7

275

,335

,335

,159

283

152

306

112

333

332

121

129

130 92

337

337 10U '291 261+ ll+O ll+l ll+0 ll+9 T61+ T61+ 311 127 127 127 30l+ 268 193

338﻿362

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

F

Page

Page

Fairviev, MdConococheaque Creek at---------------------------- 201

Falconer, N.Y., Chadakoin River at----------------------------285

Fall Creek near Ithaca, N.Y-----------------------------------3^7

Falling Creek near Chesterfield, Va--------------------------- 256

Falling River near Naruna, Va---------------------------------271

Falling Spring, Va., Jackson River at------------------------- 2kk

Falls Creek tributary near Victoria, Va---------------------— 260

Fanners Hall Creek near Champlain, Va-------------------------238

Farmville, Va., Appomattox River at--------------------------- 258

Fayetteville, N.Y., Limestone Creek at------------------------ 355

Fayetteville, Pa., Conococheaque Creek near-------------------201

Feathers Creek near Belmont, N.Y------------------------------337

Fern Cliff, Va., Big Lickinghole Creek tributary near---------256

Ferndale, Pa., Stony Creek at---------------------------------297

Fincastle, Va., North Fork near-------------------------------3U7

Fine Creek at Fine Creek Mills, Va----------------------------256

First Fork Sinnemahoning Creek near Sinnemahoning, Pa---------1U3

First Fork Sinnemahoning Creek Reservoir near

Sinnemahoning, Pa----------------------------------------lU2

Fishersville, Va., Christians Creek near----------------------20h

Fishing Creek at Mill Hall, Ra--------------------------------n+ 8

near Bloomsburg, Pa-----------------------------------------136

near Lewistown, Md------------------------------------------21 h

Fivemile Creek near Kanona, N.Y-------------------------------128

Fivemile River near Norwalk, Conn----------------------------- 88

Flanagan Mills, Va., Willis River at--------------------------255

Flatlick Branch at Sully Road near Chantilly, Va--------------230

Flint Creek at Phelps, N.Y-------------------------------------3^9

at Potter, N.Y-----------------------------------------------3^8

Flinton, Pa., Glendale Lake at Prince Gallitzin

State Park near------------------------------------------138

Fontaine Creek near Brink, Va---------------------------— 265

Forest City, Pa., Lackawanna River near------------------------133

Stillwater Lake near----------------------------------------132

Fort Run near Moorefield, W.Va---------------------------------19 ^

Fort Washington, Kt., Wissahickon Creek at---------------------- 98

Pine Run tributary at---------------------------------------- 98

Foster Joseph Sayers Lake near Blanchard, Pa------------------ 1^7

Fourmile Run at Alexandria, Va------------------------------— 226

Foxtown, Md., North Branch Casselman River tributary at——-- 320

Francisco, N.C., Dan River near---------------------------------273

Franklin, Md., Georges Creek at---------------------------------190

Franklin, Pa., Allegheny River at-------------------------------290

Patchel Run near--------------------------------------------290

Franklintown, Md., Dead Run at---------------------------------l82

Franklin, Va., Blackwater River near----------------------------263

Franklin, W.Va., Friends Run near------------------------------193

South Branch Potomac River at-------------------------------192

Unnamed Run on North Fork Mountain near---------------------193

Frankstown Branch,Juniata River at Williamsburg, Pa----------- 156

Frederick, Md., Linganore Creek near Frederick, Md------------ 215

Monocacy River at Jug Bridge---------------------------------2lU

Fredericksburg, Va., Rappahannock River near------------------2 39

Freeport, Pa., Buffalo Creek near-----------------------------30 5

French Creek at Utica, Pa-------------------------------------29 0

near Rioenixville, Pa---------------------------------------- 95

near Union City, Pa------------------------------------------289

Friendship, N.Y., Van Campen Creek at-------------------------337

Friends Run near Franklin, W.Va-----------------------------— 193

Friendsville, I Id., Bear Creek at------------------------------319

Youghiogher.y River at---------------------------------------319

Frisby Branch near Buckingham, Va—1---------------------------253

Front Royal, Va., Happy Creek at------------------------------210

South Fork Shenandoah River at------------------------------ 206

Frostburg, Md., Savage River near-------------------------------188

Frying Km Branch near Herndon, Va-----------------------------216

Fullmer Valley Creek near Ha11sport, N.Y---------------------- 336

Fullmer Valley Creek tributary near Andover, N.Y-------------- 336

G

Galeton, Pa., Pine Creek at------------------------------------lU8

Ganargua Creek at Macedon, N.Y.--------------------------------3k6

Garbutt, N.Y., Oatka Creek at---------------------------------- 3^1

Gardenville, N.Y., Buffalo Creek at..........................— 33U

Garrisonville, Va., A quia Creek near--------------------------2 33

Gauley River at Camden-on-Gauley, W.Va-------------------------330

below Summersville Dam, W.Va--------------------------------330

near Craigsville, W.Va------------------------------------— 331

Qenesee, Pa., Cryder Creek at----------------------------------335

Genesee River at Avon, N.Y-------------------------------------3U1

Genesee River at Portageville, N.Y-------------------

at Rochester, N.Y----------------------------------

at Scio, N.Y..........................-............

at Stannards, N.Y----------------------------------

near Mount Morris, N.Y-----------------------------

Georges Creek at Franklin, Md------------------------

near Gretna, Va------------------------------------

at Smithfield, Pa..................................

Germania Branch at Germania, Pa-----------------------

Germania, Pa., Germania Branch at---------------------

Gettysburg, Pa., White Run near-----------------------

Gibson, Pa., Butler Creek at--------------------------

Gillespie Run near Sutersville, Pa--------------------

Gilman, W. Va., Unnamed Run at------------------------

Gilmer Run near Marlinton, W.Va-----------------------

Gingoteague Run near Port Royal, Va-------------------

Gist Run near Dunbar, Pa------------------------------

Glade Run at Muncy, Pa--------------------------------

Glebe Branch at Valley Lee, Md------------------------

Glendale Lake at Prince Gallitzin State Park near

Flinton, Pa------------------------------------

Glennmoore, Pa., Marsh Creek near---------------------

Glyndon, Md., Slade Run near--------------------------

Goff Creek near Avoca, N.Y----------------------------

Goff Creek tributary near Howard, N.Y-----------------

GoIdvein, Va., Rock Run tributary near----------------

Goose Creek near Huddleston, Va-----------------------

near Leesburg, Va----------------------------------

near Middleburg, Va--------------------------------

Gordonsville, Va., Mountain Run tributary near--------

Goshen, Va., Calfpasture River above Mill Creek at—

Gowanda, N.Y., Cattaraugus Creek at-------------------

Graceton, Pa., Two Lick Creek at----------------------

Grafton, W.Va., Right Fork Wickwire Run on

U.S. Highway 119 near--------------------------

Tygart Lake near-----------------------------------

Grand Valley, Pa., West Branch Caldwell Creek near—

Grantsville, Md., Casselman River at------------------

Graterford, Pa., Perkiomen Creek at-------------------

Great Cacapon, W.Va., Cacapon River near--------------

Great Creek near Cochran, Va--------------------------

Great Falls, Va., Difficult Run near------------------

Rock Run near---------------------------------------

Great Mills, Md., St. Mary’s River at------------

Green Bank, W.Va., Cooper Run near--------------------

Greenbriar River at Alderson, W.Va--------------------

at Buckeye, W.Va------------------------------------

at Durbin, W.Va-------------------------------------

at Hilldale, W.Va-----------------------------------

Greene, N.Y., Chenango River at-----------------------

Greenfield, Va., Rockfish River near------------------

Green Lane, Pa., Green Lane Reservoir at--------------

Green Lane Reservoir at Green Lane Pa-----------------

Green Lick Reservoir, Pa., Green Lick Run at----------

Green Lick Run at Green Lick Reservoir, Pa------------

Green Meadows, Md., Sligo Creek at--------------------

Greensboro, Pa., Monongahela River at-----------------

Greenwood, N.Y., Bennetts Creek tributary at----------

Griffith Creek near Alderson, W.Va--------------------

Grimes, Md., Marsh Run at-----------------------------

Gretna, Va., Georges Creek near-----------------------

Whitehorn Creek tributary near----------------------

Grottoes, Va., Middle River near----------------------

Guffey, Pa., Kinzua Creek near------------------------

Guilford Downs, Md., Little Phtuxent River tributary

at--------------------------------------------------

Guilford, Md., Little Kituxent River at---------------

Gum Springs, Va., Rocketts Creek tributary near-------

Gwynns Falls at McDonogh, Md--------------------------

at Villa Nova, Md..................................

near Owings Mills, Md------------------------------

-339

•3U3

-336

-336

•	3Uo -190 .278

•	3lU

.1U3

.1U3

-212

.132

.322

.307

•	331 .239

■	322 ■152 ■234

■138

■107

■175

■128

■	127

■	236

•	269

•	216 • 216

■	2U0 . 2U8

335 • 302

308

309 . 289

320

97

198

263

221

221

23b

325

329

327 325

328 117 251

96

96

323

323

227

3lb

126

329

203

278

279

205

283

185

185

256

181

181

181

H

Halifax, Va., Banister at------------------

Hall, W.Va., Buckhannon River at-----------

Hallsport, N.Y., Fullmer Valley Creek near-

Hammondsport, N.Y., Keuka Lake at----------

Keuka Lake tributary No. 13 near----------

Hampden Sydney, Va., Buffalo Creek near----

Hancock, Md., Ditch Run near---------------

279 307 3 36 3^U 3bb

257

199﻿INDEX TO STREAMFLOW DATA

363

Page

Page

Hancock, Md., Potomac River at---------------------------

Potomac River tributary near---------------------------

Haneytown Creek near Stanardsville, Va-------------------

Hanover, Va., Pamunkey River near------------------------

Happy Creek at Front Royal, Va---------------------------

Harbor Brook at Hiawatha Boulevard, Syracuse, N.Y--------

at Syracuse, N.Y---------------------------------------

Hardware River below Briery Run, near Scottsville, Va---

Hare Creek near Corry, Pa--------------------------------

Harman, W.Va., Horse Camp Run at-------------------------

Harmony, Md., Little Catoctin Creek at-------------------

Harpers Run near Morrisville, Va-------------------------

Harper Tavern, Pa., Swatara Creek at---------------------

Harrisburg, Pa., Paxton Creek at Wildwood Lake at--------

Susquehanna River at-----------------------------------

Harris Creek near Trevilians, Va-------------------------

Harriston, Va., South River at---------------------------

Hayfield, Va., Hogue Creek near--------------------------

Hay Meadow Branch tributary at ftjplar Springs, Md-------

Hazel River at Rixeyville, Va----------------------------

Headsville, W.Va., Patterson Creek near------------------

Heathsville, Va., Bush Mill Stream near------------------

Hector Falls Creek at Burdett, N.Y-----------------------

Henderson Creek near Shadwell, Va------------------------

Hendricks, W.Va., Dry Fork at----------------------------

Henryton, Md., South Branch Pa tapsco River at-----------

Henson Creek at Qxon Hill, Md----------------------------

Hereford, Md., Piney Creek near--------------------------

Prettyboy Reservoir near-------------------------------

Herndon, Va., Frying Ran Branch near---------------------

Horsepen Run at Sully Road near------------------------

Merrybrook Run at Sully Road near----------------------

Higgins, N.Y., Sixtown Creek at--------------------------

Hightowers, N.C., South Country Line Creek near----------

Hilldale, W.Va., Greenbriar River at---------------------

Hinton, Va., War Branch near-----------------------------

Hoekessin, Del., Mill Creek at---------------------------

Hogestown, Pa., Conodoguinet Creek near------------------

Hog Rock Creek near Moores Springs, N.C------------------

Hogue Creek near Hayfield, Va----------------------------

Holiday Creek near Andersonville, Va---------------------

Holcombs Rock, Va., James River at---------------———

Hollofield, Md., Patapsco River at---------------------—

Hollow Road Creek near Middletown, Md--------------------

Holmes Run near Annandale, Va----------------------------

Homer City, lb., Yellow Creek near-----------------------

Honey Brook, Pa., West Branch Brandywine Creek near------

Honeoye Creek at Honeoye Falls, N.Y----------------------

Honeoye Falls, N.Y., Honeoye Creek at--------------------

Honeoye Lake near Honeoye, N.Y-----------------—---------

Honeoye, N.Y., Honeoye Lake near-------------------------

Hopwood, Pa., Lick Run at--------------------------------

Horne11, N.Y., Canacadea Creek near----------------------

Canisteo River below Canacadea Creek at----------—

Horse Camp Run at Harman, W.Va---------------------------

Horseheads, N.Y., Newtown Creek at-----------------------

Horsepen Run at Sully Road, near Herndon, Va-------------

Hoskins Creek near Tappahannock, Va----------------------

Howard Creek at Caldwell, W.Va---------------------------

Howard, N.Y., Goff Creek tributary near------------------

Hoyes Run, Md., Toliver Run tributary near----------------

Huddleston, Va., Goose Creek near-------------------------

Hunter Creek at Colgrave, N.Y----------------------------

Hunters Branch near Palmyra, Va--------------------------

Huntersville, W.Va., Moody Moore Hollow near--------------

Hunting Creek at Jimtown, Md------------------------------

Huntingdon, Pa., Crooked Creek near-----------------------

Juniata River at---------------------------------------

Raystown Branch Juniata River below Raystown Dam near-

Ray stown Branch Juniata River near--------------------

Huntington Creek near Pikes Creek, Pa---------------------

Huntington, W.Va., Ohio River at--------------------------

Ohio River at 2l*th Street-----------------------------

Huntingtown, Md., Cocktown Creek near---------------------

Hurricane Branch near Blackstone, Va----------------------

Hustontown, Pa., Elders Branch near-----------------------

Hutchinson River at Pelham, N.Y---------------------------

Hyattsville, Md., Northwest Branch Anacostia River near-

Hyco Creek near Leasburg, N.C-----------------------------

Hyco River at McGehees Mill, N.C—-------------------------

near Denniston, Va-------------------------------------

____199

____199

___25b

'~~2b2

"III210

IIII352 ____351

____252

____287

____311

____211

____237

____166

___167

____165

____2bl

206

II”l99

180

236

.193

___235

3U

IIII255

___312

“”3.80

IIII227

___175

___175

___216

___216

___215

___338

___276

___328

____205

____105

____162

____273

----199

----256

____2U9

___l8l

____211

___226

___301

____105

___3Ul

____3Ul

___3U0

___3U0

____317

___125

____12U

___311

___129

___216

___238

___327

___127

___318

-.269

___33lt

„25lt

326

___2lU

IIII157

___156

....158

___159

136

33U

333

186

II"26l

---159

--- 90

___227

___278

___280

___281

Hyndman, Pa., Wills Creek below-

.190

I

Idaho, Pa., Crooked Creek at---------------------

Idlewylde, Md., West Branch Herring Run at-------

Independent Hill, Va., South Fork Quantico Creek

near-------------------------------------------

Index, N.Y., Oaks Creek at-----------------------

Indiana, Pa., Stony Run at-----------------------

Indian Creek near Andover, N.Y-------------------

Indian Draft near Marlinton, W.Va----------------

Indian Rock Reservoir near York, Pa--------------

Irvona, Pa., Clearfield Creek at-----------------

North Whitmer Run at---------------------------

Ithaca, N.Y., Buttermilk Creek near--------------

Cayuga Inlet at--------------------------------

Cayuga Inlet near------------------------------

Cayuga Lake at---------------------------------

Coy Glen Creek at------------------------------

Fall Creek near--------------------------------

Six Mile Creek at Fotlers Falls near-----------

Six Mile Creek above---------------------------

Six Mile Creek tributary near------------------

Itaska, N.Y., Bioughnioga River at---------------

.298

.177

-232 .113 .300 .337 .326 .16 9 .139 .139 31*1 .3b$ 3bk 31*6 .31*5 .3U7 .31*5 .31*5 .31*5 119

Jackson River at Falling Spring, Va--------------------------2UU

Jackson Run near North Warren, Pa---------------------------2®6

Jacobs Creek near Wentworth, N.C-----------------------------2?1*

James River at Bent Creek, Va--------------------------------250

at Buchanan, Va-------------------------------------------2i*7

at Cartersville, Va--------------------------------------2 5 5

at Holcombs Rock, Va--------------------------------------2i*9

at Lick Run, Va-------------------------------------------2 ^5

at Scottsville, Va-----------------------------------------252

near Richmond, Va------------------------------------------257

James ville, N.Y., Butternut Creek near-------------------—35 j*

Jefferson, Ra., South Fork Tenmile Creek at------------------316

Jessup, Md., Dorsey Run near--------------------------------1®~*

Jimtown, Md., Hunting Creek at-------------------------------21 ^

John H. Kerr Reservoir near Boydton, Va----------------------2®0

Johns Creek at New Castle, Va--------------------------------2j* ®

Johns Creek tributary near New Castle, Va--------------------

Johnsonburg, Pa., Clarion River at----------------------------92

Johnson's Creek at Cuba, N.Y-

82

Jones Falls at Sorrento, Md----------------------------------183

Jones Springs, W.Va., Back Creek near------------------------200

Josephine, Pa., Blacklick Creek at---------------------------301

Juniata River	at Huntingdon, Ra-----------------------------156

at Mapleton	Depot, lb-------------------------------------158

at Newport,	Pa--------------------------------------------l6l

at Warrior Ridge Dam,	Pa----------------------------------156

K

Kalmia, Md., Deer Creek near---------------------------------173

Kanona, N.Y., Campbell Creek near----------------------------12®

Fivemile Creek near---------------------------------------12®

Karr Valley Creek near Almond, N.Y---------------------------i2i*

Kashong Creek near BeIlona, N.Y-Karthaus, Pa., West Branch Susquehanna River at-Keene, Va., Thomas Creek near-

Kendig Creek near MacDougall, N.Y-

Kennedyville, Md., Morgan Creek near----------------

Kernesville, N.C. Belews Creek near-----------------

Kerrs Creek near Lexington, Va----------------------

Kettle Creek at Cross Fork, Pa----------------------

near Westport, Pa-------*-------------------------

Kettle Creek Lake near Westport, Tb-----------------

Keuka Lake at Hammondsport, N.Y---------------------

Keuka Lake Outlet at Dresden, N.Y-------------------

Keuka Lake tributary No. 12 near Pulteney, N.Y------

Keuka Lake tributary No. 13 near Hammondsport, N.Y-

Keysville, Va., North Meherrin River near-----------

Kilgore Creek tributary near Leasburg, N.C----------

Kingston, Pa., Loyalhanna Creek at------------------

Kinzua Creek near Guffey, Pa------------------------

Kinzua, Pa., Allegheny Reservoir near---------------

3 U5 ,11*0

,2 52

Kemps, Md., Conococheague Creek tributary at----------------2p°

.31*5 -111 .272 _2l*9 _11* 3 ll*l* .11*1* 3U1*

131*5

3l*l+

3U1*

J6 3 .278 ’302

"283

”281*﻿364

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Page

Page

Kirkwood Creek near Kirkwood, N.Y----------------

Kirkwood, N.Y., Kirkwood Creek near--------------

Kishacoquillas Creek at Reedsville, Pa-----------

Kiskinlinetas River at Vandergrift, Pa----------

Kittanning, Pa., Allegheny River at--------------

Kitzmiller, Md., North Branch Potomac River at-

126

126

160

30U

297

186

L

Lackawanna River at Archbald, Pa-------------------------------133

at Old Forge, Pa----------------------------------------------13^

near Forest City, Pa------------------------------------------133

Lafayette, Va., Roanoke River at-------------------------------26U

Lakeland, N.Y., Ninemile Creek at------------------------------353

Lakeville, N.Y., Conesus Lake near------—--------—-----------—3^1

Lancaster, N.Y., Cayuga Creek near-----------------------------33*+

Lancaster, Pa., Conestoga Creek at-----------------------------171

Landenberg, Pa., Middle Branch White Clay Creek near-----------

Lantz, Md., Owens Creek at--------------------------------------213

Largo, Md., Western Branch near--------------------------------

Larrys Creek at Cogan House, Pa--------------------------------150

Laurel Brook, Md., Little Gunpowder Falls at-------------------^6

Laurel Hill Creek at Ursina, lb.-------------------------------320

Laurel, Md., Patuxent River near-------------------------------1®5

T. Howard Duckett Reservoir near-----------------------------1®**

Laurel Mills, Va., Battle Run near-----------------------------235

Lawrenceville, Pa., Cowanesque River near----------------------121

Lawrenceville, Va., Meherrin River near----------------------—262

Lawsons Creek near Tubeville, Va--------------------------------277

Lawsonville, N.C., Little Snow Creek near----------------------272

Layhill, Md., Bel Pre Creek at---------------------------------22U

Leaksville, N.C., Matrimony Creek near-------------------------275

Leasburg, N.C., Hyco Creek near--------------------------------278

Kilgore Creek tributary near----------------------------------278

Leesburg, Va., Goose Creek near------------------------------—216

South Fork Sycolin Creek near--------------------------------217

Lees ville Lake near Lees ville, Va----------------------------2°°

Leesville, Va., Leesville Lake near----------------------------268

Leipsic River near Cheswold, Del---------------------------—m

Lenah Run at Lenah, Va-----------------------------------------217

Lenah, Va., Lenah Run at---------------------------------------217

Lenhartsville, Pa., Maiden Creek tributary at------------------9^

Leslie, Md., Northeast Creek at--------------------------------H3

Levels, W.Va., Little Cacapon River near-----------------------197

Lewisburg, Pa., West Branch Susquehanna River at---------------153

Lewistown, Md., Fishing Creek near-----------------------------214

Lexington, Va., Kerrs Creek near-------------------------------249

Liberty Grove, Md., Basin Run at-------------------------------1^2

Liberty Reservoir near Marriottsville, Md----------------------1^9

Libertytown, Md., Dollyhyde Creek at---------------------------215

Lick Run at Hopwood, Pa----------------------------------------317

near East Waterford, Pa---------------------------------------1~1

Lick Run, Va., James River at----------------------------------24 5

Limestone Creek at Fayetteville, N.Y---------------------------®^5

Lindley, N.Y., Tannery Creek near-------------------------------123

Tioga River at------------------------------------------------122

Linganore Creek near Frederick, Md------------------------------215

Little Buffalo Creek at Cabot, Fa------------------------------30 5

Little Cacapon River near Levels, W.Va-------------------------^97

Little Catoctin Creek at Harmony, Md---------------------------

Little Conemaugh River at East Conemaugh, Pa--------------------299

Little Conneauttee Creek near McKean, Pa-----------------------289

Little Crum Creek at Swathmore, Pa---------------------------—^

Little Falls Branch near Bethesda, Md--------------------------220

Little Genesee Creek at Little Genesee, N.Y------------------ oAo

Little Genesee, N.Y., Little Genesee Creek at------------------282

Little Gunpowder Falls at Laurel Brook, Md---------------------

Little Juniata River at Spruce Creek, Pa-----------------------

at Tipton, Pa---------------------------------------------—

Little Lost Creek at Oakland Mills, Pa-------------------------

Little Mahoning Creek at McCormick, Pa-------------------------297

Little Mill Creek at Elsmere, Del------------------------------101*

near Dansville, N.Y------------------------------------------339

Little Mill Creek tributary near Dansville, N.Y----------------339

Little Patuxent River at Guilford, Md—--------------------——185

at Savage, Md-----------■-------------------------------——J.8U

Little Patuxent River tributary at Guilford Downs, Md----------185

Little Pine Creek near Etna, Pa--------------------------------30U

Little Pipe Creek at Avondale, Md------------------------------2 12

Little River near Doswell, Va----------------------------------21+1

Little Schuylkill River at Tamagua, Pa------------------

Little Snow Creek near Lawsonville, N.C-----------------

Little Wills Creek at Bard, Pa--------------------------

Little Yellow Creek near Strongstown, Pa----------------

Little Youghiogheny River tributary near Deer Park, Md-

Liverpool, N.Y., Onondago Lake at-----------------------

Loch Raven Reservoir near Carney, Md--------------------

Locust Dale, Va., Robinson River near-------------------

Locust Grove, Md., Dog Creek tributary near-------------

Loganton, Pa., Bull Run near----------------------------

Long Branch at Arlington Boulevard near Vienna, Va------

at Arlington, Va-------------------------------------

at Vienna, Va----------------------------------------

Long Run near Parsons, W.Va-----------------------------

Lost River at McCauley, near Baker, W.Va----------------

Lovingston, Va., lye River near-------------------------

Loyalhanna Creek at Kingston, Pa------------------------

at Loyalhanna Dam, Pa--------------------------------

Loyalhanna Dam, Pa., Loyalhanna Creek at----------------

Loyalhanna Lake at-----------------------------------

Loyalhanna Lake at Loyalhanna Dam, Pa-------------------

Loyalsock Creek at Loyalsockville, Pa----------------—

Loyalsockville, Pa., Loyalsock Creek at-----------------

Loysville, Pa., Bixler Run near-------------------------

Lucky Run at Arlington, Va------------------------------

Ludlowville, N.Y., Salmon Creek at----------------------

Luke, Md., North Branch Potomac River at----------------

Lunenburg, Va., North Meherrin River near---------------

Luray, Va., South Fork Shenandoah River tributary near-

Lutes Run at Lutes, Md----------------------------------

Luzerne, Pa., Toby Creek at-----------------------------

Lycoming Creek near Trout Run, Pa-----------------------

Lykens, Pa., Rattling Creek at--------------------------

Wiconisco Creek at-----------------------------------

Lynchburg, Va., Burton Creek tributary near-------------

lynch, Pa., Tionesta Creek at---------------------------

lynch River near Nortonsville, Va-----------------------

Lyndell, Pa., Marsh Creek near--------------------------

Iynnwood, Va., South Fork Shenandoah River near---------

■ 93 .272 .190 .300 .317 .35^ .177 .237 .203 .lh9 .229 .226 .229 .312 .197 .250 .302 .303 .303 .303 .303 .150 .150 .161 .226 .3U7 .189 .262 .206 .225 .23U .151 .155 .155 2U9 .287 .25U .106 .207

M

Mac Dougall, N.Y., Kendig Creek near-----------

Macedon, N.Y., Ganargua Creek at---------------

Mahoning Creek at Mahoning Creek Dam, Pa-------

at Punxsutawney, Pa-------------------------

Mahoning Creek Dam, Pa., Mahoning Creek at-----

Mahoning Creek Lake at----------------------

Mahoning Creek Lake at Mahoning Creek Dam, Pa-Maiden Creek tributary at Lenhartsville, Pa---

Mainesburg, Pa., Corey Creek near--------------

Elk Run near--------------------------------

Mamaroneck, N.Y., Beaver Swamp Brook at--------

Mamaroneck River at-------------------------

Sheldrake River at--------------------------

Mamaroneck River at Mamaroneck, N.Y------------

at Winfield Avenue, Mamaroneck, N.Y---------

Manassas, Va., Bull Run near-------------------

Occoquan River near-------------------------

Manatawny, Pa., Pine Creek near---------------

Manchester, Pa., West Conewago Creek near------

Mannboro, Va., Deep Creek near-----------------

Manns Choice, Pa., Buffalo Run tributary near-

Manns Creek near Mansfield, Pa-----------------

Manor Run near Norbeck, Md---------------------

Mansfield, Pa., Corey Creek at-----------------

Manns Creek near----------------------------

Tioga River at------------------------------

Mapleton Depot, Pa., Juniata River at----------

Marietta, N.Y., Ninemile Creek near------------

Marietta, Pa., Susquehanna River at------------

Marietta, Ohio, Ohio River near----------------

Markleton, Pa., Casselman River at-------------

Marlinton, W.Va., Gilmer Run near--------------

Indian Draft near---------------------------

Marriottsville, Md., Liberty Reservoir near—

Marsh Creek at Blanchard, Pa-------------------

near Glennmoore, Pa-------------------------

near lyndell, Pa----------------------------

Marsh Run at Grimes, Md.-----------------------

Martinsburg, W.Va., Opequon Creek near---------

.3U5

.3 U6 .296 .296 .296 296 296 . 9h 120 ’l21

! 90 . 91 . 91 . 91 . 91

.231 .231 - 9^ .168 .259 .157 .121 .223 .120 .121 .121 .158

.353 .170 m32h \321 .331 .326 .179 .1U6 .107 .106 .203

201﻿INDEX TO STREAMFLOW DATA

365

Page

Page

Martinsburg, W.Va., Tuscarora Creek above--------------------

Tuscarora Creek near mouth below--------------------------

Martinsville, Va., Smith River at----------------------------

Marvin Creek at Smethport, Pa--------------------------------

Matoaca, Va., Appomattox River at----------------------------

Matrimony Creek near Leaksville, N.C-------------------------

Mattavoman Creek near Pomonkey, Md---------------------------

Mattoax, Va., Appomattox River at----------------------------

Mattaponi River near Beulahville, Va-------------------------

near Bowling Green, Va------------------------------------

Maury River at Rockbridge Baths, Va--------------------------

near Buena Vista, Va--------------------------------------

Mayo River near Price, N.C-----------------------------------

Mayville, N.Y., Chautouqua Lake near-------------------------

McCormick, Ra., Little Mahoning Creek at---------------------

McDonald Run near East Freedom, Pa---------------------------

McDonogh, Md., Gwynns Falls at-------------------------------

McGehees Mill, N.C., Hyco River at---------------------------

McHenry Valley Creek tributary No. 1 near Alfred, N.Y--------

McHenry Valley Creek tributary No. 2 near Alfred, N.Y--------

McKean, Pa., Little Conneauttee Creek near-------------------

McLean, Va., Scott Run near----------------------------------

Meadow Brook at Hurlburt Road, Syracuse, N.Y-----------------

Meherrin River at Emporia, Va--------------------------------

near Lawrenceville, Va------------------------------------

Merrybrook Run at Sully Road, near Herndon, Va---------------

Middle Branch White Clay Creek near Landenberg, Pa-----------

Middle Branch Wyalusing Creek tributary near

Birchardville, Pa-------------------------------------

Middleburg, Va., Goose Creek near----------------------------

Middle Fork River at Audra, W.Va-----------------------------

Middle River near Grottoes, Va-------------------------------

near Verona, Va-------------------------------------------

Middlesex, N.Y., West River near-----------------------------

Middletown, Md., Catoctin Creek near-------------------------

Hollow Road Creek near------------------------------------

Milesburg, Pa., Bald Eagle Creek below Spring Creek at-------

Spring Creek at-------------------------------------------

Mill Branch near Mitchellville, Md---------------------------

Mill Creek at Coudersport, Pa--------------------------------

at Hockessin, Del-----------------------------------------

at Patchinville, N.Y--------------------------------------

at Sinclairville, N.Y-------------------------------------

near Brockway, Pa-----------------------------------------

near Buchanan, Va-----------------------------------------

near Warrensville, Pa-------------------------------------

Mill Hall, Pa., Fishing Creek at-----------------------------

Millington, Md., Unicorn Branch near-------------------------

Millville, W.Va., Shenandoah River at------------------------

Minister Creek near Truemans, Pa-----------------------------

Mink Creek at Richfield Springs, N.Y-------------------------

Mitchellville, Md., Mill Branch near-------------------------

Patuxent River at U.S. Highway 50 near--------------------

Modena, Pa., West Branch Brandywine Creek at-----------------

Monocacy River at Bridgeport, Md-----------------------------

at Jug Bridge near Frederick, Md--------------------------

Monongahela River at Braddock, Pa----------------------------

at Charleroi, Pa------------------------------------------

at Greensboro, Pa-----------------------------------------

Monroeton, Pa., Towanda Creek near---------------------------

Montdale, Pa., South Branch Tunkhannock Creek near-----------

Montevideo, Va., Cub Run tributary near----------------------

Montour Falls, N.Y., Catherine Creek tributary No. 4 near—

Montour, N.Y., Catherine Creek near--------------------------

Montross, Va., Cat Point Creek near--------------------------

Montvale, Va., South Fork Goose Creek at---------------------

Monument, Pa., Beech Creek near------------------------------

Moody Moore Hollow near Huntersville, W.Va-------------------

Moon Creek near Yanceyville, N.C-----------------------------

MoorefieId, W.Va., Fort Run near-----------------------------

South Fork South Branch Potomac River near----------------

Williams Hollow near--------------------------------------

Moores Creek near Charlottesville, Va------------------------

Moores Springs, N.C., Hog Rock Creek near--------------------

Moravia, N.Y., Owasco Inlet at-------------------------------

Morgan Creek near Kennedyville, Md---------------------------

Morgantown, W.Va., Cobun Creek at----------------------------

Deckers Creek at—-----------------------------------------—

Morris, N.Y., Butternut Creek at-----------------------------

Morrisville, Va., Harpers Run near---------------------------

Moshannon Creek at Osceola Mills, Pa-------------------------

202

203

275

283

258

275

231

258

2k2

2h2

2k8

2h8

27h

28k

297

155

181

280

12U

12k

289

221

355

261*

262

216

102

—	131

—	216

—	306

—	205

—	20k

—	3U6

—	210 — 211

—	lU6

—	1U5 -185

—	282

—	105

—	339

—	281*

—	291*

—	21*7

—	151

__lU8

__110

__210

__288

__113

-185

—	185 —106

—	213

—	211*

—	323

—	316

—	311*

—	130

—	132

—	207

—	31*3

—	3l*3 238

_ 268

__11* 8

__326

276 __ 191+

—	195 191+

—	255 .273

3k9 111 II310

__311

115

237

“ll*0

Moshannon Creek at Phillipsburg, Pa--------------------------ll*0

Mountain Grove, Va., Back Creek near-------------------------21*3

Mountain Run near Culpeper, Va-------------------------------2 37

Mountain Run tributary near Gordonsville, Va-----------------21*0

Mt. Airy, Va., Blacks Creek near-----------------------------279

Mount Jackson, Va., North Fork Shenandoah River at-----------208

Mount Morris Lake near Mount Morris, N.Y---------------------338

Mount Morris, N.Y., Genesee River near-----------------------31+0

Mount Morris Lake near-------------------------------------338

Mount Storm, W.Va., Stony River	near------------------------187

Mud Creek at East Victor, N.Y--------------------------------31*6

near Savona, N.Y-------------------------------------------129

Mud Creek tributary near Bradford, N.Y-----------------------129

Mud Lick Run near Buckhannon, W.Va---------------------------306

Muddy Creek at Castle Fin, Ra--------------------------------171

Muddy Run near Standardsville, Va----------------------------2 53

Mulholland Creek near Erwins, N.Y----------------------------127

Muncy Creek near Sonestown, Pa-------------------------------151

Muncy, Pa., Glade Run at--------------------------------------152

Murrysville, Pa., Abers Creek near----------------------------323

N

'Nantawny, Pa., Pine Creek near------------------------

Naples, N.Y., Reservoir Creek at-----------------------

Naruna, Va., Falling River near------------------------

Naticoke Creek at Union Center, N.Y--------------------

Natrona, Ra., Allegheny River at-----------------------

Nedrow, N.Y., Onondaga Reservoir near------------------

Needmore, Ph., Tonoloway Creek near--------------------

Neils Creek near Bloomerville, N.Y---------------------

Nettleridge, Va., South Mayo River near----------------

New Albany, Pa., South Branch Towanda Creek at---------

Newark, Del., Pike Creek near--------------------------

White Clay Creek above------------------------------

White Clay Creek near-------------------------------

Newburg, Ra., Newburg Run at---------------------------

Newburg Run at Newburg, Pa-----------------------------

New Castle, Va., Craig Creek'near----------------------

Craig Creek tributary near--------------------------

Johns Creek at--------------------------------------

Johns Creek tributary near--------------------------

Newell Creek near Port Allegany, Pa--------------------

Newfield, N.Y., West Branch Cayuga Inlet at------------

Newington, Va., Accotink Creek near--------------------

New Market, Va., Smith Creek near----------------------

Newport, Pa., Juniata River at-------------------------

Newtown Creek at Elmira, N.Y---------------------------

at Horseheads, N.Y----------------------------------

Niagara, Va., Roanoke River at-------------------------

Nibbs Creek tributary near Amelia, Va------------------

Ninemile Creek at Camillus, N.Y------------------------

at Lakeland, N.Y------------------------------------

near Marietta, N.Y----------------------------------

Nineveh, Ra., Browns Creek near------------------------

Norbeck, Md., Manor Run near---------------------------

North Branch Rock Creek near------------------------

Normalville, Pa., Poplar Run near----------------------

North Anna River near Doswell, Va----------------------

North Boston, N.Y., Eighteenmile Creek at--------------

North Branch Casselman River tributary at Foxtown, Md-

North Branch Patapsco River at Cedarhurst, Md----------

North Branch Phillips Creek at Withey, N.Y-------------

North Branch Potomac River at Barnum, W.Va-------------

at Kitzmiller, Md...................................-

at Luke, Md-----------------------------------------

at Pinto, Md----------------------------------------

near Cumberland, Md---------------------------------

North Branch Rock Creek near Norbeck, Md---------------

North Branch Sugar Creek tributary near Columbia

Cross Roads, Pa---------------------------------

North Cameron, N.Y., Stocking Creek tributary at-------

Northeast Branch Anacostia River at Riverdale, Md------

Northeast Creek at Leslie, Md--------------------------

Northeast River tributary near Charlestown, Md---------

North Fork Moormans River near Whitehall, Va-----------

North Fork near Fincastle, Va--------------------------

North Fork Rivanna River near Proffit, Va--------------

North Fork Shenandoah River at Cootes Store, Va--------

at Mount Jackson, Va--------------------------------

near Strasburg, Va----------------------------------

■ 9k • 3U6 .271 .118 •30U

-127 -272 -131 -103 -103 -10U -162 -162 —2U6 -21*7 ,.21+6 -21+6 -282 ..31*1* -228 -207 l6l -179 ..129 -267 -259 -352 —353 ..353 ..316 ..223 ..222 -321 -2 Ul -335 -320 -179 -337 -187 ,_l86

, J-89 -191 —191 -222

—131 -129 ,.222 .113 ..112 -2 53 ..21*7 I25I+ ”207 ‘208 ’>09﻿366

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Page

Page

North Fork Shenandoah River tributary near Waterlick, North Fork South Branch Potomac River at Cabins, W.Va North Garden, Va., South Branch North Fork Hardware

River near--------------------------------------

North Home 11, N.Y., Big Creek near--------------------

North Mayo River near Spencer, Va----------------------

North Meherrin River near Briery, Va-------------------

near Keysville, Va----------------------------------

near Lunenburg, Va----------------------------------

North River near Annapolis, Md-------------------------

near Burketown, Va----------------------------------

near Stokesville, Va--------------------------------

North Warren, Pa., Jackson Run near--------------------

Northwest Branch Anacostia River at Norwood, Md--------

near Colesville, Mi---------------------------------

near Hyattsville, Md--------------------------------

North Whitmer Run at Irvona, Pa------------------------

North Wilton, Conn., Comstock Brook near---------------

Nortonsville, Va., Lynch River near--------------------

Norwood, Md., Northwest Branch Anacostia River---------

Nottoway River near Burkeville, Va---------------------

near Rawlings, Va-----------------------------------

near Sebrell, Va------------------------------------

near Stony Creek, Va--------------------------------

Norwalk, Conn, Fivemile River near---------------------

Norwalk River at South Wilton, Conn--------------------

Nursery Run at Cloverly, Md----------------------------

Va-----209

.......193

_______252

.......123

.......273

.......263

_______263

.......262

.......182

.......205

_______204

.......286

.......223

.......22 5

......_227

......-139

......89

......254

.......223

_______260

.......26l

.......26l

......260

.......88

.......88

....._22h

0

Oakdale, Md., Batchellors Run at-----------------

Oakland, Md., Deep Creek Reservoir near-------

Youghiogheny River near-----------------------

Oakland Mills Pa., Little Lost Creek at----------

Oakmont, W.Va., Abram Creek at-------------------

Oaks Creek at Index, N.Y-------------------------

Oatka Creek at Garbutt, N.Y----------------------

at Warsaw, N.Y--------------------------------

Occoquan River near Manassas, Va-----------------

Octoraro Creek near Rising Sun, Md---------------

Ohio River at Huntington, W.Va-------------------

at Point Pleasant, W.Va-----------------------

at Point Pleasant, W.Va. (auxilary gage)------

at Pomeroy, Ohio------------------------------

at St. Marys, W.Va----------------------------

at Sewickley, Pa------------------------------

at 24th Street, Huntington, W.Va--------------

near Marietta, Ohio---------------------------

near Waverly, W.Va----------------------------

Oil Creek at Rouseville, Pa----------------------

Old Forge, Pa., Lackawanna River at-----------—

Oldtown, Md., Sawpit Run near--------------------

Town Creek near-------------------------------

Olean Creek near Olean, N.Y----------------------

Olean, N.Y., Olean Creek near--------------------

Olney, Md., Williamsburg Run near----------------

Oneida Creek at Oneida, N.Y----------------------

Oneida Lake at Brewerton, N.Y--------------------

Oneida River at Caughdenoy, N.Y------------------

Onondaga Creek at Dorwin, N.Y--------------------

at Spencer Street, Syracuse, N.Y--------------

Onondago Lake at Liverpool, N.Y------------------

Onondaga Reservoir near Nedrow, N.Y--------------

Ono, Pa., Reeds Creek near-----------------------

Opequon Creek near Berryville, Va—---------------

near Martinsburg, W.Va------------------------

Orebed Creek near Stannards, N.Y-----------------

Osceola Mills, F&., Moshannon Creek at-----------

Ossian, N.Y., Sugar Creek near-------------------

Oswego, N.Y., Oswego River at Lock 7-------------

Oswego River at Lock rJ} Oswego, N.Y-------------

Otselic River at Cincinnatus, N.Y----------------

Otto, N.Y., South Branch Cattaraugus Creek near-

Ouleout Creek at East Sidney, N.Y----------------

Owasco Inlet at Moravia, N.Y---------------------

Owasco Lake near Auburn, N.Y---------------------

Owasco Outlet near Auburn, N.Y-------------------

Owego Creek near Owego, N.Y----------------------

Owego, N.Y, Owego Creek near---------------------

Pumpelly Creek at-----------------------------

Owens Creek at Lantz, Md-------------------------

..225 ,_318 -317 -160 .J.87 -113 -341 -341 -231 .JL73 -334 ,_332 -333 -324 -325 -324 -333 -324 -325 -289 . JL 3 4 ■-197 ,-196 -282 -282 -221 •-355 ..356

-357

-351

-350

-354

-350

-166

-200

-201

-336

-104

-339

-357

-357

-118

-334

-115

-349

-348

.348

.118

-118

.118

.213

Owens Creek tributary near Rocky Ridge, Md-----------------213

Owings Mills, Md., Gwynns Falls near-----------------------l8l

Qxon Hill, Md., Henson Creek at----------------------------227

P

Paces, Va., Dan River at-------------------------------------227

Paint Branch at Interstate Highway 495 near College

Park, Md---------------------------------------------222

Palmyra, Va., Hunters Branch near----------------------------2 54

Rivanna River at-----------------------------------------2 55

Pamunkey River near	Hanover,	Va----------------------------242

Parker Branch near Stanardsville, Va-------------------------253

Parker, Pa., Allegheny River at------------------------------294

Park Mills, Md., Bennett Creek at----------------------------—215

Farr, Va., Craig Creek at------------------------------------247

Parsons, W.Va., Cheat River near------------------------------312

Long Run near---------------------------------------------312

Right Fork Clover Run near--------------------------------312

Shavers Fork at-------------------------------------------313

Passage Creek near Buckton, Va--------------------------------209

Patapsco River at Hollofield, Md-----------------------------18l

Patchel Run near Franklin, Pa--------------------------------290

Patchinville, N.Y.,	Mill	Creek	at--------------------------339

Paterson Brook near Easton, Conn----------------------------- 88

Patterson Creek near Headsville, W.Va------------------------19 3

Patuxent River at U.S. Highway 50 near Mitchellville, Md-----185

near Laurel, Md-----------------------------------------  185

near Unity, Md--------------------------------------------183

Paw Paw Branch tributary near Clayton, Del-------------------111

Paw Paw, W.Va., Potomac River at-----------------------------196

Paxton Creek at Wildwood Lake at Harrisburg, Pa--------------167

near Penbrook, Fa-----------------------------------------167

Pelham, N.Y., Hutchinson River at---------------------------- 90

Fanbrook, Pa., Paxton Creek near-----------------------------167

Fanfield, Pa., Wilson Run at---------------------------------l4l

Penhook, Va., Smith Mountain Lake near-----------------------266

Banns Creek at Penns Creek, Pa-------------------------------144

Perkiomen Creek at Graterford, Pa----------------------------- 97

Petersburg, W.Va., Brush Run near----------------------------194

South Branch Potomac River near--------------------------194

Phelps, N.Y., Flint Creek at----------------------------------349

Phenix, Va., Cub Creek at-------------------------------------271

Philadelphia, Pa., Cobbs Creek near---------------------------100

Schuylkill River at--------------------------------------- 99

Wissahickon Creek at Livzey Lane at------------------------- 99

Wissahickon Creek at mouth at----------------------------  99

Fhilippi, W.Va., Bonica Run on U.S. Highway 25O near---------209

lygart Valley River at-----------------------------------30 8

Phillipsburg, Pa., Moshannon Creek at-----------------------  140

Phillips Creek at Withey, N.Y---------------------------------332

Philpott Lake near Philpott, Va-------------------------------27 5

Philpott, Va., Philpott Lake near----------------------------275

Smith River near------------------------------------------274

Phoenixville, Pa.,	French	Creek near---------------------------95

Pickering Creek near Chester Springs, Pa---------------------95

Pigg River near Sandy Level, Va------------------------------267

Pike Creek near Newark, Del----------------------------------10 3

Pikes Creek, Pa., Huntington Creek near----------------------136

Pine Creek at Cedar	Run,	Pa--------------------------------148

at Galeton, Pa--------------------------------------------148

below Little Pine Creek near Waterville Pa---------------1^9

near Manatawny, Pa—------------- —.......................94

Pine Run tributary at Fort Washington, Pa--------------------98

Piney Creek near Hereford, Md--------------------------------175

Piney Creek tributary at Taneytown, Md-----------------------213

Piney, Pa., Clarion River near-------------------------------295

Piney River at Piney River, Va-------------------------------251

Piney River, Va., Piney River at-------------------------------251

Piney Run at Res ton, Va-------------------------------------221

near Sykesville, Md--------------------------------------1®1

Pinto, Md., North Branch Potomac River at--------------------191

Piscataway Creek at Piscataway, Md-----

near Tappahannock, Va---------------

Piscataway, Md., Piscataway Creek at--Point of Rocks, Md., Potomac River at-

Point Pleasant, W.Va., Ohio River at-------------------------332

Point Pleasant, W.Va. (auxilary gage),Ohio River at----------3 33

Pomeroy, Ohio, Ohio River at---------------------------------324

Pomonkey, Md., Mattawoman Creek near-------------------------2 31

Poplar Run near Normalville, Pa------------------------------321﻿INDEX TO STREAMFLOW DATA

367

Poplar Springs, Md., Hay Meadow Branch Tributary at-

Po River near Spotsylvania, Va-----------------------

Portageville, N.Y., Genesee River at-----------------

Port Allegany, Pa., Newell Creek near----------------

Port Royal, Va., Gingoteague Run near----------------

Portville, N.Y., Dodge Creek at----------------------

Posd Creek at Corning, N.Y---------------------------

Potato Creek at Smethport, Pa------------------------

Potomac River at Hancock, Md-------------------------

at Paw Paw, W.Va-—-------------—----—--------------

at Point of Rocks, Md------------------------------

at Shepherdstown, W.Va-----------------------------

near Washington, D.C-------------------------------

Potomac River tributary near Hancock, Md-------------

Potter, N.Y., Flint Creek at-------------------------

Potts Creek near Covington, Va-----------------------

Pottstown, Pa., Schuylkill River at------------------

Powder Mill Creek at Rocky Mount, Va-----------------

Fowelis Creek near Crozet, Va---------------------—

Pratt Hollow tributary at Pratt, Md------------------

Pratt, Md., Pratt Hollow tributary at----------------

Prettyboy Reservoir near Hereford, Md----------------

Price, N.C., Mayo River near-------------------------

Principio Creek near Principio Furnace, Md-----------

Principio Furnace, Md., Principio Creek near---------

Proffit, Va., North Fork Rivanna River near----------

Providence Forge, Va., Chickahominy River near-------

Pugh Run tributary near Columbia Furnace, Va---------

Pulteney, N.Y., Keuka Lake tributary No. 12 near-----

Pumpelly Creek at Owego, N.Y-------------------------

Pinxsutawney, Pa., Mahoning Creek at-----------------

Purchase, N.Y., Blind Brook near---------------------

Blind Brook tributary at---------------------------

Purdy Creek near Canisteo, N.Y-----------------------

Q

Quarryville, Pa., Bowery Run near— Quig Hollow Brook near Andover, N.Y-

R

Railroad Brook near Alfred, N.Y------------------

Randolph, Va., Roanoke (Staunton) River at-------

Rappahannock River at Remington, Va--------------

Rapidan River near Culpeper, Va------------------

near Ruckersville, Va--------------------------

near Stanardsville, Va-------------------------

Rappahannock River near Fredericksburg, Va-------

near Warrenton, Va-----------------------------

Rasselas, Pi., Seven Mile Run near---------------

Rattling Creek at Iykens, Pa---------------------

Rawlings, Va., Nottoway River near---------------

Raystown Branch Juniata River at Saxton, Pa-------

below Raystown Dam near Huntingdon, Pa---------

near Huntingdon, Pa----------------------------

Reading, Pa., Tuplehocken Creek near-------------

Reamstown, Pa., Stony Run at---------------------

Redbank Creek at St. Charles, Pa------------------

Red Clay Creek at Wooddale, Del-------------------

Red Clay Creek tributary near Yorklyn, Del--------

Redding, Conn., Saugatuck River near--------------

Red Lion, Del., Doll Run at-----------------------

Redstone Creek at Waltersburg, Pa-----------------

Reeds Creek near Ono, Pa--------------------------

Reedsville, Pa., Kishacoquillas Creek at—---------

Remington, Va., Rappahannock River at-------------

Renovo, Pa., West Branch Susquehanna River at-----

Young Womans Creek near------------------------

Reservoir Creek at Naples, N.Y--------------------

Reston, Va., Piney Run at-------------------------

Smilax Branch at-------------------------------

Stave Run at-----------------------------------

Richey Run at Emlenton, Pa------------------------

Richfield Springs, N.Y., Mink Creek at------------

Richmond, Va., James River near-------------------

Ridgway, Pa., Clarion River at--------------------

Right Fork Clover Run near Parsons, W.Va----------

Right Fork Wickwire Run on U.S. Highway 119 near

Grafton, W.Va------------------------------

Right Hand Fork near Appomattox, Va—

Page

Page

180

2U3

339

282

239

282

128

283

199

196

211

202

220

199

3U8

2U5

9h 2 66 252 196

196

175

27h

112

112

25h

259

209

3UU

118

296

89

89

126

172

337

337

271

236

238

237 236

239 23^ 291 155 26l 159 15°

159 9h

171 295 105 105 89 110 317 166

160 236 1^5 lUU 3U6 220 217 217 291 113 257 293 312

308

271

Ringtown, Pa., Trexler Run near----------------------

Rising Sun, Md., Octoraro Creek near-----------------

Risingville, N.Y., South Branch Michigan Creek near-

Rivanna River at Palmyra, Va-------------------------

Riverdale, Md., Northeast Branch Anacostia River at-

Riversville, Conn., East Branch Byram River at-------

Rixeyville, Va., Hazel River at----------------------

Roanoke Creek at Saxe, Va----------------------------

Roanoke Rapids, N.C., Roanoke River at---------------

Roanoke (Staunton) River at Altavista, Va------------

at Brookneal, Va-----------------------------------

at Clarkton, Va------------------------------------

at Randolph, Va------------------------------------

Roanoke River at Lafayette, Va-----------------------

at Niagara, Va-------------------------------------

at Roanoke Rapids, N.C-----------------------------

at Roanoke, Va-------------------------------------

Robinson River near Locust Dale, Va------------------

Rochester, N.Y., Allen Creek near-----------------—

Genesse River at-----------------------------------

Rockbridge Baths, Va., Maury River at----------------

Rock Creek at Sherrill Drive, Washington, D.C--------

Rockdale, N.Y., Unadilla River at-----------------—

Rocketts Creek tributary near Gum Springs, Va--------

Rockfish River near Greenfield, Va-------------------

Rockland, Del., Willow Run at------------------------

Rock Run near Great Falls, Va------------------------

Rock Run tributary near Goldvein, Va-----------------

Rocks, Md., Deer Creek at----------------------------

Rockville, Md., Watts Branch at----------------------

Rockville, W.Va., Big Sandy Creek at-----------------

Rocky Mount, Va., Powder Mill Creek at---------------

Rocky Ridge, Md., Owens Creek tributary near---------

Romney, W.Va., Buffalo Creek near--------------------

Roseville, N.C., Double Creek near-------------------

South Hyco Creek near------------------------------

Rossville, Md., Stemmers Run at-—-----------------—-

Rorick Hollow Creek near Breesport, N.Y--------------

Round Hill, Conn., East Branch Byram River at--------

Rouseville, Pa.., Oil Creek at-----------------------

Rowlesburg, W.Va., Buffalo Creek near----------------

Cheat River at-------------------------------------

Roxboro, N.C., Storys Creek near---------------------

Roxbury Mills, Md., Cattail Creek at-----------------

Ruckersville, Va., Rapidan River near----------------

Rum Brook at Elms ford, N.Y--------------------------

Rush River at Washington, Va-------------------------

Russell, Pa., Akeley Run near------------------------

Conewango Creek at---------------------------------

Rustburg, Va., Button Creek near---------------------

Button Creek tributary near------------------------

Rye, N.Y., Beaver Swamp Brook at---------------------

Blind Brook at-------------------------------------

137

173

128

255

222

89

236

272

28l

269

269

270

271 26U 267

28l

31*3

3U3

2U8

223

115

256

251

109

221

236 173 220 31 .266 213 191* 278

279 178 130

88

289

313

313

280 183

237 92

235

286

285

270

270

90

89

S

Saint Charles, Pa., Redbank Creek at-------------------------295

Saint Clement Creek near Clements, Md------------------------233

Saint Jones River at Dover, Del------------------------------ 110

Saint Mary’s River at Great Mills, Md------------------------231*

Saint Marys, W.Va., Ohio River at---------------------------- 32h

Salamanca, N.Y., Allegheny River at-------------------------- 282

Salisbury, Pa., Big Piney Run near--------------------------- 321

Salmon Creek at Ludlowville, N.Y----------------------------- 3^7

Sand Run near Buckhannon, W.Va------------------------------- 307

Sand Spring Run near White Deer, Pa--------------------------153

Sandy Level, Va., Pigg River near---------------------------- 267

Sandy River near Danville, Va-------------------------------- 276

Sandy Run near Bellwood, Pa---------------------------------- 156

Sasco Brook near Southport, Conn-----------------------------

Saugatuck River near Redding, Conn--------------------------- 89

Savage, Md., Little Patuxent River at------------------------l®14

Savage River below Savage River Dam, near

Bloomington, Md---------------------------------------- 189

near Barton, Md------------------------------------------   188

near Frostburg, Md----------------------------------------- 188

Savage River Reservoir near Bloomington, Md------------------ 188

Savona, N.Y., Mud Creek near--------------------------------- 129

Saw Mill Branch tributary near Blackbird, Del---------------- HI

Saw Mill River at Yonkers, N.Y------------------------------- 92

Sawpit Run near Oldtown,	Md-------------------------------- 197﻿368

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

Page

Page

Saxe, Va., Roanoke Creek at------------------------------

Saxton, Ife., Raystown Branch Juniata River at-----------

Schell Run at Tyrone, Ra---------------------------------

Schenevus Creek at Schenevus, N.Y------------------------

Schenevus, N.Y., Schenevus Creek at----------------------

Scio, N.Y., Genesee River at-----------------------------

Snowball Hollow Creek near----------------------------

Vandermark Creek near---------------------------------

Schler Run at Danville, Pa-------------------------------

Schuyler, N.Y., Canadarago Lake at-----------------------

Schuylkill River at Berne, Ra----------------------------

at Philadelphia, Pa-----------------------------------

at Pottstown, Pa--------------------------------------

Scott Run near McLean, Va--------------------------------

Scottsville, Va., James River at-------------------------

Hardware River below Briery Run near------------------

Scriba Creek near Constantia, N.Y------------------------

Sebrell, Va., Nottoway River near------------------------

Second Creek near Second Creek, W.Va---------------------

Second Creek, W.Va., Second Creek near-------------------

Seeley Creek near Elmira, N.Y----------------------------

Seneca Creek at Dawsonville, Md--------------------------

Seneca Lake at Watkins Glen, N.Y-------------------------

Seneca River at Baldwinsville, N.Y-----------------------

Seven Mile Run near Rasselas, Pa-------------------------

Seward, Pa., Conemaugh River at--------------------------

Sewickley, Pa., Ohio River at----------------------------

Shadwell, Va., Henderson Creek near----------------------

Shamokin Creek near Shamokin, Ra-------------------------

Shamokin, Ra., Shamokin Creek near-----------------------

Shannopin, Pa., Dunkard Creek at-------------------------

Sharpsburg, Md., Antietam Creek near---------------------

Shavers Fork at Parsons, W.Va----------------------------

Shawsville, Va., South Fork Roanoke River near-----------

Sheldrake River at Mamaroneck, N.Y-----------------------

Shellpot Creek at Wilmington, Del------------------------

Shenandoah River at Millville, W.Va----------------------

Shepherdstown, W.Va., Potomac River at-------------------

Sherburne, N.Y., Chenango River at-----------------------

Sherman Creek at Shermans Dale, Pa-----------------------

Shermans Dale, Pa., Sherman Creek at---------------------

Sideling Hill Creek near Beliegrove, Md------------------

Sigel, Pa., Clear Creek near-----------------------------

Silvara, Pa., Tuscarora Creek near-----------------------

Sinclairville, N.Y., Mill Creek at-----------------------

Singsing Creek near Big Flats, N.Y-----------------------

Sinnemahoning Creek at Sinnemahoning, Pa-----------------

Sinnemahoning, Ra., First Fork Sinnemahoning Creek near-

First Fork Sinnemahoning Creek Reservoir near---------

Sinnemahoning Creek at--------------------------------

Six Mile Creek at Potter Falls above Ithaca, N.Y---------

near Ithaca, N.Y-------------------------------------

Six Mile Creek tributary near Ithaca, N.Y----------------

Sixtown Creek at Higgins, N.Y----------------------------

Skaneateles Lake at Skaneateles, N.Y---------------------

Skaneateles, N.Y., Skaneateles Lake at-------------------

Skin Creek near Brownsville, W.Va------------------------

Skippack Creek near Collegeville, Ra---------------------

Skippack, Pa., Zacharias Creek near----------------------

Slade Run near Glyndon, Md-------------------------------

Slate River near Arvonia, Va-----------------------------

Sligo Creek at Green Meadows, Md-------------------------

Smethport, Pa., Marvin Creek at--------------------------

Potato Creek at--------------------------------------

Smilax Branch at Reston, Va------------------------------

Smith Creek near New Market, Va--------------------------

Smithfield, Pa., Georges Creek at------------------------

Smith Mountain Lake near Rsnhook, Va---------------------

Smith River at Bassett, Va-------------------------------

at Eden, N.C------------------------------------------

at Martinsville, Va-----------------------------------

near Philpott, Va------------------------------------

Snake Creek near Brookneal, Va---------------------------

Snowball Hollow Creek near Scio, N.Y---------------------

Snow Shoe, Ra., South Fork Beech Creek near--------------

Solomon Creek at Wilkes-Barre. Ra------------------------

Sonestown, Ra., Money Creek near-------------------------

Sorrento, Md., Jones Falls at----------------------------

South Addison, N.Y., Tuscarora Creek near----------------

South Anna River near Ashland, Va------------------------

South Anna River tributary near Ashland, Va--------------

-272

-159

-157

-llU

-11**

-336

-337

-337

-137

-113

92

-	99

-	9** -221 -252 -252 -356 -26l -328 .328 -130 -218 —3**3 —3**9 -291 -300

32U -2 55 -155 -155 —315 -20 3 -313 .. 26 b

-	91 -10 3 -210 -202 -117 -162 -162 .-197 -293 -132 -28** -129 -lUl -lU3 ._1**2 ...11*1 -3U5

__3** 5

__3U5

-338 __3**9 —3**9 —309

-	97

-	96 —175 -253 —227 —283 —283 —218 —207 —31** -266

__27**

-275 -275 —27** —271 -337 __1**7 -135 -151 -183 -127 —2Ul ..2Ul

South Branch Cattaraugus Creek near Cattaraugus, N.Y---------33**

near Otto, N.Y--------------------------------------------3 3**

South Branch Codorus Creek near York, Pa---------------------169

South Branch Michigan Creek near Risingville, N.Y------------128

South Branch North Fork Hardware River, near

North Garden, Va-------------------------------------2 52

South Branch Patapsco River at Henry ton, Md-----------------180

South Branch Potomac River at Franklin, W.Va-----------------192

near Petersburg, W.Va-------------------------------------19**

near Springfield, W.Va------------------------------------19 5

South Branch Towanda Creek at New Albany, Pa-----------------131

South Branch Tunkhannock Creek near Montdale, Pa-------------132

South Canisteo, N.Y., Colonel Bill's Creek at----------------126

South Country Line Creek near Hightowers, N.C—----------------276

South Dansville,	N.Y.,	Sponable Creek near------------------339

South Dansville,	N.Y.,	Stony Brook at-----------------------339

South Fork Beech	Creek	near Snow Shoe,	Pa------------------1**7

South Fork Broad	Run near Areola, Va------------------------216

South Fork Goose	Creek	at Montvale, Va---------------------268

South Fork QuanDico Creek near Independent Hill Va-----------232

South Fork Roanoke River near Shawsville, Va-----------------26b

South Fork Shenandoah River at Front Royal, Va---------------206

near Lynnwood, Va------------------------------------------207

South Fork Shenandoah River tributary near Luray, Va---------206

South Fork South Branch Potomac River at Brandywine, W.Va—19**

near Moorefield, W.Va-------------------------------------19 5

South Fork Sycolin Creek near Leesburg, Va-------------------217

South Hyco Creek near Roseville, N.C.------------------------279

South Fork Tenmile Creek at Jefferson, Ra--------------------316

South Mayo River near Nettleridge, Va------------------------272

South Plymouth, N.Y., Canasawacta	Creek near---------------116

Southport, Conn., Sasco Brook near--------------------------- 88

South River at Harr is ton, Va-------------------------------20 6

near Steeles Tavern, Va-----------------------------------2*+ 8

near Waynesboro, Va---------------------------------------20 5

South Wilton, Conn., Norwalk River at------------------------ 88

Spencer, N.Y., Catatonk Creek at-----------------------------119

Spencer, Va., North Mayo River near--------------------------273

Sponable Creek near South Dansville, N.Y---------------------339

Spotsylvania, Va., Po River near-----------------------------2*+3

Sprankle Mills, Pa., Big Run near----------------------------29 5

Spring Creek at Milesburg, Ra--------------------------------1**5

at Spring Creek, W.Va--------------------------------------326

near Axemann, Pa----------------------------------------1 ** 5

Springfield, W.Va., South Branch Potomac River---------------19 5

Spring Grove, Pa., Codorus Creek at--------------------------169

Springmills Creek at Springmills, N.Y------------------------335

Springmills, N.Y., Springmills Creek at----------------------3 35

Springwater Creek at Springwater, N.Y------------------------3**0

Springwater, N.Y., Springwater Creek at----------------------3*+ 0

Spruce Creek, Pa., Little Juniata River at-------------------156

Stanardsville, Va., Conway River near-------------------------2 36

Haneytown Creek near---------------------------------------254

Muddy Run near---------------------------------------------253

Parker Branch near-----------------------------------------253

Rapidan River near-----------------------------------------236

Swift Run tributary near----------------------------------2 5**

Stannards, N.Y., Chenunda Creek at----------------------------336

Chenunda Creek tributary near------------------------------336

Genesee River at-------------------------------------------336

Orebed Creek near------------------------------------------336

Stave Run at Reston, Va--------------------------------------217

Steeles Tavern, Va., South River near------------------------2U8

Stemmers Run at Rossville, Md--------------------------------178

Stemmers Run, Md., Brien Run at-------------------------------179

Sterling Creek at Sterling, N.Y------------------------------3**2

Sterling, N.Y., Sterling Creek at----------------------------3**2

Sterling Run Ra., Driftwood Branch Sinnemahoning Creek at—1^®

Stillwater Lake near Forest City, Ra--------------------------132

Stocking Creek tributary at North Cameron, N.Y---------------i29

Stockton Creek near Afton, Va---------------------------------252

Stokesville, Va., North River near---------------------------20 ^

Stony Brook at South Dansville, N.Y---------------------------^39

Stony Creek at Columbia Furnace, Va---------------------------209

at Ferndale, Pa--------------------------------------------2^9

near Dauphin, fh--------------------------------------------^3

Stony Creek, Va., Nottoway River near-------------------------2^®

Stony River near Mount Storm, W.Va---------------------------

Stony Run at Indiana, Pa------------------------------------- 800

Reamstown, Pa----------------------------------------------171﻿INDEX TO STREAMFLOW DATA

369

Page

Page

Storys Creek near Roxboro, N.C--------------------

Strasburg, Va., North Fork Shenandoah River near-

Strongstown, Pa., Little Yellow Creek near--------

Sucker Run near Coatesville, Pa-------------------

Sugar Creek at Sugar Creek, Pa--------------------

near Ossian, N.Y-------------------------------

Sugar Creek, Pa., Sugar Creek at------------------

Sugarland Run near Dranesville, Va----------------

Summersville Dam, W.Va., Gauley River below-------

Summersville Lake near Summersville, W.Va---------

Summersville, W.Va., Summersville Lake near-------

Sunbury, Pa., Susquehanna River at----------------

Susquehanna River at Conklin, N.Y-----------------

at Conowingo, Md-------------------------------

at Danville, Pa--------------------------------

at Harrisburg, Pa------------------------------

at Marietta, Pa--------------------------------

at Sunbury, Pa---------------------------------

at Towanda, Pa---------------------------------

at Unadilla, N.Y-------------------------------

at Vestal, N.Y.................................-

at West Pittston, Pa---------------------------

at Wilkes-Barre, Pa—---------------------------

near Waverly, N.Y------------------------------

Sutersville, Pa., Gillespie Run near--------------

Youghiogheny River at-----------------—--------

Sutton Lake at Sutton, W.Va-----------------------

Sutton, W.Va., Elk River at-----------------------

Swain, N.Y., Ewart Creek at-----------------------

Swanton, Md., Crabtree Creek near-----------------

Swatara Creek at Harper Tavern, Pa----------------

Swarthmore, Pa., Little Crum Creek at-------------

Swift Run tributary near Stanardsville, Va--------

Sykesville, Md., Piney Run near-------------------

Syracuse, N.Y., Harbor Brook at-------------------

Harbor Brook at Hiawatha Boulevard-------------

Meadow Brook at Hurlburt Road------------------

Onondaga Creek at 6pencer Street---------------

Onendaga Creek at Dorwin Avenue-------------------

280

,209

300

106

,291

339

,291

219

330

330

330

15U

116

.171

,136

.165

,170

,15U

.131

Ilk

,118

,132

.135

.119

,322

322

,333

,333

338

.189

.166

,101

,25U

181

351

352 355

350

351

T

Taberg, N.Y., East Branch Fish Creek at-----------

Tamaqua, Pa., Little Schuylkill River at----------

Taneytown, Md., Piney Creek tributary at----------

Tannery Creek near Lindley, N.Y-------------------

Tappahannock, Va., Hoskins Creek near-------------

Piscataway Creek near--------------------------

Tenmile Creek at Avoca, N.Y-----------------------

near Clarksville, Pa---------------------------

Tearcoat Creek tributary near Augusta, W.Va-------

Thomas Creek near Keene, Va------------------------

Thornton Gap, Va., Thornton River tributary near-Thornton River tributary near Thornton Gap, Va---

T. Howard Duckett Reservoir near Laurel, Md-------

Three Springs, Pa., Aughwick Creek near-----------

Tinker Creek near Daleville, Va-------------------

Tioga, Pa., Crooked Creek at----------------------

Tioga River at---------------------------------

Tionesta Creek at Lynch, Pa-----------------------

at Tionesta Dam, Pa----------------------------

Tionesta Dam, Pa., Tionesta Lake at---------------

Tionesta Lake at Tionesta Dam, Pa-----------------

Tionesta Dam, Pa., Tionesta Creek at--------------

Tioughnioga River at Cortland, N.Y----------------

at Itaska, N.Y---------------------------------

Tioga River at Lindley, N.Y-----------------------

at Mansfield, Pa-------------------------------

at Tioga, Pa-----------------------------------

near Erwins, N.Y-------------------------------

Tipton, Pa., Little Juniata River at--------------

Toby Creek at Luzerne, Pa-------------------------

Toliver Run tributary near Hoyes Run, Md----------

Toms Run at Cooksburg, Pa-------------------------

Tonoloway Creek near Needmore, Pa-----------------

Totopotomoy Creek near Atlee, Va------------------

Towanda Creek near Monroeton, Pa------------------

Towanda, Pa., Susquehanna River at----------------

Town Creek near Old Town, Md----------------------

Transit Bridge, N.Y., Angelica Creek at-----------

Trapping Brook near Wellsville, N.Y---------------

35U

93

213

123

238

239

127

315

198

252

23b

23U

18U

159

266

121

120

287

288 288 288 288 117

119 122 121

120 127 156 13U 318 293 198 2U2 130 131 196 338 337

Trevilians, Va., Harris Creek near---------------------------2U1

Trexler Run near Ringtown, Pa--------------------------------137

Triadelphia Lake near Brighton, Md---------------------------183

Troups Creek near Troupsburg, N.Y-------------------------------

Troupsburg, N.Y., Troups Creek near-----------------------------

Trout Run, Pa., Lycoming Creek near-----------------------------

Truemans, Pa., Minister Creek near----------------------------288

Tunkhannock Creek near Tunkhannock, Pa--------------------------

Tulpehocken Creek at Blue March damsite, near Reading, pa— 9U

near Reading, Pa------------------------------------------ 95

Tunkhannock, Ra., Tunkhannock Creek near------------------------

Tunnelton, Pa., Conemaugh River at---------------------------30 3

Turbeville, Pa., Lawsons Creek near---------------------------277

Tuscarora Creek above Martinsburg, W.Va-----------------------702

near mouth below Martinsburg, W.Va------------------------203

near Silvara, Pa------------------------------------------132

near South Addison, N.Y-----------------------------------127

Tuscarora Creek tributary near Woodhull, N.Y-----------------126

Two Lick Creek at Grace ton, Pa------------------------------302

Tye River near Lovingston, Va---------------------------------250

Tye River, Va., Buffalo River near----------------*----------250

Tygart Lake near Grafton, W.Va--------------------------------309

Tygart Valley River at Belington, W.Va------------------------307

at Colfax, W.Va------------------------------------------308

near Dailey, W.Va-----------------------------------------306

at Elkins, W.Va-------------------------------------------306

at Riilippi, W.Va-----------------------------------------308

lyre, N.Y., Black Brook at------------------------------------3^9

Tyrone, Pa., Bald Eagle Creek at------------------------------157

Schell Run at-...................-.......................157

U

Unadilla River at Rockdale, N.Y-----------------------------H5

Unadilla, N.Y., Susquehanna River at------------------------H**

Unicorn Branch near Millington, Md--------------------------110

Union Center, N.Y., Naticoke Creek at-----------------------H®

Union City, Pa., French Creek near--------------------------2®9

Union City Reservoir near--------------------------------2®®

Union City Reservoir near Union City, Pa---------------------2”°

Unity, Md., Patuxent River near------------------------------183

Unnamed Run at Gilman, W. Va---------------------------------307

on North Fork Mountain near Franklin, W. Va.--------------*-93

Upper Darby, Pa., Cobbs Creek below Indian Creek near--------101

Ursina, Pa., Laurel Hill Creek at----------------------------320

U.S. Highway No. 1 near Riiladelphia, Pa., Cobbs Creek at—1°® Utica, Pa., French Creek at----------------------------------29°

V

Valley Lee, Md., Glebe Branch at-------------

Van Campen Creek at Friendship, N.Y----------

Vandergrift, Pa., Kiskiminetas River at------

Vandermark Creek near Scio, N.Y--------------

Verona, Va., Middle River near---------------

Vestal, N.Y., Susquehanna River at-----------

Victoria, Va., Falls Creek tributary near----

Vienna, Va., Difficult Run at Washington and

Old Dominion Railroad near-----------

Long Branch at Arlington Boulevard near---

Long Branch at---------------------------

Villa Nova, Md., Gwynns Falls at-------------

Virgil Creek at Dryden, N.Y------------------

.23b

.337

,30U

.337

,20U

.118

.260

.220

.229

.229

.181

,3U6

W

Waldy Run near Emporium, Pa---------------

Wales Hollow, N.Y., Buffalo Creek near—

Waltersburg, Pa., Redstone Creek at-------

Wapwallopen Creek near Wapwallopen, Pa---Wapwallopen, Pa., Wapwallopen Creek near-

War Branch near Hinton, Va----------------

Wardensville, W.Va., Cacapon River above-

Warren, Pa., Allegheny River at-----------

Warrensville, Pa., Mill Creek near--------

Warrenton, Va., Broad Run near------------

Cedar Run near------------------------

Rappahannock River near---------------

Warrior Ridge Dam, Pa., Juniata River at-

Warsaw, N.Y., Oatka Creek at--------------

Washington, D.C., Potomac River near------

—lUl —335

___317

—135

___135

___205

___198

___285

___151

___230

___228

---23l

---156

.—31*1 ___220﻿370

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Page

Page

Washington, D.C., Rock Creek at Sherrill Drive-----------------223

Washington, Va ., Rush River at--------------------------------23 5

Washingtonville, Pa., East Branch Chillisquaque Creek near-----x5^

Waterboro, N.Y., Conewango Creek at----------------------------285

Waterlick, Va., North Fork Shenandoah River near---------------209

Waterloo Mills, near Devon, Pa., Darby Creek near-------------- 99

Waterville, Pa., Pine Creek below Little Pine Creek near-------xi*9

Watkins Glen, N.Y., Seneca Lake at-----------------------------3^3

Watts Branch at Rockville, Md----------------------------------220

Waverly, N.Y., Susquehanna River near--------------------------xx9

Waverly, W.Va ., Ohio River near-------------------------------325

Waynesboro, Pa., Antietam Creek near---------------------------2®2

Waynesboro, Va., South River near------------------------------2^5

Webster Springs, W.Va., Elk River below------------------------332

Wellsville, N.Y., Dyke Creek at--------------------------------336

Trapping Brook near------------------------------------------337

Wentworth, N.C., Dan River near---------------------------------27^

Jacobs Creek near--------------------------------------------27^

West Branch Brandywine Creek at Coatesville, Pa----------------10 5

near Honey Brook, Pa-----------------------------------------105

at Modena, Pa------------------------------------------------106

West Branch	Caldwell Creek near Grand	Valley,	Pa-------------2®9

West Branch	Cayuga Inlet at Newfield,	N.Y--------------------3^U

West Branch Clarion River at Wilcox, Pa------------------------293

West Branch	Herring Run at Idlewylde,	Md----------------------1^7

West Branch	Mamaroneck River at White	Plains,	N.Y------------ 91

West Branch Susquehanna River at Bower, Pa---------------------137

at Cherry Tree, Pa-------------------------------------------137

near Curwensville, Pa----------------------------------------138

at Karthaus, Pa---------------------------------------------1110

st Lewisburg, Fa---------------------------------------------153

at Renova, Pa------------------------------------------------1^5

at Williamsport, Pa------------------------------------------150

West Cameron, N.Y., Canisteo River at---------------------------x2®

West Conewago Creek near Manchester, Pa------------------------1^

West Creek near Emporium, Pa-----------------------------------x ^

West Davenport, N.Y., Charlotte Creek at-----------------------x^

Western Branch near Largo, Md-----------------------------------1°5

Western Run at Western Run, Md---------------------------------1^;?

Western Run, Md., Western Run at-------------------------------1^6

Western Run tributary at--------------------------------------1^

Western Run tributary at Western Run, Md-----------------------

West Fork River at Brownsville, W.Va----------------------------^°9

at Butcherville , W.Va---------------------------------------310

at Clarksburg, W.Va-..........-.............................3X0

at Enterprise, W.Va------------------------------------------3X1

West Greenwood, N.Y., Dyke Creek near---------------------------336

West Hickory, Pa., Allegheny River at--------------------------2Q6

Westminister, Md., Cranberry Branch near------------------------x7®

West Nottingham, Md., Basin Run at-----------------------------1?2

West Pittston, Pa., Susquehanna River at------------------------132

Westport, Pa., Kettle Creek near-------------------------------x^

Westport, Pa., Kettle Creek Lake near--------------------------ij1^

West River near Middlesex, N.Y----------------------------------3^6

West Wyoming, Fh., Abrahams Creek at----------------------------135

White Clay Creek above Newark, Del-----------------------------103

near Newark, Del---------------------------------------------10^

White Deer Creek above Sand Spring Run near White Deer, Pa-----153

near White Deer, Pa------------------------------------------153

White Deer Hole Creek near Elimsport, Pa-----------------------x 5 2

White Deer, Pa., Sand Spring Run near---------------------------153

White Deer Creek, above Sand Spring Run near----------------x 5 3

White Deer Creek near---------------------------------------x 5 2

Whiteford, Md., Broad Creek tributary at-----------------------x^x

Whitehall, Va., Doyles River near-------------------------------253

North Fork Moormans River near------------------------------2 5 3

White Marsh, Md., Whitemarsh Run at----------------------------176

Whitemarsh Run at White Marsh, Md------------------------------176

White Plains, N.Y., West Branch Mamaroneck River at------------ 91

White Run near Gettysburg, Pa-----------------------------------2X2

White Sulphur Springs, W.Va., Dry Fork at----------------------327

Whitethorn Creek tributary near Gretna, Va---------------------2?9

Whitney Point Lake at Whitney Point, N.Y-----------------------xx®

Whitney Point, N.Y., Whitney Point Lake at---------------------llQ

Wiconisco Creek at Iykens, Pa---------------------------------- 155

Wilcox, Pa., West Branch Clarion River at----------------------293

Wilkes-Barre, Pa., Solomon Creek at-----------------------------135

Susquehanna River at-----------------------------------------135

Williamsburg, Pa., Frankstown Branch Juniata River at----------156

Williamsburg River near Olney, Md-------------------------------221

Williams Hollow near Moorefield, W.Va---------------------------19^

Williamsport, Pa., West Branch Susquehanna River at---------

Williams River at Dyer, W.Va--------------.-----------------

Williamsville, Va., Bullpasture River at--------------------

Willis River at Flanagan Mills, Va--------------------------

Willow Run at Rockland, Del---------------------------------

Wills Creek near Cumberland, Md-----------------------------

below Hyndman, Pa----------------------------------------

Wilmington, Del., Brandywine Creek at-----------------------

Shellpot Creek at----------------------------------------

Wilson Run at Benfield, Pa----------------------------------

Winchester, Va., Cedar Creek near---------------------------

Winfield Avenue, Mamaroneck, N.Y., 2iamaroneck River at-----

Winters Run near Benson, Md---------------------------------

Winterstown, Pa., East Branch Codorus Creek tributary near

Wiscoy Creek at Bliss, N.Y----------------------------------

Wissahickon Creek at Fort Washington, Pa--------------------

at Livezey Lane, Philadelphia, Pa------------------------

at mouth, Philadelphia, Pa-------------------------------

Withey, N.Y., North Branch Phillips Creek at----------------

Phillip-- Creek at---------------------------------------

Wolf Den Branch near Cedarville, Md-------------------------

Wooddale, Del., Red Clay Creek at---------------------------

Woodhull, N.Y., Tuscarora Creek tributary near--------------

.150 -329 _2^ -255 -190 J-90 J-90 J-09 J-03 J-hl ^08 . 91 J.7U J.68 .338

-	98

-	99

-	99 .337 -337 _232 ^05 _L26

Y

Yanceyville, N.C., Moon Creek near--------------------

Yellow Breeches Creek near Camp Hill, Pa--------------

Yellow Creek near Homer City, Pa----------------------

Yellow Creek Lake at Yellow Creek State Park, Pa------

Yellow Creek State Park, Fa., Yellow Creek Lake at----

Yonkers, N.Y., Saw Mill River at---------■------------

Yorklyn, Del., Red Clay Creek tributary near----------

York, Pa., Codorus Creek near-------------------------

Indian Rock Reservoir near-------------------------

South Branch Codorus Creek near--------------------

Youghiogheny River.below Confluence, Pa---------------

at Connellsville, Pa-------------------------------

at Friendsville, Md--------------------------------

near Oakland, lid----------------------------------

at Sutersville, Pa---------------------------------

at Youghiogheny River Dam, Pa----------------------

Youghiogheny River Dam, Pa., Youghiogheny River at----

Youghiogheny River Lake at-------------------------

Youghiogheny River Lake at Youghiogheny River Dam, Pa1

Youngsville, F&», Brokenstraw Creek at----------------

Young Womans Creek near Renovo, Pa--------------------

Z

..276 367 ..301 .301 .301 .. 92

3-05

369

369

369

,320

322 .319 .317 322 .319 .319 319 319 .287 3 U U

Zacharias Creek near Skippaek, Pa Zuni, Va., Blackwater River at---

. 96

262﻿APPENDICES

APPENDIX A, TABLES A-l— A-8 APPENDIX B, DATA SOURCES﻿372

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE Al.—Summary of flood stages and discharges

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June-July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Streams tributary to Long Island Sound

1	01208900	Patterson Brook near Easton, Conn.———————	1.21
2	01208950	Sasco Brook near Southport, Conn. ———————	7.27
3	01208990	Saugatuck River near Redding, Conn.———————	20.8
4	01209600		3.53
5	01209700	Norwalk River at South Wilton, Conn.——————	30.0
6	01209770	Fivemile River near Norwalk, Conn.—				8.96
7	01211700	East Branch Byram River at Round Hill, Conn.—		1.69
8	01212100	East Branch Byram River at Riversville, Conn.———	7.40
9	01299000	Blind Brook near Purchase, N.Y.------------------	1.79
10	01299100		1.04
11	01300000	Blind Brook at Rye, N.Y.			—							9.20
12	01300450	Beaver Swan?) Brook at Rye, N.Y.——————————	1.64
13	01300500	Beaver Swamp Brook at Hama rone ck, N.Y.----—------	4.71
14	01300700	West Branch Mamaroneck River at White Plains, N.Y.-	1.09
15	01300800	Mamaroneck River at Winfield Avenue, Mamaroneck, RY.	14.5
16	01300900	Sheldrake River at Mamaroneck, N.Y.————————	5.55
17	01301000	Mamaroneck River at Mamaroneck, N.Y.--------------	23.4
18	01301500	Hutchinson River at Pelham, N.Y. ————————	5.76
19	01302000	Bronx River at Bronxville, N.Y.——————————	26.5

1960-72	1962	5.37	90	June	19	5.1	80	(i)
1960-72	1968	4.15	340	June	19	7.00	1,640	(i)
1962-72	1969	5.88	2,160	June	19	4.33	851	a)
1960-72	1971	3.91	250	June	19	3.13	130	w
1963-72	1971	4.37	1,700	June	19	4.79	2,220	(i)
1956	1955	13.5	a)					
1962-72	1962	5.10	1,070	June	19	6.09	1,600	(i)
1960-72	1968	3.50	184	June	19	4.19	245	a)
1963-72	1968	6.77	1,040	June	19	7.62	1,700	a)
		—	...	...	June	19	...	1,140	a)
		...	—.	...	June	19	...	119	a)
1944-72	1955	9.62	1,360	June	19	12.44	2,320	>100
		...	...	...	June	19	...	135	a)
1944-72	1962	3.09	167	June	19	3.06	197	>100
		...	...	...	June	19	...	253	(1)
...	...	...	...	June	19	...	2,590	>100
		...	...	...	June	19	...	372	(1)
1944-53,	1971	6.68	2,260	June	19	9.71	4,740	>100
1955-72  1938	1944  1938		Td					
1944-72	1971	5.18	526	June	19	4.53	257	3
1944-72	1969	7.31	1,580	June	19	9.63	2,500	>100

Hudson River basin

01376430  01376500		.93  25.6					June 19 June 20		331
	Saw Mill River at Yonkers, N.Y.——————————		1945-72	1955	5.34	890		5.55	636

Delaware River basin

22	01469500	Little Schuylkill River at Tama qua, Pa.——————	42.9	1920-72	1955	11.10	7,790	June 22	7.64	3,800	12
23	01470500	Schuylkill River at Berne, Pa.——————————	355	1948-72	1955	15.73	29,400	June 22	19.0	42,800	>100
24	01470720	Maiden Creek tributary at Lenhartsville, Pa.———	7.46	1962-72	1965  1971	3/6.7  5.09	800	June 22	6.44	1,530	TO
25	01470960	Tulpehocken Creek at Blue Marsh damsite, near Reading, Pa.	175	1966-72	1971	11.68	9,400	June 22	18.7	16,100	50
26	01471000	Tulpehocken Creek near Reading, Pa*————————	211	1951-72	1971	a)	10,000	June 23	15.65	17,000	
27	01471800	Pine Creek near Manatawny, Pa.————————	15.6	1961-72	1969	9.2	809	June 22	9.25	812	
28	01472000	Schuylkill River at Pottstown, Pa. ———————	1,147	1902-72	1902	21.0	53,900	June 23	29.97	95,900	
29	01472157	French Creek near Phoenixville, Pa.———————	59.1	1969-72	1971	9.66	3,330	June 22	13.66	11,200	35
30	01472174	Pickering Creek near Chester Springs, Pa.----------	5.98	1967-72	1971	4.99	1,640	June 22	5.21	2,410	90
31	01472200	Green Lane Reservoir at Green Lane, Pa.---—-------	70.9	1956-72	1961	4/288.25	3/15,430	June 23	4/290.08	5/17,030	—
32	01473000	Perkiomen Creek at Graterford, Pa.----------------	279	1915-72	1935	18.26	39,900	June 22	17.08	35,800	60
33	01473100	Zacharias Creek near Skippack, Pa.					7.27	1960-72	1971	10.8	10,000	June 22	9.76	5,860	>100
34	01473120	Skippeck Creek near Collegeville, Pa.———————	53.7	1966-72	1971	22.5	40,400	June 22	10.48	5,240	4
35	01473880	Pine Run tributary at Fort Washington, Pa.————	2.01	1962-72	1967	7.34	300	June 22	6.40	128	>2
36	01473900	Wissahickon Creek at Fort Washington, Pa.-————	40.8	1961-72	1971	13.32	4,250	June 22	10.50	2,670	>2
37	01473980	Wlssahlckon Creek at Livezey Lane, Philadelphia, Pa.	59.2	1965-72	1971	6.27	5,390	June 22	4.39	2,390	>2
38	01474000	Wissahickon Creek at mouth, Philadelphia, Pa.———	64.0	1965-72	1967	6.45	4,310	June 22 June 23	6/6.02	2,380	>2
39	01474500	Schuylkill River at Philadelphia, Pa.———————	1,853	1869-1972	1869	17.0	135,000	June 23	14.65	103,000	30
40	01475300	Darby Creek near Waterloo Mills near Devon, Pa.——	5.15	...	...	...	...	June 22	5.49	985	
41	01475510	Darby Creek near Darby, Pa.———————————	37.4	1964-72	1968	9.12	4,610	June 22	7.04	2,690	>2
42	01475530	Cobbs Creek at U.S. Highway No. 1 near Philadelphia, Pa.	4.78	1965-72	1971	6.97	1,040	June 22	5.12	306	>2
43	01475540	Cobbs Creek below Indian Creek near Upper Darby, Pa.	9.65	1965-72	1971	11.12	2,920	June 22	8.18	1,300	4
44	01475550	Cobbs Creek at Darby, Pa.-		—---------		22.0	1964-72	1971	7.21	4,390	June 22	5.16	2,010	4
45	01475030	Little Crum Creek at Swathmore, Pa.—------------	1.15	1971-72	1971	9.77	605	June 22	4.34	105	
46	01477000	Chester Creek near Chester, Pa.				61.1	1932-72	1971	24.59	21,300	June 22	13.28	6,180	6
47	01477800	Shellpot Creek at Wilmington, Del.————— Christiana River at Goochs Bridge, ©el-				7.46	1940-72	1971	11.91	6,850	June 22	6.66	2,240	5
48	01478000		20.5	1944-72	1947	12.41	2,620	June 22	11.35	3,320	IT
49	01478200	Middle Branch White Clay Creek near Lasdenberg, Pa.	12.7	1960-72	1960	9.41	1,900	June 22	12.29	3,860	60
50	01478500	White Clay Creek above Newark, Del.———————	66.7	1953-59,  1963-72	1967	9.97	4,540	June 22	13.77	10,200	>100
51	01478950	Pike Creek near Newark, Del.—————————	6.04	1969-72	1969	9.15	2,550	June 22	6.78	942	11
52	01479000	White Clay Creek near Newark, Del.———————	87.8	1932-36,  1944-57,  1960-72  1937	1967  1937	16.41  23	6,640  (1)	June 22	17.74	9,080	>100
53	014T9200	Mill Creek at Hockessin, Del.		It.19	1966-72	1969	11.29	2,100	June 22	7.98	687	(i)
54	01479950	Red Clay Creek tributary near Yorklyn, Del.——	.38	1966-72	1969	6.53	200	June 22	5.29	56	(i)
55	01480000	Red Clay Creek at Wooddale, Del.-----------------	47.0	1944-72	1960	9.93	4, 780	June 22	8.96	4,120	
56	01480100	Little Mill Creek at Elsmere, Del. ————————	6.70	1964-72	1967	8.58	3,960	June 22	5.85	1,130	(i)
57	01480300	West Branch Brandywine Creek near Honey Brook, Pa.	18.7	1961-72	1960	8.60	1,870	June 22	11.41	8,160	>100
58	01480500	West Branch Brandywine Creek at Coatesville, Pa.—-	45.8	1942-72	1942	1/12.3	8,600	June 22	9.92	7,770	>100
59	01480610	Sucker Run near Coatesville, Pa.—------	2.57	1964-72	1970	5.78	590	June 22	6.96	926	>100
60 See 1	01480617 ootnotes a	West Branch Brandywine Creek at Modena, Pa.———— t end of table.	55.0	1970-72	1971	8.17	2,530	June 22	11.48	7,950	>100﻿APPENDIX A

373

TABLE A1 .—Summary of flood stages and discharges--Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Delaware River basin—Continued

61	01480675	Marsh Creek near Glenmoore, Pa. ————————	8.57	1967-72	1971	3.73	884	June 22	4.68	946	9
62	01480680	Marsh Creek near Lyndell, Pa.—————————	17.8	1960-72	1960	6.32	1,150	June 22	7.80	(i)	
63	01480700	East Branch Brandywine Creek near Downingtown, Pa.	60.6	1966-72	1971	8.49	4,440	June 22	12.06	8,070	ao
64	01481000	Brandywine Creek at Chadds Ford, Pa.-—----------—	287	1912-72	1920	15.0	17,200	June 22	16.56	23,800	>100
65	01481200	Brandywine Creek tributary near Centerville, Del.—	.97	1966-72	1971	9.35	• 405	June 22	5.92	170	(i)
66	01481450	Willow Run at Rockland, Del.----—			.37	1966-72	1971	12.70	620	June 30	8.26	263	
67	01481500	Brandywine Creek at Wilmington, Del.———————	314	1947-72	1971	13.83	21,300	June 23	15.49	29,000	
68	01482310	Doll Run at Red Lion, Del.——			1.2	1966-72	1971	4.71	140	June 22	5.59	215	
69	01483200	Blackbird Creek at Blackbird, Del.—————-------	3.85	1952-72	1960	4.10	510	June 22	5.04	712	>100

Smyrna River basin

70  71	01483290  01483400	Paw Paw Branch tributary near Clayton, Del.——— Saw Mill Branch tributary near Blackbird, Del.——	1.3  .6	1966-72  1966-72	1969  1969	8.13  4.88	350  39	June 22 June 22	8.43  4.82	760  37	(1)  (1)
		Lei	)sic River	basin							
72	01483500	Leipsic River near Cheswold, Del.———————	9.35	1944-72	1960	6.45	1,340	June 22	5.53	785	13
St. Jones River basin											
73	01483700	St. Jones River at Dover, Del.—————————	31.9	1959-72	1960	9.45	1,900	June 23	7.52	996	6
Che			ster River	basin							
74  75  76	01493000  01493500  01494020	Unicom Branch near Millington, Md.—-------------  Morgan Creek near Kennedyville, Md.----------------  Browns Branch tributary near Church Hill, Md.——	22.3  10.5  1.7	1949-72  1952-72  1971-72	1960  1960  1971	7.17  8.88  12.3	1,060  1,530  890	June 22 June 22 June 22	7.03  13.07  10.95	1,020  7,500  450	40  >100  (1)
Elk River basin											
77	01495000	Big Elk Creek at Elk Mills, Md.—-----------------	52.6	1932-72  1884	1937  1884	14.5  19	10,600  (1)	June 22	13.46	8,720	30
			Northea	st River ba	sin						
78  79	01496000  01496080		24.3  1.7	1949-72  1967-72	1967  1970	7.74  5.08	4,060  380	June 22 June 22	8.41  6.4	4,800  615	60  (1)
		Northeast River tributary near Charlestown, Mdu——									
		Princ	ipio Creek	basin							
80	01496200	Principio Creek near Principio Furnace, Md.-———-	9.03	1968-72	1969	9.26	7,060	June 22	8.49	3,020	Cl)

Susquehanna River basin

81

82

83

01496370

01496450

01496500

Mink Creek at Richfield Springs, Conadarago Lake at Schuyler, N.Y. Oaks Creek at Index, N.Y.--------

N.Y

84

85

86 87

01497800

01498500

01499500

01500000

Schenevus Creek at Schenevus, N.Y.-------

Charlotte Creek at West Davenport, N.Y. East Sidney Lake at East Sidney, N.Y.— Ouleout Creek at East Sidney, N.Y.-----.

88

01500500

Susquehanna River at Unadllla, N.Y.

89	01502000

90	01502500

Butternut Creek at Morris, N.Y.* Unadllla River at Rockdale, N.Y.

91

92

93

01503000

01503980

01505000

Susquehanna River at Conklin, N.Y.

Chenango River at Eaton, N.Y.------

Chenango River at Sherburne, N.Y.—

10.4	1969-72	1970	4.13	380	June 22	
65.0	1969-72	1972	5.66			June 25	3.11
102	1930-32,  1938-72	1959	6.87	2,550	June 23	4.35
57.8	1963-72	1964	8.14	2,200	June 23	(1)
167	1938-72	1938	4/ 9.65	14,000	June 23	4/ 4.93 T,158.63
103	1953-72	1960	1,194.4	5/25,100	June 24	
103	L941-72  L935	1942  1935	7.62  (1)	7,250  16,700	June 30	3.72
982	L938-72	1942  1960	13.94  14.25	21,500	June 23	7.87
59.7	L938-72	1964	8.47	4,260	June 22	6.05
520	L930-33,  L938-72	1942	12.98	17,400	June 23	8.73
2,232	1913-72	1936  1948	20.14  20.83	61,600	June 23	12.89
24.3	1964-65,  1967-72	1964	8.12	2,570	June 22	7.92
263	1938-72  1936	1942  1964  1936	2/9.99  9.80  10.6	9,200  (1)	June 22	9.57

100	<2
608	<2
200	<2
1,820	<2
1/5,480	
1,170	<2
6,140	<2
1,480	<2
6,640	<2
26,500	<2
1,100	<2
7,500	17

See footnotes at end of table﻿374

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^JULY 1972

TABLE Al.—Summary of flood stages and discharges—Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfa)	Date	Gage  height  (ft)	Dis-  charge  (cfa)	Recur-  rence  interval  (years)

Susquehanna River basin—Continued

94	01505500	Canasawacta Creek near South Plymouth, N.Y.	—		57.9	1945-72
95	01507000	Chenango River at Greene, N.Y.—-——————	593	1937-72
96	01508500	Albright Creek at East Homer, N.Y.				6.81	1939-68,  1970-72
97	01509000	Tloughnioga River at Cortland, N.Y.———————	292	1939-72
98	01510000	Otselic River at Cincinnatus, N.Y.————	147	1938-72
99	01511000	Whitney Point Lake at Whitney Point, N.Y.			257	1943-72
100	01511500	Tioughnioga River at Itaska, N.Y.------------------	735	1930-67,  1969-72
101	01512500	Chenango River near Chenango Forks, N.Y.-----------	1,483	1913-72
102	01513500	Susquehanna River at Vestal, N.Y.—----------------	3,960	1936-72
103	01513790	Naticoke Creek at Union Center, N.Y.--------------	89.7	1956,  1963-64,  1966-68,  1970-72
104	01513840	Pumpe11y Creek at Owego, N.Y.----------------------	8.59	1967-68
105	01514000	Owego Creek near Owego, N.Y.---------------------	185	1930-72
106	01514100	Catatonk Creek at Spencer, N.Y.----—-------------	26.5	1955
107	01515000	Susquehanna River near Waverly, N.Y.-----—-------	4,773	1936-72
108	01516500	Corey Creek near Mainesburg, Pa.————————	12.2	1955-72
109		Corey Creek at Mansfield, Pa.——————————	22.1	—
110	—	Tioga River at Mansfield, Pa.———————————	156	—
111	01516800	Manns Creek near Mansfield, Pa.——————————	3.01	1960-72
112	01517000	Elk Run near Mainesburg, Pa.———————	10.2	1954-72
113	01518000	Tioga River at Tioga, Pa.-		282	1939-72  1889
114	01518500	Crooked Creek at Tioga, Pa.—————————	122	1954-72
115	01518970	Troups Creek near Troupsburg, N.Y.----------------	30.2	—
116	01520000	Cowanesque River near Lawrenceville, Pa.----------	298	1952-72
117	01520500	Tioga River at Lindley, N.Y.———————————	771	1930-72
118	01520507	Tannery Creek near Lindley, N.Y.-----------------	9.13	—
119	01520970	Canisteo River tributary near Almond, N.Y.—-———	.17	—
120	01520973	Canisteo River tributary No. 2 near Almond, N.Y.-—	.31	—
121	01520991	Canisteo River at Bishopville, N.Y.————————	22.4	—
122	01521000	Arkport Reservoir near Arkport, N.Y.———————	30.5	1952-72
123	01571500	Canisteo River at Arkport, N.Y.----		—	30.6	1937-72  1935
124	01521610	Big Creek near North Hornell, N.Y.———————	16.8	1935
125	01522075	Canacadea Creek near Alfred, N.Y.————————	1.28	—
126	01522076	Canacadea Creek tributary No. 2 at Alfred, N.Y.——	.52	—
127	01522078	Canacadea Creek tributary No. 1 at Alfred, N.Y.-—-	1.02	—
128	01522083-	East Branch Canacadea Creek at Alfred Station, N.Y.	6.54	—
129	01522085	Canacadea Creek at Alfred Station, N.Y.					14.8	—
130	01522430	McHenry Valley Creek tributary No. 2 near Alfred, N.Y.	1.73	—
131	01522435	McHenry Valley Creek tributary No. 1 near Alfred, N.Y.	.96	
132	01522500	Karr Valley Creek near Almond, N.Y.-———————	27.6	1937-68,  1971-72
133	01523000	Almond Lake near Almond, N.Y.—————————	55.8	1950-72
134	01523500	Canacadea Creek near Hornell, N.Y.—	————	57.9	1927-28,  1935,  1939-72
135	01524500	Canisteo River below Canacadea Creek at Hornell,N.Y.	158	1943-72
136	01524610	Bennetts Creek tributary at Greenwood, N.Y.-			3.14	—
137	01524990	Purdy Creek near Canisteo, N.Y.——————————	21.2	1935
138	01525000	Bennetts Crqek at Canisteo, N.Y.————————	95.3	1939-47
139	01525050	Colonel Bill's Creek at South Canisteo, N.Y.———	10.1	—
140	01525500	Canisteo River at West Cameron, N.Y.———	340	1931,  1935,  1937-72
141	01525750	Tuscarora Creek tributary near Woodhull, N.Y.——	9.43	1967-68
142	01526000	Tuscarora Creek near South Addison, N.Y.—————	114	1937-72
143	01526070	Canisteo River at Erwins, N.Y.——————————	551	—
144	01526495	Mu 1 ho 11 and Creek near Erwins, N.Y.————————	5.06	1967-68
145	01526500	Tioga River near Erwins, N.Y.—————————	1,377	1919-72
146	01526976	Kirkwood Creek near Kirkwood, N.Y.	———————	3.70	—
147	01527000	Cohocton River at Cohocton, N.Y.————————	52.2	1951-72
148	01527428	Neils Creek near Bloomerville, N.Y.———————	18.0	1935
149	01527485	Tenmile Creek at Avoca, N.Y.———————————	17.9	—
150	01527500	Cohocton River at Avoca, N.Y.—————————	157	1939-45
151	01527580		4.86	—
152	01527620	Goff Creek near Avoca, N.Y.——————————	23.8	—
153	01528000	Fivemile Creek near Kanona, N.Y.—————————	66.8	1937-72
154	01528210	Campbell Creek near Kanona, N.Y.————————	32.7	1935
155	01528375	Stocking Creek tributary at North Cameron, N.Y.——	2.64	—-
156	01528950	Mud Creek tributary near Bradford, N.Y.———	2.34	—
157	01529000		76.6	1919,  L937-72

1961	5.94	6,980	June	22	5.40	5,000	7
1942	18.33	18,900	June	23	14.50	12,000	5
1947	3.71	787	June	23	4.40	1,200	>100
1964	12.49	13,000	June	23	10.47	7,730	4
1942	10.67	8,390	June	23	9.39	5,530	4
1950  1948	4/ 10.68 t, 005.0	7,830  71,440	June	25	^/996.52	^51,720	...
1935	16.61	61,100	June	23	8.38	11,400	2
1935	20.3	96,000	June	23	11.19	26,200	3
1936	30.5	107,000	June	23	22.35	58,000	2
1955	—	9,900	June	23	15.33	13,500	>100
1967	5.15	1,100	June	23	7.17	1,660	>100
1935	11.50	23,500	June	23	10.15	10,600	9
1955			1,680	June	23				1,500	4
1936	21.4	128,000	June	23	21.24	121,000	40
1955	7.88	2,120	June	23	10.44	5,580	>100
						June	22			10,600	>100
	...				June	22	...	24,200	80
1965	5.79	566	June	22	7.00	714	16
1955	V 6.77	1,240	June	22	6.00	3,940	>100
1946	15.47	39,000	June	22	19.70	59,000	>100
1889	17.4	ci)					
1955	12.73	10,900	June	23	18.29	21,000	>100
					June	23			4,500	(D
1964	11.89	25,400	June	23	17.26	40,500	>100
1946	22.87	75,000	June	23	26.27	128,000	>100
	...	...	June	23		2,730	100
		—	...	June	23	...	56	(1)
...			...	June	23				43	(1)
	A/ —  [7268.4			June	23	kj —	3,400	30
1956		1/2,730	June	23	1,304.04	5/7,940	—
1938			2,000	June	23	3.60	1,080	19
1939	5.63	—					
1935				4,820					
1935			11,900	June	23	...	6,680	>100
	...	—	June	23				656	(i)
					June	23			358	a)
				June	21			570	(i)
				June	23			2,660	>100
				June	21			6,080	>100
—	—	—	June	21	—	1,100	(1)
—	—	—	June	21	—	450	(1)
1967	9.11	6,250	June	23	12.2	10,900	>100
1956	£286.0	5/8,700	June	23	t[298.58	5/14,100		
1935	16.61	21,000	June	23	6.14	5,880	(1)
1943	13.30	9,340	June	23	13.45	9,560	>100
			...	June	21			680	(1)
1935	y —	8,990	June	22	1,160.12	6,940	>100
1946	1,130.50	10,000	June	22	4/1,134*41	19,500	>100
...				—	June	22	—	2,820	>100
1935	20.8	35,000	June	23	23.48	43,000	>100
1968	4.67	2,360	June	23	6.53	1,440	(X)
1951	8.79	14,000	June	22	10.4	18,700	>100
			—	June	23	967.4	65,000	>100
1966	3.20	96	June	23				590	(1)
1946	23.54	94,000	June	23	26.74	190,000	>100
			...	June	23	—	810	>100
1960	6.23	883	June	23	9.82	2,260	>100
1935			5,040	June	23	—	3,750	>100
		4/		—	June	23	...	2,240	>100
1942	1,188.22	3,880	June	23	...	13,300	>100
				—	June	21	—	660	100
...			...	June	22	...	3,550	>100
1940	1/6.10	—	June	23	5.95	5,110	>100
1956	4.59	2,680					
1935			14,000	June	23	...	7,340	>100
			...	June	23	...	452	(1)
...			—	June	23	...	757	(1)
1956	6.89	1,860	June	23	8.66	6,100	>100

See footnotes at end of table﻿APPENDIX A

375

TABLE Al.—Summary of flood stages and discharges--Continued

	Perma-  nent  station  No.			Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Susquehanna River basin—Continued

158	01529500	Cohocton River near Campbell, N.Y.----------------	470	1919-72	1935	11.6	41,100	June 23	11.16	32,000	>100
159	01529530  01530200  01530285	South Branch Michigan Creek near Risingville, N.Y.	.96  31.6  14.7	1953	1953	---	819	June 22	...	168  3.000  3.000	(1)  >100  >100
161		Sing Sing Creek near Big Flats, N.Y.----—--------		...							June 22	...		
162	01530303	Chemung River near Big Flats, N.Y.————————	2,150	1936	1936	—	87jr200	June 23	It/ 898.7	235,000	>100
163	01530440	Newtown Creek at Horseheads, N.Y.————————	56.4	—	...	...	—	June 22	...	5,200	>100
164	01530500	Newtown Creek at Elmira, N.Y.——————————	77.5	1938-72	1942	15.23	3,460	June 23	—/l9.28	4,000	>100
					1955	17.06	u>		it/909.48		
165	01530770	Seeley Creek near Elmira, N.Y.-	———————	95.6	...	—.	—	...	June 23		18,900	>100
166	01530910	Rorick Hollow Creek near Breesport, N.Y.—————	1.65	...	—	—	...	June 23	—	333	(1)
167	01531000	Chemung River at Chemung, N.Y.--------------------	2,506	1904-72	1946	23.97	132,000	June 23	31.62	189,000	>100
168	01531250	North Branch Sugar Creek tributary near Columbia	8.83	1963-72	1967	5.14	1,150	June 22	6.24	2,410	70
		Cross Roads, Pa.									
169	01531500	Susquehanna River at Towanda, Pa.-----------------	7,797	1865-1972	1946	25.08	191,000	June 24	33.43	320,000	>100
170	01532000	Towanda Creek near Monroeton, Pa.---------------	215	1914-72	1946	12.53	31,300	June 22	15.30	47,000	>100
171  172	01532200  01532850	South Branch Towanda Creek at New Albany, Pa.—— Middle Branch Wyalusing Creek tributary near	13.3  5.67	1963-72  1960-72	1964  1967	7.4  6.20	1,530  640	June 22 June 22	9.86  6.85	2,850  1,120	35  16
		Birchardville, Pa.									
173	01533250	Tuscarora Creek near Silvara, Pa.————————	11.8	1963-72	1964	12.92	1,350	June 22	13.07	1,610	9
	01533800  01533950		7.38  12.6	1963-72  1961-72	1967  1970	17.2  5.73	2,460  1,440	June 22 June 22	7.8  5.43	870  1,160	
175		South Branch Tunkhannock Creek near Montdale, Pa.-									3
176	01534000	Tunkhannock Creek near Tunkhannock, Pa.----------	383	1914-72	1964	14.26	33,600	June 23	11.26	15,100	3
177	—	Susquehanna River at West Pittston, Pa.-----------	9,533	...	...	4/ —		June 24	4/ —	339,000	>100
178	01534180	Stillwater Lake near Forest City, Pa.—————	37.1	1960-72	1960	1,603.2	A/5,860	June 23	1,602.00	5/5,460	—
179  180 181	01534300  01534500  01536000	Lackawanna River near Forest City, Pa.———— Lackawanna River at Old Forge, Pa.————————	38.8  108  332	1942-72  1940-72  1939-72	1942  1942  1955	10.58  20.05	2,530  9,510  31,000	June 26 June 22 June 23	4.84  6.09  8.78	1,010  3,000  9,340	CD  (i)  a)
182  183			10.5  9,960					June 22 June 24		1,040	9
	01536500	Susquehanna River at Wilkes-Barre, Pa.—————		1784-1972	1936	33.07	232,000		40.91	345,000	>100
					1865	33.1					
184	01537000	Toby Creek at Luzerne, Pa.-——————————	32.4	1942-72	1942	...	3,010	June 22	6.07	3,390	70
					1946	5.01	—				
185	01537500		15.7	1940-72	1955  1933	9.83  11.4	2,450  (1)	June 22	6.92	1,220	
											
186	01538000	Wapwallopen Creek near Wapwallopen, Pa.————	43.8	1920-72	1955	9.23	3,140	June 22	11.04	5,410	>100
187	01538800	Huntington Creek near Pikes Creek, Pa. — ————	4.94	1960-72	1969	8.87	740	June 22	9.34	948	60
188	01539000	Fishing Creek near Blooms burg, Pa.———————	274	1939-72	1940	12.08	18,100	June 22	15.18	30,900	>100
189	01540200	Trexler Run near Ringtown, Pa.—————————	1.77	1959-72	1961	3.11	178	June 22	5.15	487	60
190	01540500	Susquehanna River at Danville, Pa. ————————	11,220	1899-72	1904	3/30.7	...	June 24	1/32.32	—	
					1936	27.4	250,000	June 25	32.16	363,000	>100
				1865	1865	28	u)				
191  192  193  194  195  196  197  198  199  200 201 202	01540650  01541000  01541180  01541200  01541308  01541340  01541500  01542000	Schler Run at Danville, Pa.-----------------------  Blizzard Run at Danville, Pa.—————————  West Branch Susquehanna River at Cherry Tree, Pa.-West Branch Susquehanna River at Bower, Pa.———  Curwensvllle Lake near Curwensville, Pa.———	  West Branch Susquehanna River near Curwensville,Pa. Bradley Run near Ashvllle, Pa.——————————  Glendale Lake at Prince Gallitzin State Park near Flinton, Pa.  North Whitmer Run at Irvona, Pa.—————————  Clearfield Creek at Irvona, Pa.———————  Clearfield Creek at Dimeling, Pa. ————————	5.42  1.95  58.8 315 365 367  6.77  41.9  20.7 193 371  68.8	1899-1972  1966-72  1956-72  1968-72  1963-72  1914-72  1941-72  1936	1936  1968  1964  1971  1967  1936  1964  1936	4/ 19.74 1,197.06 14.19 4/ 2.68 1,429.40  *8.49  9.34  19.36	31,500  5/54,500  15,700  5/ 558 ^29,180	June 22 June 22 June 23 June 23 June 23 June 25 June 23 June 24  June 23 June 23 June 23 June 23	4/ 18.64 1,214.11 11.40 4/ 3.82 1,431.63  17.56  14.25	2,310 460 6,790 27,500 —/ 87,650 8,590 679 1/33,390	>100  50  50  >100  (I)  6  30  >100  (1)  >100
							30,600  2,930  (1)			2,650  24,800  22,400  5,120	
											
£03	—	Moshannon Creek at Phillipsburg, Pa#———————	81.1			...	—	—	June 23	—	6,070	100
204	01542500	West Branch Susquehanna River at Karthaus, Pa.—	1,462	1936-72	1936	24.5	135,000	June 23	18.57	84,300	(1)
205	01542720	Wilson Run at Penfieid, Pa.———————————	8.34	1962-72	1964	4.39	592	June 22	4.68	403	2
206	01542810	Waldy Run near Emporium, Pa.		————————	5.24	1963-72	1967	6.32	828	June 22	5.86	469	4
207	—	Driftwood Branch Sinnemahoning Creek at Emporium, Pa.  West Creek near Emporium, Pa.	86.2	—	—	...	—	June 22	—	6,180	9
208	01542860		59.1	...	...	...		June 22	—	7,510	30
209	01543000	Driftwood Branch Sinnemahoning Creek at Sterling	272	1914-72	1942	14.70	47,800	June 22	12.20	32,000	40
		Run, Pa.								60,800	40
210	01543500	Sinnemahoning Creek at Sinnemahoning, Pa.———	685	1936-72	1936	21.94	61,200	June 23	4/ 21.78		
211	01543900	First Fork Sinnemahoning Creek Reservoir near	243	1956-72	1964	it/ 994.50	5/39,250	June 26	r,015.87	£/62.030	—
		S innemahoning, Pa.								7,150	u)
212	01544000	First Fork Sinnemahoning Creek near Sinnemahoning, Pa.  Germania Branch at Germania, Pa.————————	245	1942-72	1942	—	80,000	June 28	4.75		
213	01544450		2.40	1964-72	1964	2.63	141	June 23	4.55	210	2
214	01544500	Kettle Creek at Cross Fork, Pa.--———————		136	1936,	1936	14.0	20,000	June 23	11.76	14,300	
215  216	01544800  01545000	Kettle Creek Lake near Westport, Pa.———————  Kettle Creek near Westport, Pa.—————————	226  233	1941-42  1962-72  1955-72	1970  1956	it/913.50	—/45,350 7,970	June 25 June 28	ft/ 919.13 8.69	5/51,700 5,750	(i)
					1959	1/13.31	—				>100
217	01545500	West Branch Susquehanna River at Renovo, Pa.———	2,975	1889-1972	1936	29.39	236,000	June 23	26.56	181,000	
218	01545600	Young Womans Creek near Renovo, Pa.———————	46.2	1965-72	1970	3.33	844	June 23	7.98	5,370	18
219	01546500	Spring Creek near Axemann, Pa.	87.2	1941-72	1950	5.44	1,670	June 23	8.75	5,410	>100
				1936	1936	8.6	u)				
220	01547100	Spring Creek at Milesburg, Pa	142	1967-72	1970	7.14	1,360	June 23	13.20	8,170	>100

See footnotes at end of table.﻿376

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE Al.—Summary of flood stages and discharges--Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Susquehanna River basin—Continued

221	01547200	Bald Eagle Creek below Spring Creek at Milesburg,Pa	265	1956-72	1964	/, 6*60 638.68	8,950	June 23	11.67	21,300	>100
222	01547480	Foster Joseph Sayers Lake near Blanchard, Pa.—	339	1971-72	1972		5/46,100	June 25	it/ 658.41	5/103,950		
223	01547500	Bald Eagle Creek at Blanchard, Pa.	______	339	1955-72	1964	11.59	10,100	June 28	9.37	4,890	a)
224	01547700	Marsh Creek at Blanchard, Pa.———————	44.1	1956-72	1961	6.63	3,300	June 23	7.96	4,870	80
225	01547800	South Fork Beech Creek near Snow Shoe, Pa.——	12.2	1959-72	1964	4.92	967	June 23	5.36	1,170	45
226	01547950	Beech Creek near Monument, Pa.——	—		——	152	1968-72	1970	10.24	3,070	June 23	15.22	9,740	13
227	01548000	Bald Eagle Creek at Beech Creek Station, Pa.———	559	1911-72	1936	14.42	25,600	June 23	12.29	19,400	a)
228	01548020		1.99	1963-72	1967	7.26	113	June 22	8.97	351	13
229	...	Fishing Creek at Mill Hall, Pa.	————	179	—	—	—	—	June 23	—	25,000	>100
230			Pine Creek at Galeton, Pa.—		—		—		167	...	...	...	...	June 22	...	15,900	30
231	01548500	Pine Creek at Cedar Run, Pa.	———			604	1919-72	1946	14.39	52,000	June 23	16.0	66,000	>100
232	01549500	Block House Creek near English Center, Pa.		——	37.7	1936,  1941-72	1936	9.0	5,780	June 23	9.34	6,260	60
233	01549700	Pine Creek below Little Pine Creek near Waterville, Pa.	944	1958-72	1959  1964	2/16.0  13.67	45,300	June 23	22.76	104,000	>100
234	01549780	Larrys Creek at Cogan House, Pa.———————	6.80	1960-72	1964	4.49	701	June 22	5.29	1,130	100
235	01550000	Lycoming Creek near Trout Run, Pa..—			173	1914-72	1946	19.37	21,800	June 22	20.19	25,900	>100
236	01551500	West Bench Susquehanna River at Williamsport, Pa.	5,682	1889-1972	1936	33.57	264,000	June 23	34.75	279,000	>100
237	01552000	Loyalsock Creek at Loyalsockville, Pa.——	—	443	1926-72	1926  1950	12.3  12.32	51.200  51.200	June 23	14.74	88,700	>100
238	01552100	Mill Creek near Warrensville, Pa.————————	11.9	1961-72	1964	4.73	962	June 22	6.14	2,230	23
239	01552500	Muncy Creek near S ones town, Pa. ---—-------------	23.8	1941-72	1952	8.61	7,310	June 22	8.94	8,260	>100
240	...	Glade Run at Muncy, Pa.——————————	6.62	—	—	—	.—	June 22	—	1,780	50
241	01553050	White Deer Hole Creek near Elimsport, Pa.————	18.2	1961-72	1964	9.05	1,480	June 22	11.83	4,200	>100
242	01553120	White Deer Creek above Sand Spring Run near White Deer, Pa.	17.8	1968-72	1970	5.30	302	June 22	9.47	2,330	30
243	01553130	Sand Spring Run near White Deer, Pa.--------------	4.93	1968-72	1971	5.38	180	June 22	5.68	1,000	50
244	01553140	White Deer Creek near White Deer, Pa.—————	40.0	1968-72	1970  1971	6.22  3/6.84	637	June 22	9.89	6,410	>100
245	01553500	West Branch Susquehanna River at Lewisburg, Pa.		6,847	1936-72	1936	32.1	287,000	June 24	34.23	300,000	>100
246	01553600	East Branch Chillisquaque Creek near Washington, Pa.	9.48	1961-72	1970	7.85	1,440	June 22	11.11	4,390	>100
247	01554000	Susquehanna River at Sunbury, Pa.————————-	18,300	1819-1972	1936	34.65	556,000	June 24	35.80	620,000	>100
248	01554500	Shamokin Creek near Shamokin, Pa.———————	54.2	1940-72	1962	5.00	3,120	June 22	8.72	4,070	>100
249	01555000	Penns Creek at Penns Creek, Pa.————————	301	1930-72	1934	13.00	14,900	June 23	14.85	34,600	>100
250	01555500	East Mahantango Creek near Dalmatia, Pa.--————	162	1930-72	1933	13.66	10,600	June 22	26.62	69,900	>100
251			Wiconisco Creek at Lykens, Pa.——————————	29.0	—	—	—	—	June 22	—	18,700	>100
252	...		18.9	—	—	—	—	June 22	—	13,500	>100
253	01555800	McDonald Run near East Freedom, Pa.—-------------	1.54	1959-72	1966	3.38	350	June 23	3.63	134	<2
254	01556000	Frankstown Branch Juniata River at Williamsburg, Pa.	291	1889-1972	1936  1889	18.58  19.1	47,600  35,500	June 23	18.39	16,400	15
255	01556400	Sandy Run near Be11wood, Pa.—				5.58	1962-72	1967	6.25	887	June 22	5.75	628	7
256	01556500	Little Juniata River at Tipton, Pa.	————-	93.7	1946-72	1950	9.06	5,700	June 23	9.24	6,140	16
257	01557100		1.68	1958-72	1969	3.00	225	June 22	2.68	220	5
258	01557500	Bald Eagle Creek at Tyrone, Pa.—————————	44.1	1945-72  1936	1950  1936	i/J-5	5,140  (1)	June 22	6.66	5,050	60
259	01558000	Little Juniata River at Spruce Creek, Pa.———	220	1936-72	1936	19.1	39,800	June 23	16.98	28,600	>100
260			Juniata River at Warrior Ridge Dam, Pa.——	805	—	—	—	—	June 23	—	53,700	90
261	01559000	Juniata River at Huntingdon, Pa.———————	816	1896-98,  1900-22,  1924-29,  1931-38,  1942-72	1936	21.87	81,000	June 23	20.02	57,000	90
262	—	Crooked Creek near Huntingdon, Pa.--------------	26.4	—	—	—	—	June 22	—	4,540	>100
263	01559700	Buffalo Run tributary near Manns Choice, Pa.——	5.28	1962-72	1967	4.26	1,010	June 22	3.33	528	5
264	01560000	Dunning Creek at Belden, Pa.————————	172	1936,  1940-72	1936	17.8	16,900	June 23	12.67	12,000	>100
265	01562000	Raystown Branch Juniata River at Saxton, Pa.——	756	1889-1972	1936	24.54	80,500	June 22	17.74	40,000	45
266	01563000	Raystown Branch Juniata River near Huntingdon, Pa.	957	1936-72	1936	31.0	87,000	June 23	y725.2	48,000	u>
267	01563200	Raystown Branch Juniata River below Raystown Dam near Huntingdon, Pa.	960	1970-72	1970	18.54	24,100	June 23	18.22	23,300	a)
268	01563500	Juniata River at Mapleton Depot, Pa.			2,030	1936-72	1936	38.2	145,000	June 23	33.07	125,000	>100
269	01563800	Elders Branch near Hus ton town, Pa	3.46	1960-72	1967	7.23	294	June 22	8.60	540	8
270	01564500	Aughwick Creek near Three Springs, Pa.————	205	1939-72  1889	1950  1889	18.04  19.3	20,600  (1)	June 22	19.20	23,700	80
271	01565000		164	1940-72	1950	13.12	9,830	June 23	16.17	16,400	>100
272	01565700	Little Lost Creek at Oakland Mills, Pa.———	6.52	1960-72	1970	7.33	288	June 22	8.41	468	(U
273	01565920	Lick Run near East Waterford, Pa.				8.38	1962-72	1966	9.33	340	July 16	9.85	1,870	
274	01567000	Juniata River at Newport, Pa.				—....	3,354	1889-1972	1889	35.9	209,000	June 23	33.97	187,000	>100
275	01567500	Bixler Run near Loysville, Pa.--—--------------	15.0	1954-72	1956	10.39	8,780	July 16	9.69	6,570	30
276	01568000	Sherman Creek at Shermans Dale, Pa.—————	200	1927-72	1927	20.34	44,000	June 23	18.09	27,500	60
277	01568500	Clark Creek near Carsonville, Pa.———————	22.5	1938-72	1937  1946	4.81	988	June 22	10.98	4,800	>100
278	01569000	Stony Creek near Dauphin, Pa.--------------------	35.0	1938-72	1943	7.97	2,360	June 22	14.44	9,990	>100
279	01569340	Newburg Run at Newburg, Pa.—————————	5.29	1964-71	1969	8.6	5,000	June 22	7.4	1,180	in
280	01570000	Conodoguinet Creek near Hogestown, Pa.	470	1912-19,  1930-58,  1968-72	1952	12.16	15,700	June 23	17.01	33,700	>100
281	01570100	Conodoguinet Creek tributary No. 1 near Enola, Pa.	.77	1969-72	1971	3.49	64	June 22	5.71	604	>100
282	01570300	Conodoguinet Creek tributary No. 3 at Enola, Pa.--	.38	1969-72	1970	5.04	77	June 22	7.73	263	>100
283	01570500	Susquehanna River at Harrisburg, Pa.——————	24,100	1786-1972	1936	29.23	740,000	June 24	32.57	1,020,000	>100
284	01571000	Paxton Creek near Penbrook, Pa.—————————	11.2	1940-50	1949	6.97	1,900	June 22	—	3,300	>100

See footnotes at end of table.﻿APPENDIX A

377

TABLE Al..—Summary of flood stages and discharges-Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Susquehanna River basin—Continued

285	01571020	Paxton Creek at Wildwood Lake at Harrisburg, Pa.—	19.0									June 22	...	2,290	Cl)
286	01571500	Yellow Breeches Creek near Camp Hill, Pa.———	216	1909-19,  1955-72	1915	8.61	5,550	June 22	18.33 14.74	15,900	>100
287	01572900	Reeds Creek near Ono, Pa.————————	8.63	1962-72	1966	7.55	1,700	—		(i)	—
288	01573000	Swatara Creek at Harper Tavern, Pa.————	337	1899-1972	1889	25.6	88,000	June 23	23.72	66,700	>100
289	01573086	Beck Creek near Cleona, Pa.------—---------------	7.87	1964-72	1970	6.25	640	June 22	11.53	5,150	>100
290	01574000	West Conewago Creek near Manchester, Pa.———	510	1929-72	1933	24.14	47,600	June 22	30.26	81,700	>100
291	01574500	Codorus Creek at Spring Grove, Pa.----------------	75.5	1930-64,  1966-72	1933	11.84	11,200	June 22	15.57	19,400	>100
292	01574700	Indian Rock Reservoir near York, Pa.————	93.7	1943-72	1952	4/402.80	5/3,360	June 23	it/ 436.44	-/30.220	...
293	01574800	East Branch Codorus Creek tributary near Winterstown, Pa.	5.17	1960-72	1969	7.02	351	June 22	10.44	2,190	>100
294	01575000	South Branch Codorus Creek near York, Pa.———	117	1928-72	1933	17.97	19,300	June 22	22.62	26,700	>100
295	01575500	Codorus Creek near York, Pa.———————	222	1933,  1940-72	1933	24.0	32,000	June 22	26.36	30,000	>100
296	01576000	Susquehanna River at Marietta, Pa.—	—				25,990	1889-1972	1936	60.73	787,000	June 23	64.54	1,080,000	>100
297	01576320	Stony Run at Reams town, Pa.——————— —	3.55	1964-72	1968	6.30	890	June 22	7.00	995	35
298	01576500	Conestoga Creek at Lancaster, Pa. ————————	324	1929-72	1933	17.52	22,800	June 23	27.80	88,300	>100
299	01577500	Muddy Creek at Castlefin, Pa.————————	133	1929-38,  1968-71	1933	21.11	16,600	June 22	20.25	18,000	70
300	01577940	Broad Creek tributary at Whiteford, Md.—————	.77	1971-72	1971	6.62	156	June 22	9.65	310	a)
301	01578200	Conowingo Creek near Buck, Pa.————————	8.71	1963-72	1970	6.94	693	June 22	7.76	1,270	11
302	01578310	Susquehanna River at Conowingo, Md.------—------	27,100	1968-72	1970	26.40	434,000	June 24	36.83	1,130,000	>100
303	01578400	Bowery Run near Quarryville, Pa.————————	5.98	1963-72	1964	7.7	2,220	June 22	6.55	1,050	14
304	01578500	Octoraro Creek near Rising Sun, Md.--	———-	193	1933-58,  1963-72  1884	1942  1884	17.57  24.3	35,000  (1)	June 22	18.92	29,000	(1)
305	01578800	Basin Run at West Nottingham, Md.	——-——-----	1.3	1967-^1	1967	13.60	825	June 22	11.80	640	a)
306	01579000	Basin Run at Liberty Grove, Md.-		———————	5.31	1949-58,  1965-72	1967	7.66	3,500	June 22	6.92	2,560	16
307	01580000	Deer Creek at Rocks, Md.	——————--—-——	94.4	1888-1972	1933	17.7	13,600	June 22	17.09	12,200	70
308	01580200	Deer Creek near Kalmia, Md.—		—————	125	1968-72	1967	10.45	6,130	June 22	16.08	16,800	80

Bush River basin

309	01581500	Bynum Run at Bel Air, Md.——————————	8.52	1945-50*  1956-72	1945	6.25	3,620	June 22	8.32	4,650	60
310	01581700	Winters Run near Benson, Md.————————	34.8	1968-72	1971	8.96	5,350	June 22	11.60	7,600	100

Gunpowder River basin

311	01581900	Prettyboy Reservoir near Hereford, Md.———		79.8	1933-72	1934	V  522.46	^21,110	June 22	i/  525.12	-122,480	
312	01582000	Little Falls at Blue Mount, Md.---——-------------	52.9	1945-72  1933	1950  1933	13.32  14	5,730  (1)	June 22	18.54	8,280	>100
313	01582510	Piney Creek near Hereford, Md.-------------—-----	1.5	1966-72	1971	13.27	790	June 22	19.4	1,370	a)
314	01583000	Slade Run near Glydon, Md.----------------------	2.09	1948-72	1956	4.68	485	June 22	4.80	515	60
315	01583495	Western Run tributary at Western Run, Md.-————	.26	1966-72	1967	8.11	236	June 22	—	515	CD
316	01583500	Western Run at Western Run, Md.———	————	59.8	1945-72	1956	10.84	5,590	June 22	26.0	38,000	>100
317	01583580	Baisman Run at Broodmoor, Md.——————————	1.47	1965-72	1968	^85	8/ 490 28,520	June 22	6.08 ^ 248.62	692	(1)
318	01583980	Loch Raven Reservoir near Carney, Md.-———	—	303	1914-72	1933			June 22		—'31,040		
319	01584500	Little Gunpowder Falls at Laurel Brook, Md.-—-----	36.1	1927-72	1933	10.3	9,200	June 22	10.18	9,030	60
320	01585100	Whitemarsh Run at White Marsh, Md.————————	7.61	1960-72	1971	14.05	8,000	June 22	10.04	2,170	a)

Back River basin

321	01585200	West Branch Herring Run at Idlewylde, Md.—————	2.13	1958-72	1971	6.80	1,740	June 29	6.50	1,560	12
322	01585300	Stemmers Run at Rossville, Md.—————————	4.94	1959-72	1971	11.34	5,950	June 22	7.55	1,530	4
323	01585400	Brien Run at Stemmers Run, Md.—————————	1.97	1959-72	1971	10.75	3,500	June 22	5.66	632	6

Patapsco River basin

324	01585500	Cranberry Branch near Westminster, Md.-------——--	3.29	1949-72	1970	5.54	1,070	June 22	5.85	1,510	80
325	01586000	North Branch Patapsco River at Cedarhurst, Md.——	56.6	1946-72	1955	4,10.38	8/M3°	June 22	4/ 20.75	27,800	>100
326	01586990	Liberty Reservoir near Marriottsville, Md.——	164	1953-72	1956	*421.60	“44,670	June 22	427.42	“'49,550	—
327	01587050	Hay Meadow Branch tributary at Poplar Springs, Md.	.54	1966-72	1971	10.55	630	June 21	8.48	420	CD
328	D1587500	South Branch Patapsco River at Henryton, Md.———	64.4	1949-72	1956	19.40	12,100	June 22	28.14	26,900	>100
329	D1588000	Piney Run near Sykesville, Md.———————	11.4	1932-72	1956	12.0	7,380	June 22	11.0	9,700	>100
330	01589000	Patapsco River at Hollofield, Md. ———————	285	1945-72	1956	15.88	19,000	June 22	31.3	80,600	>100
				1933	1933	19.5	Cl)				
331	01589100	East Branch Herbert Run at Arbutus, Md.—————	2.47	1956-72	1971	5.94	1,180	June 22	6.35	1,340	CD
332	01589200	Gwynns Falls near Owings Mills, Md.———————	4.90	1959-72	1971	5.13	1,360	June 22	5.70	5,500	>100
333	01589240	Gwynns Falls at McDonogh, Md.	19.3	1958-72	1967	8.81	1,650	June 22	18.8	14,700	>100
334	01589300	Gwynns Falls at Villa Nova, Md.-------------------	32.5	1956-72	1956	12.6	5,270	June 22	21.5	16,200	>100
335	01589330	Dead Run at Franklintown, Md.------------------	5.52	1960-72	1968	10.22	2,750	June 22	12.5	7,400	>100
336	01589440		25.2	1958-72	1968	11.30	2,160	June 22	18.11	iS,?O0	>100
		South River basin									
337	01590000	North River near Annapolis, Md.——————————	8.5	1933-72	1944	6.22	5,000	June 22	2.36	122	>2
338	01590500	Bacon Ridge Branch at Chesterfield, Md.—————	6.92	1944-52,	1944	5.49	2,100	June 22	3.68	215	>2
				1965-72							
See fc	otnotes at	end of table.									﻿378

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE Al.—Summary of flood stages and discharges -.Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Patuxent River basin

339	01591000	Patuxent River near Unity, Md.—	———————	34.8	1945-72	1971	18; 60	21,800	June 22	16.1	14,500	35
340	0159150Q	Cattail Creek at Roxbury Mills, Md.----------------	27.7	1945-56	1956	14.19	10,100	June 22	16.4	(i)		
341	01591600	Trladelphia Lake near Brighton, Md-------------	78.4	1942-72	1971	4/367.5	8/7,250	June 22	4/371.0	8/8,210	—
342	01592495	T. Howard Duckett Reservoir near Laurel, Md. —-----	132	1954-72	1971	4/289.1	8/7,130	June 22	4/289.65	8/7,290		
343	01592500	Patuxent River near Laurel, Md.				132	1945-72	1971	18.5	12,000	June 22	25	26,000	a)
344	01593350	Little Patuxent River tributary at Guilford Downs,Md	.95	1966-72	1968	8.53	a)	June 22	10.28	620	(i)
345	01593500	Little Patuxent River at Guilford, Md.				38.0	1933-72	1952	13.26	5,300	June 22	18.38	12,400	>100
346	01594000	Little Patuxent River at Savage, Md.---------------	98.4	1940-72  1933	1952  1933	13.15  17.5	6,280  (1)	June 22	25.4	35,400	>100
347	01594400	Dorsey Run near Jessup, Md.					11.6	1949-72	1955	12.77	1,400	June 22	14.0	1,700	60
348	01594440	Patuxent River at U.S. Highway 50 near Mltchellville, Md.	348	—	—	—	— -	June 22	—-	31,100	(i)
349	01594445	Mill Branch near Mltchellville, Md.-----------------	1.1	1966-72	1969	11.42	540	June 22	6.56	150	(1)
350	01594500	Western Branch near Largo, Md.---		—-------	30.2	1950-72	1971	8.87	1,760	June 22	8.54	1,540	12
351	01594600	Cocktown Creek near Huntingtown, Md.		3.86	1957-72	1960	7.96	1,120	June 22	5.63	165	<2

Potomac River basin

352	01595200	Stony River near Mt. Storm, W.Va.		48.8	1962-72	1963	3/8.41	3,120	June 23	5.10	750	(i)
353	01595300	Abram Creek at Oakmont, W.Va.					47.3	1955,  1957-72	1955	9.82	3,830	July 5	6.95	1,540	<2
354	01595500	North Branch Potomac River at Kltamiller, Md.-			225	1950-72	1954	13.73	33,400	June 23	7.07	4,680	<2
355	01595800	North Branch Potomac River at Bamum, W.Va.-				266	1967-72	1967	9.70	12,200	June 23	7.47	5,440	<2
356	01596005	Savage River near Frostburg, Md.									1.5	1971-72	1972	19.60	60	June 23	19.74	70	a)
357	01596500	Savage River near Barton, Md.------------—-----—-	49.1	1949-72	1954	8.45	7,510	June 23	3.39	854	<2
358	01597000	Crabtree Creek near Swanton, Md.-- — --------------	16.7	1949-72	1949	5.01	3,260	June 29	2.19	233	<2
359	01597490	Savage River Reservoir near Bloomington, Md.--------	105	1952-72	1954	4/1,471.78	5/21,200 “ 6,530	June 29	4/1,469.87	5/20,500		
360	01597500	Savage River below Savage River Dam, near Bloomington, Md.	106	1949-72	1954	7.70		June 29	4.57	1,660	<2
361	01598500	North Branch Potomac River at Luke, Md.—-----------	404	1900-06,  1950-72  1924	1954  1924	17.15	39,400  51,000	June 23	7.50	5,620	<2
362	01599000	Georges Creek at Franklin, Md.		—				72.4	1931-72  1924	1936  1924	9.6  10	8,500  (1)	June 29	6.44	1,250	<2
363	01600000	North Branch Potomac River at Pinto, Md.--—--—		596	1924,1936,  1939-72	1924	24	55,000	June 29	10.45	8,380	<2
364	01600700	Little Wills Creek at Byard, Pa.--		—				10.2	1961-72	1967	8.91	1,100	June 22	9.13	789	4
365	01601000	Wills Creek below Hyndman, Pa.-		—-—			—	146	1952-72	1954	11.02	11,600	June 23	8.91	7,560	6
366	01601500	Wills Creek near Cumberland, Md.-------------- — ---	247	1924,  1930-72	1936	20.2	38,100	June 23	10.06	11,300	8
367	01603000	North Branch Potomac River near Cumberland, Md.--- —	875	1889-1972	1889	29.2	89,000	June 23	14.55	17,400	<2
368	01603500	Evitts Creek near Centerville, Pa.-——————	30.2	1933-72	1936	7.13	5,240	June 22	5.06	2,750	17
369	01604500	Patterson Creek near Headsvllle, W.Va.———————	219	1939-72	1955	12.20	16,000	June 23	9.93	4,090	<2
370	01605500	South Branch Potomac River at Franklin, W.Va.-------	182	1941-69  1936	1949  1936	11.40  13	15,000  (1)	June 21	5.68	3,610	<2
371	01605600	Friends Run near Franklin, W.Va.		—-—			4.55	1970-72	1969	1.87	58	June 21	(1)	9/40	(1)
372	01605700	Unnamed Run on North Fork Mountain near Franklin, W.Va.	.45	1965-72	(i)	<4.47	(i)	June 22	3.40	17	(i)
373	01606000	North Fork South Branch Potomac River at Cabins, W.Va.	314	1936-72	1949	18.0	50,000	June 21	9.15	6,530	<2
374	01606500	South Branch Potomac River near Petersburg, W.Va.-—	642	1877,  1929-72	1949	22.83	62,000	June 21	9.25	10,600	<2
375	01606800	Brushy Run near Petersburg, W.Va.———————	1.43	1965-72	1971	4.62	57	June 22	4.30	46	a)
376	01607500	South Fork South Branch Potomac River at Brandywine, W.Va.	102	1944-72	1949	14.6	41,200	June 21	8.55	6,170	4
377	01608000	South Fork South Branch Potomac River near Moorefleld, W.Va.	283	1924,  1929-36,  1939-72	1949	16.1	39,000	June 22	7.28	5,740	2
378	01608050	Fort Run near Moorefleld, W.Va.--———————	4.92	1970-72	1972	3.18	137	June 23	8.49	888	(1)
379	01608100	Williams Hollow near Moorefleld, W.Va.--—--------	.24	1965-72	a)	<5.37	<D	June 22	5.70	75	(1)
380	01608400	Buffalo Creek near Romney, W.Va.—————————	4.37	1969-72	1969	8.00	550	June 22	7.15	438	(1)
381	01608500	South Branch Potomac River near Springfield, W.Va.—	1,471	1878,  1900-01,  1904-06,  1929-72	1936	34.2	143,000	June 23	17.87	31,500	4
382	01609000	Town Creek near Oldtown, Md.———			148	1928-36,  1968-72	1936	19.08	27,000	June 22	14.13	11,700	(i)
383	01609500	Sawpit Run near Oldtown, Md.---						5.08	1948-58,  1963-72	1954	4.72	770	June 22	4.33	600	20
384	01609800	Little Cacapon River near Levels, W.Va.-------			108	1967-72	1967	10.24	5,510	June 22	12.97	10,500	13
385	01610000	Potomac River at Paw Paw, W.Va.------———————	3,109	1936-72	1936	54.0	240,000	June 23	28.83	64,500	5
386	01610105	Pratt Hollow tributary at Pratt, Md.		——			.70	1971-72	1971	11.40	40	June 22	12.84	110	(i)
387	01610155	Sideling Hill Creek near Bellegrove, Md.——		102	1968-72	1970	8.18	5,750	June 22	12.44	14,200	a)
388	01610200	Lost River at McCauley, near Baker, W.Va.		155	1972	1972	7.04	4,070	June 23	11.58	14,600	16
389	01610300	Cacapon River above Wardensvll^, W.Va.-----------	181	1972	1972	7.76	5,270	June 23	11.15	16,200	15
390	01611150	Tearcoat Creek tributary ne« Augusta, W.Va.-——	2.65	1965-72	(i)	<3.96	(i)	June 22	4.50	160	a)
391	01611500	Cacapon River near Great Cacapon, W.Va.-					677	1889,  1923-72	1936	30.1	87,600	June 22	22.17	45,500	17
392	01613000	Potomac River at Hancock, Md.-----								4,073	1889-1972	1936	47.6	340,000	June 2j	30.79	112,000	7
393 See f	01613050 ootnotes a	end of table.	10.7	1963-72	1970  1971	6.81 3/7.3^	685	June 22	9.17	1,300	9﻿APPENDIX A

379

TABLE Al.—Summary of flood stages and discharges—Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Potomac River basin—Continued

394	01613150	Ditch Run near Hancock, Md.	4.8	1965-72	1970	7.69	400	June 22	9.07	555	(i)
395	01613160	Potomac River tributary near Hancock, Md.	1.2	1965-72	1965	4.75	140	June 22	5.10	174	to
396	01613900	Hogue Creek near Hayfleld, Va. — -—————————	15.0	1961-72	1970	7.43	1,950	June 22	8.85	2,760	>100
397	01614000	Back Creek near Jones Springs, W.Va.					243	1929-31,  1936,  1937-1972	1942	25.17	22,400	June 22	23.15	18,700	>100
398	01614090	Conococheague Creek near Fayetteville, Pa	5.05	1961-72	1961	2.80	114	June 22	3.45	392	50
399	01614500	Conococheague Creek at Fairvlew, Md.----------------	494	1889,  1928-72	1889	16.5	22,000	June 23	24.5	32,400	>100
400	01614700	Conococheague Creek tributary at Kemps, Md.———	1.1	1968-72	1970	3.81	100	June 22	3.55	43	a)
401	01615000	Opequon Creek near Berryvllle, Va.----------—--—--	57.4	1944-72  1942	1970  1942	12.82  18.4	10,600  (1)	June 22	12.59	9,870	>100
402	01616500	Opequon Creek near Martinsburg, W.Va.---------------	272	1906,  1948-72  1936	1970  1936	15.81  17.5	14,000  (1)	June 22	17.45	19,000	>100
403	01617000	Tuscarora Creek above Martinsburg, W.Va.---	———	11.3	1949-63,  1968-72	1971	10.52	308	June 2j	11.20	450	>100
404			Tuscarora Creek near mouth below Martinsburg, W.Va.-	25.0	—	—	—	—	June 23	—	900	>100
405	01617800	March Run at Grimes, Md.-----—		———------	18.9	1964-72	1971	2.74	146	June 22	3.44	268	(l)
406	01618000	Potomac River at Shepherdstown, W.Va.------—				5,936	1889-1972	1936	42.1	335,000	June 23	31.58	187,000	18
407	01619000	Antietam Creek near Waynesboro, Pa.——				93.5	1949-51,  1966-72	1970	7.87	2,040	June 22	12.53	5,430	(i)
408	01619475	Dog Creek tributary near Locust Grove, Md.-—--—		.13	1966-72	1967	8.10	111	June 22	5.36	30	(i)
409	01619500	Antietam Creek near Sharpsburg, Md.			281	1929-72	1956	16.73	12,600	June 23	14.30	9,880	50
410	01620500	North River near Stokesville, Va.-		—				17.2	1942,  1947-72	1949	10.9	11,100	June 21	5.25	1,650	7
411	01621200	War Branch near Hinton, Va.			—				9.45	1949-72	1949	6.70	2,500	June 21	3.70	700	4
412	01622000	North River near Burketown, Va.--—				379	1852-1972	1949	36.3	62,600	June 22	16.58	12,900	4
413	01624300	Middle River near Verona, Va.									178	1968-72	1971	13.79	7,220	June 21	13.10	6,590	7
414	01624800	Christians Creek near Fishersville, Va.			70.1	1968-72	1969	12.78	3,800	June 21	12.50	3,630	7
415	01625000	Middle River near Grottoes, Va.----—------- — -----	375	1877-1972	1936	28.57	24,500	June 22	21.51	16,300	15
416	01626000	South River near Waynesboro, Va.----————————	127	1928-72	1969	15.27	17,400	June 21	14.25	14,000	20
417	01627500	South River at Harriston, Va.--—---—----—--------	222	1924-51,  1969-72  1870	1942  1870	17.2  18.8	23,100  (1)	June 21	15.25	21,300	20
418	01628500	South Fork Shenandoah River near Lynnwood, Va.---—-	1,084	1870-1972	1942	27.2	80,000	June 22	23.45	50,700	15
419	01628600	Cub Run tributary near Montevideo, Va.--------------	.42	1966-72	1969	5.15	92	June 21	5.12	91	4
420	01629100	South Fork Shenandoah River tributary near Luray, Va.	.54|	1966-72	1967	6.60	102	June 22	6.48	99	4
421	01631000	South Fork Shenandoah River at Front Royal, Va.--—-	1,642	1870-1972	1942	34.8	130,000	June 22	23.98	75,100	20
422	01632000	North Fork Shenandoah River at Cootes Store, Va.----	210	1836-1972	1942	25.3	50,000	June 22	14.98	13,900	4
423	01632900	Smith Creek near New Market, Va.------—				93.2	1961-72	1971	9.96	2,860	June 22	13.22	6,280	>100
424	01632950	Crooked Run tributary near Conicville, Va.-—-—			.31	1966-72	1967	4.32	26	June 22	4.72	34	<2
425	01633000	North Fork Shenandoah River at Mount Jackson, Va.-—	506	1942-72	1942	20.2	80,000	June 22	16.08	21,200	6
426	01633500	Stony Creek at Columbia Furnace, Va.	79.4	1947-72  1942	1959  1942	9.20  11.5	6,900  (1)	June 22	9.19	6,850	40
427	01633700	Pugh Run tributary near Columbia Furnace, Va.-------	.56	1966-72	1971	4.54	84	June 22	4.96	98	3
428	01634000	North Fork Shenandoah River near Strasburg, Va.-----	768	1870-1972	1942	31.2	100,000	June 22	20.88	25,100	8
429	01634500	Cedar Creek near Winchester, Va.					103	1936-72	1942	27.0	22,000	June 22	23.19	20,300	90
430	01635200	North Fork Shenandoah River tributary near Waterlick, Va.	.48	1966-72	1971	3.89	29	June 21	4.86	63	3
431	01635500	Passage Creek near Buckton, Va.	t	—		87.8	1933-72	1942	15.5	21,000	June 22	13.56	13,100	20
432	01636210	Happy Creek at Front Royal, Va.---------------—		14.0	1949-72  1942	1948  1942	7/6.40  10714	2,490  (1)	June 22	6.13	1,600	9
433	01636500	Shenandoah River at Millville, W.Va.	——		3,040	1870,  1896-98,  1900-01,  1903-18,  1924,  1929-1972	1942	32.4	230,000	June 23	21.89	103,000	18
434	01637000	Little Catoctin Creek at Harmony, Md.---—----------	8.83	1948-72	1952	8.49	5,400	June 21	5.64	1,960	9
435	01637500	Catoctin Creek near Middletown, Md			66.9	1948-72	1949	11.18	7,760	June 22	12.28	11,200	>100
436	01637600	Hollow Road Creek near Middletown, Md.				2.3	1965-72	1971	6.28	440	June 21	9.4	815	a)
437	01638500		9,651	1889-1972	1936	41.03	480,000	June 23	37.43	347,000	40
438	01638900	White Run near Gettysburg, Pa.--				12.4	1961-72	1961	11.9	2,760	June 22	13.55	4,360	>100
439	01639000	Monocacy River at Bridgeport, Md	173	1943-72  1933	1943  1933	20.53  25	15,000  (1)	June 22	24.05	21,300	>100
440	01639095	Piney Creek tributary at Taneytown, Md.—-------—--	.62	1967-72	1969	10.22	210	June 22	11.64	278	a)
441	01639500	Big Pipe Creek at Bruceville, Md.---—	102	1948-72	1949	11.92	9,500	June 22	17,86	22,800	>100
442	01640000	Little Pipe Creek at Avondale, Md.------------------	8.10	1948-56,  1959-64,  1967-72	1956	8.47	1,880	June 22	10.45	2,400	60
443	01640500	Owens Creek at Lantz, Md.-		—		5.93	1932-72	1934	8.4	3,270	June 22	5.14	940	6
444	01640700	Owens Creek tributary near Rocky Ridge, Md.-				1.2	1967-72	1970	13.40	383	June 22	12.29	363	(i)
445	01641000	Hunting Creek at Jimtown, Md.--			18.4	1950-72	1952	4.94	1,170	June 22	5.26	1,330	15
446	01641500	Fishing Creek near Lewis town, Md.---------- — -----	7.29	1948-72	1949	3.73	500	June 21	4.01	610	50
447	01642400	Dollyhyde Creek at Libertytown, Md.				2.7	1967-72	1969	8.88	760	June 21	13.20	1,620	(i)
448	01642500	Linganore Creek near Frederick, Md.-------------—-	82.3	1933-72	1955	11.39	4,130	June 22	19.46	20,100	>100
449	01643000	Monocacy River at Jug Bridge near Frederick, Md. ——	817	1930-72  1889	1933  1889	28.1  30	51.000  56.000	June 23	35.9	81,600	>100
450	01643500	Bennett Creek at Park Mills, Md.———----------	62.8	1949-72	1971	14.33	13,000	June 21	22.1	32,200	>100
451	01643700	Goose Creek near Middleburg, Va.----—-------------	123	1966-67,  1970-72	1967	14.44	6,920	June 22	27.46	19,200	>100
452 See fc	01644000 otnotes at	Goose Creek near Leesburg, Va.--—					  end of table.	332	1910-12,  1930-72  1889	1937  1942  1889	7/26.86  29	35.600  35.600 45,000	June 22	30.59	78,100	>100﻿380

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE Al.—Summary of flood stages and discharges—Continued

	Perma-  nent  station  No.		Drainage area (sq mi)	Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination		Period	Year	Gage  height  (ft)	Dis-  charge  (cfa)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Potomac River basin--Continued

	01644100 . 01644200 01644250 01644264  01644271  01644272 01644290 01644295 01644370 01644420 01645000 01645200 01645895  01645950			1966-72  1962-72  1966-72	1969	8.00	550		21	12.33	1,130	40
			1.09		1969  1967	4.34  10.80	(1)  1,070		21	8.46	(1)	(1)
								June	21	16.80	4,180	>100
456			1.50  7.20  1.43  .08  .32  13.4  .27  101  3.70  24.7  2.06  3.22  57.9  4.69						21	4/302.63  4/287.38  4/281.15  1.84	1,840	(1)
									21		8,250	(1)
458									21		1,330	(1)
				1969-72  1967-72  1960-72  1967-72  1931-72  1958-72	1971	1.61	' 55	June	21		87	(1)
					1971  1969	4.38  4.68	70	June	21	5.79	230	(1)
							(1)	June	21	8.69	8,800	(1)
					1969	11.60	153	June	21	13.75	396	(1)
					1971  1970	16.32  6.55	25,900	'June	22	16.4	26,100	>100
							1,220	June	21	7.22	2,900	>100
465		Difficult Run at Washington and Old Dominion Railroad, near Vienna, Va.						June  June	22  21	4/227.0  4/300.60  5.9	12,000  1,270	(1)  (1)
				1967-72  1935-72  1961-72	1968  1967		1,200	June	21		1,360	(1)
	01646000  01646200  01646500  01646550  01647685  01647720  01647725  01648000  01649100  01649500  01650050					13.18	6,610	June	22	21.40	32,200	>100
469					1966	23.30	3,560	June	21	25.0	2,800	(1)
			11,560	1931-72  1945-72  1967-72  1967-72  1967-72  1930-72  1933-72  1967-72  1967-72  1967-72  1963-72  1967-69,*  1971-72  1924-72	1936	7/28.1  6.82	484,000  2,680	June	24	22.03	359,000	30
					1966			June	21	6.62	2,540	25
			2.25  9.73  1.01  62.2  16.5  72.8  2.45  .35		1971		1,140	June	21	8.26	3,110	<i)
					1971  1971	5.86  4.67	1,030	June	22	14.1	10,100	a)
							'536	June	21	5.12	909	a)
475  476  477		Rock Creek at Sherrill Drive, Washington, D.C.---—-Paint Branch at Interstate Highway 495 near College Park, Md.  Northeast Branch Anacostia River at Riverdale, Md.—			1956  1933  1971	13.19  7/15.5  5.43  3.56  2.83	7,220  10,500  1,500	June  June  June  June	22  22  22  21	16.2  9.52  6.24	12,500  6,410  10,600  3,750	>100  (1)  >100  (1)
					1971		260	June	21	4.85	695	(1)
	01650190  01650450  01650470  01650500  01650990  01651000  01652400  01652430  01652470  01652500  01652610  01653000  01653500  01653600  01653950  01653960  01653987				1969		240	June	21	4.09	550	(1)
			1.69  .47  21.1  13  49.4  .94  .90  1.22  14.4  7.10  33.7  16.7  39.5 1.18 2.12  18.2  23.5 39.9  12.3  93.4  2.94  50.5 .79  343  25.8 7.13 1.67 5.92  39.6  7.10 148  57.7 7.64  34.9		1971  1967	8.49  7/4.60  10.99	1,030	June	21	10.47	1,930	(1)
							'570	June	21	5.92	571	(1)
483  484  485		Northwest Branch Anacostia River near Colesvllle, Md			1953		4,910	June  June	22  22	15.89	11,000  6,990	>100  (1)
		Northwest Branch Anacostia River nearfyattsville, Md		1933,  1939-72  1963-72  1966-72  1966-72  1951-72  1960-72  1953,  1955-72  1949-72  1966-72  1960-72  1947-72	1966  1969  1969  1969	13.50  26.9  8.6	7,000  1,280	June  June	22  21	14.47 24.6a	18,000  980	>100  (1)
^87							1*780	June	21	5.44	700	(1)
488  489							1^900	June	21	8.22	1,250	(1)
					1969  1967  1966  1971  1971  1969	11.6	14^600	June	21	12.4	10,000	(1)
							2^700	June	21	9.2	3,000	(1)
^91						14.14  7.63  7.19	9,300	June	22	18.14	19,900	(1)
492							3,440	June	22	6.89	2,450	9
							1,180	June	22	9,80	4,900	a)
							2,000	June	21	5.85	1,280	u)
495  496		Long Branch at Arlington Boulevard near Vienna, Va.-Accotlnk Creek at King Arthur Road, near Annandale, Va.			1969	11.85	7,870	June  June  June	21  22  22	4/290.73  4/255.24  15.96	1,800  11,500  12,000	a)  u)  (i)
498  499  500  501  502  503  504	01655112  01655500  01656000  01656200  01656500  01656600  01656700  01656725  01656800  01656850  01656910  01656940  01657000  01658000  01658500  01660400  01660900  01660930  01661000  01661050  01661430  01661500							June	22	68.8	19,000	(i)
				1951-72  1942  1951-72  1942  1950-	72  1951-	72 1966-72 1969-72 1967 1969-72 1963-72  1961-72  1951-	72 1950-72  1952-	72	1955	9.59  13  17.25  22  6.99  13.08  9.10  14.64  16  8.52 6.22  11.44  19.27  7.52 8.40	3,100	June	21	12.87	7,840	>100
					1942  1955 1942 1967  1956		(1)  7,300	June	22	27.66	38,600	>100
							(1')  200	June	21	7.86	276	3
							11,600	June	21	13.92	16,800	>100
					1968		310	June	21	16.20	575	>100
					1971		16,900	June	22	50.31	56,400	>100
					1967  1969  1967		(1)  2,940	June	22	18.92	39,400	>100
506  507  508							443	June	21	10.68	8,300	(1)
		Cain Branch near Chantilly, Va.  Flatlick Branch at Sully Road near Chantilly, Va.— -			1971		2,300	June  June  June	21  21  22	4/266.51  4/253.44  23.9	2,200  6,600  36,000	(1)  (1)  (1)
510		Big Rocky Run at Sulley Road, near Centrevllle, Va.-			1967		13,000	June  June	21  22	4/247.62  37.80	7,100  76,100	(1)  >100
					1955  1969		9,300	June	22	7.10	7,350	50
513  514		South Fork Quantlco Creek near Independent Hill, Va.					1,040	June  June	21  22	11.35  16.32	3,940  11,600	>100  >100
				1966-72  1966-72  1948-72  1969-72  1968-72  1947-72		5.42  7.00  8.56  5.55  8.66  13.34	140	June	22	6.59	255	(1)
516  517  518  519  520			10.4 10.7  18.5		1971  1950  1969  1969  1969		320	June	22	8.91	4,820	>100
							7,800	June	22	6.63	1,600	35
							1,500	June	22	6.55	4,350	>100
							100	June	22	4.56	29	a)
		St. Marys River at Great Mills, Md.-----------------	24.0				7,950	June	22	9.75	1,890	5
		Great	Wiocomico	River basir								
521	01661800		6.82	1964-72	1969	6.13	450	June	22	5.42	165	3
												

See footnotes at end of table.﻿APPENDIX A

381

TABLE A1.—Summary of flood stages and discharges--Continued

Re-  port  No.	Perma-  nent  station  No.				Maxi	mum pr<	•viously kn	own	Maximum June—July 1972			
		Stream and place of determination		age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Rappahannock River basin

522	01662000
523	01662300
524	01662500
525	01662800
526	01663500
527	01664000
526	01664800
529	01665000
530	01665200
531	01665300
532	01665400
533	01665500
534	01666500
535	01667500
53b	01667600
537	01668000
538	81668200
539	01668300
5to	01668500
54l	01668800
5te	01669000
	

Rappahannock River near Warrenton, Va.----------

Thornton River tributary near Thornton Gap, Va.

Rush River at Washington, Va.-------------------

Battle Run near Laurel Mills, Va.---------------

Hazel River at Rixeyville, Va.------------------

Rappahannock River at Remington, Va.'

Harpers Run near Marrisville, Va.----

Mountain Run near Culpeper, Va.------

Rock Run tributary near Gold vein, Va.-------

Rapidan River near Stajiardsvllle, Va.-------

Conway River near Stanardsville, Va.--------

Rapidan River near Ruckersville, Va.---------

Robinson River near Locust Dale, Va.---------

Rapidan River near Culpeper, Va.-------------

Cedar Run tributary near Culpeper, Va.------

Rappahannock River near Fredericksburg, Va.'

Gingoteague Run near Part Royal, Va.---------

Farmers Hall Creek near Champlain, Va.-------

Cat Point Creek near Montross, Va.----------•

Hoskins Creek near Tappahannock, Va.— Piscataway Creek near Tappahannock, Va.

195	I942-72	1942	23.5	32,000	June 22	20.87	
1.3f	1967-72	1971	8.34	54	June 22	9.90	140
14.7	1954-72	1955	8.14	2,500	June 22	6.44	1,460
27.6	1958-72	i960	11.37	1,120	June 21	11.53	
287	1937,  1942-72	1942	31.8	60,000	June 22	23.40	2)500
620	1828-1972	1942	30.0	90,000	June 22	24.82	
2.2f	1966-72	1969	5.65	460	June 21	12.53	1,900
15-9	1950-72	1950  1955	11.20	5,440	June 21	9.86	3,oto
1.00	1966-72	1967	4.70	200	June 21	7.37	
37.6	1967-72	1971	17.0	(D	June 21	18.28	(1)
25.8	1967-72	1971	17.33	W	June 21	20.43	(1)
n4	1942-72	1942	20.8	30,700	June 21	16.87	17,600  24,500
179	1942-72	1942	23.9	44,000	June 22	20.92	
472	1931-72	1942	30.3	58,100	June 22	29.53	55)600
.5*	1966-72	1966	6.43	U7	June 21	6.63	'125  107,000
1,596	1889-1972	1942	26.9	140,000	June 22	22.56	
2.82	1966-72	1969	8.4	130	June 22	9.94	*388
2.If:	1966-72	1969	19.20	510	June 22	15.72	U52
45.6	1935.  1944-72	1969	10.45	6,820	June 22	9.33	4,200
15.5	1965-72	1969	10.23	1,380	June 22	5-99	289  1,090
28.0	1952-72	1969	7.52	2,380	June 22	6.04	

Piankatank River basin

543

01669500

Dragon Swamp near Church Viev, Va.

84.9

I9I4.72

1935

1963

1935

10.00

17

June 24

Ware River basin

5^4 OI67OOOO Beaver dam Swamp near Ark, Va.

6.6311950-72	i960 |	5.88

570 June 22

7.81

1,610

3.39

York River basin

50

<2

h

50

20

35

>100

10

90

1

(1)

20

35

50

9

55

15

35

to

3

11

545	01670100	Mountain Run tributary near Gordonsville, Va.		.50	1966-72	1971	8.50	118		11.13	147  23,300	13  75  15  90
546	OI671OOO	North Anna River near Doswell, Va.	—	441	1927-72	1969	32.60	24,800	June 22	31.58		
547	01671100	Little River near Doswe11, Va.			107	1928  1962-72	1928  1969	33.7  11.09	12,000	June 22	9.88	8,300  2,580  2,310	
548	01671500	Bunch Creek near Boswells Tavern, Va.		4.31	1949-72	1969	10.64	2,750	June 21	10.44		
549	01671750	Harris Creek near Trevilians, Va.		3.31	1969-72	1969	16.7	3,300		14.54		
550	01672400	South Anna River tributary near Ashland, Va.			•3:	1966-72	1969	9.3	360				>100  30
551	01672500	South Anna River near Ashland, Va.		394	1928,  1931-72	1969	24.99	17,100	June 21	21.90	12,600	
552	01673000	Pamunkey River near Hanover, Va.			l,08l	1942-72  1928	1969  1928	31.12  32.6	40,300  (1)	June 23	29.22	29,900	50
553	01673500	Totopotanoy Creek near At lee, Va.	—	5.8S	1945^  1949-72	1955	8.62	748	June 22	6.88	308	11
554	01673800	Po River near Spotsylvania, Va.		77.4	1963-72	1969	14.00	4,48o	June 22	10.0^		>100  75
555	01674000	Mattaponi River near Bowling Green, Va.			257	1942-72  1928	1942  1928	17.45  19.5	10,1400  15,000	June 23	18.95	13,400	
556	01674500	Mattapani River near Beulahville, Va.		601	1928,  1942-72	1969	24.04	12,300	June 25	23.97	16,900	>100
557	01674700	Aylett Creek at Aylett, Va.		6.17	1969-72	1969	4.50	320	June 22	4.75	625	20

James River basin

558	02011500	Back Creek near Mountain Grove, Va.		—	134
559	02012500	Jackson River at Falling Spring, Va.			411
560	02013000	Dunlap Creek near Covington, Va.		164
561	02014000	Potts Creek near Covingtco, Va.		153
562	02015700	Bullpasture River at Williamsville, Va.		HO
563	02016000	Cowpasture River near Clifton Forge, Va.		461
564	02016500	James River at Lick Run, Va.			—	1,373
565	02017300	Craig Creek near New Castle, Va.			112
566	02017400	Johns Creek tributary near New Castle, Va.		1.57
567	02017500	Johns Creek at New Castle, Va.	—	104
568	02017700	Craig Creek tributary near New Castle, Va.	—	2.0'
569	02018000	Craig Creek at Parr, Va.		—		329
570	02018500	Catawba Creek near Catawba, Va.							34.3
571	02018800	North Fcrk near Fine as tie, Va.		4.17
572	02019400	Mill Greek near Buchanan, Va.		29.6

1951-72	1967	10.77	12,700	June 21	9.25	8,270	
1913	1913	17	(1)				
1926-72	1936	14.74	24,700	June 21	12.72	16,100	5
1913	1913	20	50,000				
1929-72	1969	13.13	10,300	June 21	15.65	13,400	>100
1913	1913	18	(1)				
1929-56,	1935	10.10	7,510	June 21	12.33	12,400	60
1966-72							
1913	1913	12.5	CD				
1961-72	1967	5.91	6,230	June 21	4.54	3,720	3
1926-72	1936	18.62	34,200	June 22	12.63	15,700	5
1913	1913	20.8	45,000				
1924,	1936	25.65	66,600	June 21	27.01	66,300	25
1926-72							25
1877	1877	33	120,000				
1967-72	1969	10.49	3,600	June 21	17.09	16,500	80
1967-72	1971	4.32	75	June 21	8.48	354	8
1927-72	1935	10.80	8,000	June 21	12.48	7,960	60
1968-72	1970	6.38	252	June 21	7.85	372	7
1926-72	1935	17.0	19,100	June 21	19.29	20,200	50
1944-72	1954	6.58	2,780	June 21	10.35	7,740	65
7.940	1940	13.26	(1)				
1968-71	1968,	5.15	304	June 21	7.00	620	7
	1971						
1950-72	1961	10.83	7,200	June 21	9.08	4,370	6
1928	1928	14 1	(1)				

footnotes at end of table﻿382

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE A1 .—Summary of flood stages and discharges

Re-

port

No.

Perma-

nent

station

No.

Stream and place of determination

Drainage area (sq mi)

Maximum previously known

Gage

height

(ft)

Dis-

charge

(cfs)

Maximum June—July 1972

Gage

height

(ft)

Dis-

charge

(cfs)

Recur-

rence

interval

(years)

James River Las in--Continued

573

574

575

576

577

578

579

580

581 58s

583

581*

585

586

587

588

589

590

591

592

593

594

595

02019500

02020500

02021500

02022500

02023300

02021*000

02025500

02025800

02026000

02027000

02027500

02027700

02027800

02028500

02029000

020291*00

020291*50

02030000

02030100

02030500

02030800

02030900

02031500

James River at Buchanan, Va.------------------------

Calfpasture River above Mill Creek at Cosher, Va.—

Maury River at Rookhridge Baths, Va.

Kerrs Creek near Lexington, Va.------

South River near Steeles Tavern, Va. Maury River near Buena Vista, Va.— James River at Holcombs Rock, Va.--

Burton Creek tributary near Lynchburg, Va.'

James River at Bent Creek, Va.--------------

Tye River near Lovingston, Va.--------------

Piney River at Piney River, Va.---------------------

Buffalo River tributary near Amherst, Va.-----------

Buffalo River near Tye River, Va.-------------------

Rockfish River near Greenfield, Va.—----------———

James River at Scottsville, Va.---------------------

South Branch North Folk Hardware River near North Garden, Va.

Thomas Creek near Keene, Va.------------------------

Hardware River below Briery Run, near Scottsville, Va.

Frisby Branch near Buckingham, Va.-------—----------

Slate River near Arvonia, Va.—----------------------

Stockton Creek near Afton, Va.----------------------

Powells Creek near Crozet, Va.----------------—-—

North Fork Moormans River near Whitehall, Va.-------

596 02032200

597	02032300

598	02032530

599	02032550

600	02032550

601	02032600

602	02032680 '02033300

02033700 02031*000 02031*050 02031*500 02035000 020351*00 020351*50 02036500 02037500 02038000 02038800 02038850 02039000

603

60I*

605

606

607

608

609

610 611

612

613 6ll*

615

616

617

618

619

620 621

622

623

621*

625

626

627

628 629

630

631

632

633

631*

635

636

637

638

639

Doyles River near Whitehall, Va.--------------------

Muddy Run near Stanardsville, Va.-------------------

Parker Branch near Stanardsville, Va.---------------

Haneytown Creek near Stanardsville, Va.-------------

Lynch River near Hartonsville, Va.------------------

Swift Run tributary near Stanardsville, Va.---------

Marth Fork Rivanna River near Proffit, Va.-----------

Moores Greek near Charlottesville, Va.---------------

Henderson Creek near S halve 11, Va.----------------

Rivanna River at Palmyra, Va.------------------------

Hunters Branch near Palmyra, Va.--------------------

Willis River at Flanagan Mills, Va.------------------

James River at Cartersville, Va.---------------------

Big Lickinghole Creek tributary near Ferncliff, Va.'

Rocketts Creek tributary near Gum Springs, Va.-------

Fine Creek at Fine Creek Mills, Va.—-----------------

James River near Richmond, Va.----------------------

Falling Creek near Chesterfield, Va.-----------------

Appcmattax River near Appomattox, Va.----------------

Holiday Creek near Andersonville, Va.---------------

Buffalo Creek near Hampden Sydney, Va.--------------

02039500

02040000

0201*0600

0201*1000

0201*1650

0201*2500

Appomattox River at Farmvllle, Va.' Appomattox River at Mattoax, Va.--

Nibbs Creek tributary near Amelia, Va.-

Deep Creek near Mannbaro, Va.--------—

Appcmattax River at Matoaca, Va.-------

Chickahominy River near Providence Forge, Va.-

2,075

144

329

35.'

15.'

646

3,259

2

3,683

92

•3<

1*7.

ll*7

91*.

1*,581*

6,

5:

•2f

116

4.3:

226 2.8c 2.3: 11.1*

6.7c

3.3c

3.21

i*.i*:

13.6 .3:

176

3.52 1.76

661* 1.63 262 6,257

•55

.31*

22.1

6,758

32.8

5-79

8.53

69.7

303

726

158

l^W

21*8

•35

Chowan River basin

0201*1*000

0201*1*200

0201*1*1*00

0201*1*500

0201*5500

0201*6000

0201*7000

0201*7500

0201*8000

0201*9500

020501*00

02050500

02051000

02051500

02051600

02052000

02052500

Nottoway River near Burkeville, Va.

Falls Creek tributary near Victoria, Va. Hurricane Branch near Blackstone, Va.— Nottoway River near Rawlings, Va.---------

Nottoway River near Stony Creek, Va.-Stony Creek near Dinwiddle, Va.—-—

Nottoway River near Sebrell, Va.-----

Blackwater River near Dendron, Va.---

Blackwater River at Zuni, Va.--------

Blackwater River near Franklin, Va.—

North Msherrin River near Briery, Va.----

North Msherrin River near Keysville, Va.

North Msherrin River near Lunenburg, Va.

Meberrin River near Lawrencevllle, Va.-Great Creek near Cochran, Va.---------—

Meberrin River at Emporia, Va.-Fontaine Creek near Brink, Va.-

38.7

•3b

1.61

309

579

112

1,1*21

291*

1*56

617

1.19|

9.2

55.6

552

30.7

71*7

65.2

1930-72

191*7-72

1962-72

1967-72

191*0,

1951-72

1930-72

19U7-72

191*0-72

191*0-72

191*0-72

191*0-72

1966-72

191*9-61,

1966-72

191*0

191*7-72

19I1O

1873-1972

1958-72

1873-1972

1954-72

19W

1870-1972	1877	31*.9	11*2,000	June	22	30A9	111,000	100
1939-72	191*9	12.Ill	—	June	22	11.1*3	13,700	25
	1971	11.97	16,600					
1929-1972	1936	13.07	33,000	June	22	10.81	19,000	15
1927-72	1950	2/1.3.8	23,000	June	21	7.92	3,300	3
1951-72	1969	8.70	4,700	June	21	5.80	2,040	10
1936-72	1969	31.23	105,000	June	21	17.10	27,800	12
1900-17,	1969	35.50	150,000	June	22	32.28	126,000	70
1927-72								
1966-72	1970	5-1*0	380	June	21	7.88	790	35
1925-72	1969	21*.77	ll*l*,000	June	21	27.13	176,000	>100
1931*,	1969	29.0	80,000	June	21	11*. 34	12,200	15
1939-72								
191*9-72	1969	13.8	38,000	June	21	9.95	10,000	45
1966-72	1971	3-32	30	June	21	7.18	187	25
1961-72	1969	27.9;	1*5,000	June	21	25.22	36,600	>100
191*3-72	1969	31.2	70,000	June	21	18.11	17,500	15
1870-1972	1870	30.7	215,000	June	22	34.02	301,000	>100
191*9-72	1969	8.7	6,200	June	21	8.80	(1)	(1)
1966-72	1969	7.37	1*1*0	June	21	6.96	325	>100
1939-72	1969	31.0	52,000	June	21	25.50	21,600	50
1967-72	1971	7.80	800	June	21	16.50	2,110	>100
1927-72	1935	22. IE	26,900	June	22	25.10	42,200	>100
1967-72	1969	9-3	650	June	21	9.68	678	12
1967-72	1971	3.9£	Cl)	June	21	5.21	(1)	(1)
1952-72	1955	7.91*	2,1*00	June	21	7.1*2	2,190	30
191*2	191*2	11.7	7,620					
1967-72	1971	12.01*	CD	June	21	12.90	(1)	(1)
1967-72	1971	6.77	2,500	June	21	7.20	3,160	>106
1967-72	1969	8.51*	1,300	June	21	8.1*1*	1^270	
1967-72	1971	12.7C	520	June	21	13.72	l] 120	20
1967-72	1971	14.35	6,500	June	21	16.50	18,000	>100
1966-72	1971	6.2C	19	June	21	8.50	63	80
1970-72	1971	16.67	5,000	June	21	30.1*0	31,800	>100
1967-72	1969	16.85	2,000	June	21	16.30	790	20
1966-72	1969	9.60	2,000	June	21	11.59	(1)	(1)
1931*-72	1969	39.85	86,000	June	22	37.34	73,400	50
1967-72	1969	10.82	1,500	June	21	10.50	L400	>100
1927-72	1937	23-86	9,580	June	22	29.8	12/21*. 000	
1899-1972	1969	33.75	250,000	June	22	37.87	362,000	>100
1962-72	1969	5.55	600	June	21	4.93	’280	
1966-72	1969	9-72	190	June	21	9.58	187	
191*5-72	1961	8.35	3,61*0	June	22	6.60	2,140	
1935-72	1969	21*.95	222,000	June	23	28.62	313,000	>100
1955-72	i960	12.67	2,510	June	22	8.46	'6l4	
1955-72	1971	6.06	780	June	21	8.68	3,870	>100
1967-72	1971	5.21*	635	June	21	14.64	9*640	
191*7-72	1971	11.96	8,280	June	21	12.38	9,160	>100
191*0	191*0	15 „	fl)					
1927-72	191*0	23.60	21,000	June	22	29.70	33,100	>100
1901-05,	1940	35.3	35,ooo	June	25	34.08	31,100	75
1927-72								
1966-72	1969	8.00	us	June	21	9.48	740	>160
191*6-72	1971	19.53	10,200	June	22	16.93	7,640	
191*0,	1971	l**-35	22,000	June	27	14.60	22,800	25
1970-72		11.67						
191*2-72	1955		7,710	June	25	10.07	3,440	6

191*0

1971

1971

1971

1971

19I1O

1971

19I1O

191*0

191*0

19I1O

1971

1971

191*0

1971

191*0

191*0

1959

1966

19I1O

1958

191*0

27.I*

22.33

5.75

9.20

21.36

23.66

15.07

29.7 13.1

22

7.85

7.9!*

10.3

28.30

1*8

1*2.0

14.58

31.5 I8.18

18.5

(1)

13,1*00

138

1*1*0

23,900

25,200

5,03°

1*8,000

10,000

16,000

21,000

1*72

1,670

,(D

ll*,l*00

(l)

38,000

l*,8l0

1*0,000

2,660

(1)

June 21 June 21 June 22

June 21* June 23 June 27 June 24 June 26 July 2 July 16 June 21 June 21

June 23 June 22

June 2k June 22

21.95

9.15

13.31

20.42

19.85

8.72

18.58

l+.l*6

8.25

8.7U

7.65

8.03

20.65

23.96

15.31*

21.81*

13.60

11,800

'31*3

1,31*0

21,100

8,630

1,01*0

9,81*0

81*8

1,010

1,610

448

1,720

1*,780

9,760

5,1*70

9,770

1,600

>100

>100

>100

6

<2

1*

<2

<2

<2

35

60

1*

20﻿APPENDIX A

383

TABLE A1 .—Summary of flood stages and discharges —Continued

Re-  port  No.				Maxi	mum prt	viously known		Maximum June—July 1972			
	nent  station  No.	Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Roanoke River, basin

640

641 61*2 61*3

61*1*

61*5

61*6

61*7

61*8

61*9

650

651

652

653

651*

655

656

657

658

659

660

661 662 663

661*

665

666

667

668

669

670

671

672

673 67U

675

676

677

678

679

680

681

682

683

681+

685

686

687

688

689

690

691

692

693 69^ 695

696

697

698

02053800

0205^500

02055000

02055100

02056000

020571*00

02057700

02058400

020591+00

020591+50

02059500

02060500

02061500

02062500

02063600

02063700

02061+000

02065100

02065200

02065300

02065500

02066000

02066500

02068500

02068610

02068660

02069030

02069700

02070000

02070500

02070810

02071000

020711+10

02071900

02072000

02072500

02073000

02071+000

02071+500

02075000

02075160

02075230

02075500

02075900

02076200

02076500

02076600

02076700

02077000

02077200

02077210

020772lt0

02077250

02077300

02077310

02077500

020791+90

0207961+0

02080500

South Fcrk Roanoke River near Shavsville, Va. -

Roanoke River at Lafayette, Va.-----------------

Roanoke River at Roanoke, Va.-------------------

Tinker Creek near Daleville, Va.----------------

Roanoke River at Niagara, Va.-------------------

Smith Mountain Lake near Penhook, Va.-----------

Powder Mill Creek at Rock Mount, Va.------------

Pigg River near Sandy Level, Va.----------------

Leesville Lake near Leesvllle, Va.--------------

South Fork Goose Creek at Montvale, Va.---------

Goose Creek near Huddleston, Va.----------------

Roanoke (Staunton) River at Altavista, Va.------

Big Otter River near Evlngton, Va.--------------

Roanoke (Staunton) River at Brookneal, Va.------

Button Creek near Rustburg, Va.-----------------

Button Creek tributary near Rustburg, Va.-------

Falling River near Iferuna, Va.-----------------

Shake Creek near Brookneal, Va.-----------------

Roanoke (Staunton) River at Clarkton, Va.-------

Right Hand Fork near Appanattax, Va.------------

Cub Creek at Phenix, Va.------------------------

Roanoke (Staunton) River at Randolph, Va.-------

Roanoke Creek at Saxe, Va.--------------------—

Dan River near Francisco, N. C.-----------------

Hog Rock Creek near Moores Springs, N. C.-------

Little Snow Creek near Lawsonvilie, N. C.-------

Belews Creek near Kernersville, N. C.-----------

South Mayo River near Nettleridge, Va.----------

North Mayo River near Spencer, Va.--------------

Mayo River near Price, N. C.--------------------

Jacobs Creek near Wentworth, N. C.--------------

Dan River near Wentworth, N. C.------------------

Matrimony Creek near Leaksville, N. C.----------

Philpott Lake near Philpott, Va.-----------------

Smith River near Philpott, Va.-------------------

Smith River at Bassett, Va.---------------------

Smith River at Martinsville, Va.--------—----—

Smith River at Eden, N. C.----------------------

Sandy River near Danville, Va.------------------

Dan River at Danville, Va.—---------------------

Moon Creek near Yanceyville, N. C.--------------

South Country Line Greek near Hightowers, N. C. Dan River at Paces, Va.-------------------------

Lawsons Creek near Turbeville, Va.--------------

Bearskin Creek near Chatham, Va.----------------

Georges Creek near Gretna, Va.------------------

Whitethorn Creek tributary near Gretna, Va.-----

Blacks Creek near Mt. Airy, Va.-----------------

Banister River at Halifax, Va.------------------

Hyco Creek, mear Leasburg, N. C.»---------------

Kilgore Creek tributary near Leasburg, N. 0.

Double Creek near Roseville, N. C.--------------

South Hyco Creek near Roseville, N. C.----------

Hyco River at McGehees Mill, N. C.--------------

Storys Creek near Raxbaro, N. C.----------------

Hyco River near Denniston, Va.------------------

John H. Kerr Reservoir near Boyd ton, Va.-------

Allen Creek near Boydton, Va.-------------------

Roanoke River at Roanoke Rapids, N. C.-----------

110

257

395

11.7

512

1,02k

350

1,505

7.

188

.61*

56

1,789

320

2,1*15

•59

.16

173

1.68

2,691

2.08

98.0

2,977 135 121*

•30

5A

15

81*.6 108 260

16

1.050

12.0 216 216 259 380 538

112

2.050

29.9

7.1

2,550

8.7

1*.06

9.21*

1.93

3.1*1*

5l*7

1*1* .0

.22

7.1*7

55

191

2.0

289

7,780

53.1*

8,1*10

1961-	72 1959 I9I0-72 1899-1972

1957-	72

19i*0

1927-72

1963-	72 1967-72

1964-	72

1962-	72 1967-72

1924-27,

1930-	72 1928

1931-	72

1937-	72

1878,

1924-	72

1966-	72

1962-	72 1930-34, 1940-72

1967-	72

1964-72

1964-	72

1946-	72 1940 1878,

1901-72

1947-	72 1940

1925-	72 1916 1954-72 1954-72 1954-72

1963-	72

1929-	72

1930-	72 1954-72 1940-72 1908

1958-	72

1950-	72 1947-72

1938-	72 1930-72 1940-72 1930-72 1892-1972 1954-72 1954-72

1951-	72 1940 1951-72 1967-72

1950-	72 1966-72

1966-72

1905,

1929-72

1965-	72

1954-72

1965-72

1962-72

1965-72

1954-72

1929-34,

1951-	72 1928 1950-72 1962-72 1771-1972

1967 1959 1940 1940

1961 1940 1940 1971 1969

1964

1965

1968 1937

1928 1940 1937

1939

1940

1971

1964

1940

1971

1967

1971

1948 1940

1940

1971

1940

1937

1916

1964

1962

1969

1970 1947 1937 1954 1945 1908 1969

1971

1949 1937 1937 1940 1940 1940

1954

1955

1954 1940 1959 1967 1967

1967 1971 1944

1968 1961 1968 1968 19 66

1955

1929

1928

1958

1971

1940

6.

9.

12.

18.

8,

9.

17.

4/795.

15.

21.

4/614,

5.

25.

3,340 (1)

19,000 22,800 2,180 (1) ■J 24,400 ‘1,146,500 1.58 14,900 5/98,180 750

20,300

2/35.3

4o.o8

23.1

46.5

4.05

4.65

26.5^

7.10

24.87

9.50

13.0

17.5

41.6

15.

6/25

12,

15

22,

23,

24, 10, 15, 14, 28, 27,

34,

1 / 17'

4/977,

20,

22,

21,

19

14,

20,

20,

22,

25, 32, 14, 11,

7,

5,

10,

4o,

35.92

24.21

4.74

21.0C

15.5£

20.9=

21.8E

. . 26.4 4/309 21.8c 39.0

OiH.

(1)

105,000

27,500

130.000

72

45

22,000

380

24,700

400

2,720

(1)

150.000

7,110

(1)

12,400

16,000

279

2,000

3,600

3,290

17,200

30.000 2,800

38,100

(1)

2,300

5/174,740

17.000 38,200

39.000 45,600

23.000

75.000 3,050 2,360

34.000

(1)

7,740

1,530

1,440

340

870

50.000

2,480

252

892

2,400

3,870

350

7,630

(1) 1,965,700 5,620

261.000

June 21

June 21 June 21 June 21

June 21 June 22 July 5 June 22 June 23 June 21 June 21

June 22 June 21

June 21 June 21

June 22

June 21 June 22 June 21 June 22

June 23

June 21

June 21 June 21 June 21 June 21 June 21 June 21 June 21 June 22

June 21 June 22 June 22 June 21 June 21 June 21 June 21 June 22 June 21 June 21 June 23

June 21 June 21 June 21 June 21 June 21 June 22

June 21 June 21 June 21 June 21 June 22 June 21 June 22

June 27 June 22 June 28

11.12

15.60

19.61

9.82

18.98

4/797.6

15.65

24.07

4/613.0

8.10

19.43

26.78

21.03

34.27

5.65

4.35

29.21

10.00

35.56

15.54

20.37

30.96

13.11

6/14.79

9.32

19.95

24.3 24.87 18.32 13.41

14.02

30.2 31.60

18, 4/983, 8, 8, 14. 16, 9. 21.

13. 17. 33.

14.

13.

7.

7.

2l:

2.97

21.74

I5.I5

20.7

16.82

4/314, 16.80 9*55

14,200

24,500

25,300

4,000

5/ 28,800 T, 200,600 202 22,700 5/94,960 2,060 13,600

37,300

18,800

58,400

152

35

32.600

o 715

85.500 705

7,380

72.500

4,270

7,530

145

3,000

5,600

16,100

12.600 27,100

4,500

54.200

2,800

5/191,700

4,560

6,550

20,900

24.800

10.500

59.200 4,010

1,050

64.800

2,040

1,920

1,160

510

1,080

16,000

2,54o

(1)

178

2,770

3,420

320

3,820

58 ^

,332,300

2,160

24,600

>100

>100

>100

>100

>100

(I)

25

(i)

10

4

15

10

8

3

>100

>100

10

50

25

15

25

11

3

>100

100

75

35

50

35

>100

100

(lj

m

25

25

50

3

25

10

10

10

10

10

10

<2

4

15

(1)

See footnotes at end of table.﻿384

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

TABLE Al.—Summary of flood stages and discharges—Continued

	Perma-  nent  station  No.			Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Allegheny River basin

31.3					
44.6				—	...
7.79	1960-72	i960	6.9:
55.2	— -	—	...
160	—	—		
550	1940-72	1942	27.6
37.0	—	—	—
45.7	—					
2.1	1967	1967	—
198	1959-68,  1970-72	1967	16.06
1,608	1904-72	1956	15.11
46.4	1966-72	1967	
2,180	1966-72	1969	
2,223	1936-72	1956	19.9:
290	1939-72	1947	—
		1956	n.5f
17.6	1954	1954	
189	1950-72	1956	10.61
194	1935-72	1947	4.56
816	1940-72	1947	10.6s
	1936	1936	10.9
9.64	1962-72	1966	2.96
12.8	1963-72	1972	5.3:
12.3	1964-72	1964	6.3c
321	1910-72	1913	14.2
3,660	1942-72	1956	17.2c
233	1938-72	1959	11.2'
10.8	1961-72	1969	4/ 3-87 -1,161.5:
478	1941-72	1964	
479	191*1-72	1964	
		1964	11.33
4.37	1964-72	1964	9.9S
300	1910-72	1959	4/ 11-97 263.9C
220	1970-72	1972	
221	1910-72	1947	13.5C
3.60	1961-72	1969	4.9C
1,028	1912-72	1913	15.7
166	1932-72	1946	11.4s
5.69	196]-72	1968	5.17
5,982	1864-1972	1865	25.0
5.88	1963-72	1963	3.3:
		1964	3.3:
		1966	3.3:
7.84	1952-72	1967	4/ 11-7S ^,676.5!
72.4	1952-72	1956	
73.2	1949-72	1957	7.2'
	1946	1946	8.3
63.0	1954-72	1967	10.01
204	1946-72	1946	9.2
	1942	1942	16.7
303	1941-53	1942	16.4
8.67	1960-72	1964	7.22
12.6	1960-72	1964	2/4.37
		1964	4.17
807	1935-72	1936	19
951	1935-72	1936	(1)
7,671	1865-1972	1665	29.4
	1959	1959	I/29.6c
2.12	1965-72	1966	6.43
7.38	1964-72	1966	6.2;
528	1919-72	1936	I/18.6C
158	1936-72	1936	2/15.6
87.4	1940-72	1952	11.42
		1959	L/2A3.86  -£,161,32
340	1942-72	1964	
344	1939-72	1942	8.1c
8,973	1806-1972	1913	30.7
191	1936-72	1936	18.6
277	1941-72	1948	4/889.02
278	1910-72	1936	17.86
3.68	1961-72	1961	5.3C
1*51	1914-72	1936	30.26
183	1935-72	1936	(1)
715	1935-72	1936	26.4
192	1952-72	1954	12.67
4.39	1964-72	1969	,8.33
7.36	1960-72	1963	5/5.56
		1964	i/ 5.06  -i, 282.90
52.5	1971-72	1972	

699

70c

701

705

703

704 70;

706 707

70f

709

710

711

712

713

714

Vi

716

717

7l£

719

720

721

722

723

724

725

726

727 72£

729

730

731

735 733 73*< 73!

736

737

736

739

740

741

742

743

744

74:

746

747

74£

749

750

751

752

753

754

755

756

757

758

759

760

761

762

763

03010500

03010678

03010718

03010783

03010800

03011020

03011800

03012520

03012600

03013000

03013070

03013990

03014500

0301500C

03015080

03015280

03015390

03015500

03016000

03017500

03017800

03019500

03020000

03020440

03020500

03021518

03021520

03021700

03024000

03025000

03025200

03025500

03026400

03026500

03027000

03027500

03028000

03028500

03029000

03029200

03029400

03029500

03030500

03031500

03031780

03031950

03032500

03034000

03034500

03035500 03036000 03036500 03038000 03038500 03039000 03039200 03040000 03043TOO

03041500 03042000 764 03042170 76; 03042200

766 03042260

Mill Creek at Coudersport, Pa.----------------

Allegheny River at Coudersport, Pa.-----------

Be veil Creek near Part Allegany, Pa.---------

Marvin Creek at Smethpart, Pa.----------------

Potato Creek at Smethpart, Pa.----------------

Allegheny River at Eldred, Pa.---------■------

Little Genesee Creek at Little Genesee, N. Y.

Dodge Creek at Partville, N. Y.——-------------

Johnson's Creek at Cuba, N. Y.----------------

Olean Creek near Olean, N. Y.-----------------

Allegheny River at Salamanca, N. Y.--

Kinzua Creek near Guffey, Pa.--------

Allegheny Reservoir near Kinzua, Pa.'

Allegheny River at Warren, Pa.-------

Conevango Creek at Waterbaro, N. Y.-

Mill Creek at Sine lair ville, N. Y.~ Chautauqua Lake near Mayville, N. Y.-Chadakoin River at Falconer, N. Y.--Conevango Creek at Russell, Pa.------

Akeley Run near Russell, Pa.----------

Jackson Run near North Warren, Pa.----

Hare Creek near Carry, Pa.------------

Broke ns trav Creek at Youngsville, Pa.-Allegheny River at West Hickory, Pa.-

Tionesta Creek at lynch, Pft*---------

Minister Creek near Truemans, Pa*-----

Tionesta Lake at Tionesta Dam, Pa.----

Tionesta Creek at Tionesta, Ra.-------

West Branch Caldwell Creek near Grand Valley, Pa.—

Oil Creek at Rouseville, Pa.-------------------------

Union City Reservoir near Union City, Pa.------------

French Creek near Union City, Pa.-----------------—

Little Conneauttee Creek near McKean, Pa.------------

French Creek at Utica, Pa.---------------------------

Sugar Creek at Sugar creek, Pa.----------—-----------

Patchel Run near Franklin, Pa.--------------------

Allegheny River at Franklin, Pa.-------------------—

Richey Run at Ernienton, Pa.-------------------------

Sevenmile Run near Rasselas, Pa.------------------

East Branch Clarion River Lake at East Branch Clarion River Dam, Pa.

East Branch Clarion River at East Branch Clarion River Dam, Pa.

West Branch Clarion River at Wilcox, Pa.----------

Clarion River at Johnsonburg, Pa.----------------

Clarion River at Ridgvay, Pa.-Clear Creek near Sigel, Pa.-— Toms Run at Cooksburg, Pa.-----

Clarion River at Cooksburg, Pa.-

Clarion River near Piney, Pa.---

Allegheny River at Parker, Pa.—

Mill Creek near Brockway, Pa.------------

Big Run near Sprankle Mills, Pa.—--------

Redbank Creek at St. Charles, Pa.—-——

Mahoning Creek at Punxsutavney, Pa.------

Little Mahoning Creek at McCormick, Pa.-

Mahoning Creek Lake at Mahoning Creek Dam, Pa.-

Mahoning Creek at Mahoning Creek Dam, Pa.------

Allegheny River at Kittanning, ftt.------------

Crooked Creek at Idaho, Pa.--------------------

Crooked Creek Lake at Crooked Creek Dam, Pa.—■

Crooked Creek at Crooked Creek Dam, Pa.--------

Clear Run near Bucks town, Pa.---------------—

Stony Creek at Ferndale, Pa.------------------—

Little Conemaugh River at East Conemaugh, Pa.-

Conemaugh River at Seward, Pa.------------

Blacklick Creek at Josephine, Pa.---------

Stony Run at Indiana, Pa.-----------------

Little Yellow Creek near Strongs town, Pa.-

Yellow Creek Lake at Yellow Creek State Park, Pa.—

7^0

55,000

632

18,200

49,100

, 4,090 719,560

60.500 8,600

2,740

2,050

14.400

14.600 735

1,020

I,	370

18.000

101,000

15.000 726

6111,320

13.500

500

21,000

5/21,600

20,000

830

35.600

10,000

504

196.000 509 509 509

1,620

5/73,230

2,590

4,000

5,490

II,	700

(1)

34.000 766

656

56.000

50.000

250.000

306

822

50.000

12.500 5,300

5/72,580

10.400

269.000

19.400 5/58,020

21.000

250

59.000

28,800

90.000 11,900

394

,	541

5/l6,4io

June 22 June 22 June 21 June 22 June 22 June 23 June 23 June 23 June 23 June 23

6.40

29.05

11.52

June 23 June 22 r /

June 27 £1,362.:

June 28 June 26

June 23 June 25 June 24 June 26

June 23 June 23 June 23 June 23 June 25 June 23 June 23 June 25 June 27

June 23 June 23 June 26 June 26 June 23 June 26 June 23 July 2 June 25 June 23

June 21 June 24

June 24

June 22 June 22

June 23 June 22 June 22

June 23 June 23

June 23

June 22 June 22 June 23 June 23 June 23

June 27 June 27 June 23 June 23 June 25 June 25 June 23 June 23 June 23

June 23 June 23 June 23 June 23

June 23


24.01

■“I*

14.12

10.16

10.17 4.01 8.81

2.60 4.22 5.63 IO.78

11.18

10.42

,/	3.41

8.59

10.25

,264.30

8.00

4.52

10.01

9.85

6.28

15.84

3.4o

4/	4.84

-1,685.55

6.03

9.64 9.94

19.49 7.57

3.65

18.84

22.23

6.15 6.11 17.75 15.94 13.20

^,160.16

7.85 25.42

, . 15.93 4/901.29

8.85 4.53

13.36 10.48

I8.93

13.99 8.56 6.10

-,285.02

i

3,490

5,790

3.000

4.200 12,800

65.400 8,330

4.200 609

6.000

73.000 5,220

,121,120

25.000

з,	970

2,070

1.650 9,920

683

627

744

и,	8oo 42,300

12.400

, 539 5/72,080 8,890

397

12.000

5/22,170

2,880

596

13,600

8,240

1.650

85.400

521

976

5/85,010

1,810

4,900

11,600

19,000

871

532

53.300 74,500

147.000

235

854

32.800

17.300

6,200

2/69,870

7,820

184.000 13,200

5/61,450

5,350

266

22.800

16,600

49.300 20,800

420

820

5/18,420

80

>100

>100

40

100

>100

>100

15

(1)

3

>100

>100

(i)

2

a

a?

3

2

3

0?

16

<2

4

7

U)

.25

(D

10

>100

(1)

5

(1)

18

(1)

(1)

3

11

>100

>100

(1)

4

14

60

>100

50

8

’ 6

<2

11

>100

>100

>100

<2

1*0

See footnotes at end of table.﻿APPENDIX A

385

TABLE Al.—Summary of flood stages and discharges--Continued

Re-

port

No.

Perma-

nent

station

No.

Stream and place of determination

Maximum previously known

age			Gage	Dis-
area	Period	Year	height	charge
(sq mi)			(ft)	(cfs)

Maximum June-Jcly 1972

	Gage	Dis-	Recur-
Date	height  (ft)	charge  (cfs)	rence  interval  (years)

Allegheny River basin—Continued

768

769

770

771

772

773

TJh

775

776

777

778

03042280	Yellow Creek near Hcmer City, Pa.		59.5	1968-72	1968  1971
03042500	Tvolick Creek at Graceton, Pa.		171	1952-72	1954
03043500	Conemaugh River Lake at Conemaugh River Dam, Pa.		1,351	1952-72	1964
03044000	Conemaugh River at Tunnelton, Pa.		—			1,358	1940-72	1945
03045000	Loyalhanna Creek at Kingston, Pa.—-—						172	1918-72	1954
03046500	Loyalhanna lake at Loyalhanna Dam, Pa.			290	1943-72	1948
03047000	Loyalhanna Creek at Loyalhanna Dam, Pa.—				292	1940-72	1941
03048500	Kiskiminetas River at Vandergrift, Pa.			1,825	1920-72	1936
03049000	Buffalo Creek near Freeport, Pa.—		—				137	1941-72	1954
03049100	Little Buffalo Creek at Cabot, Pa.—		—			4.66	1959-72	1962
03049500	Allegheny River at Natrona, Pa.		—			n,4io	1936-72	1936
03049800	Little Pine Creek near Etna, Pa.		—-—				5.78	1963-72	1963  1971

3/7.

3/8,

i»/968, 21, . . 15. i/956, 1°, •a. 13, 5,

32,


76

1,300	June 23
12,900	June 23
i/230,520	June 25
59,200	June 25
29,700	June 23
5A7,910	June 25
11,700	June 30
185,000	June 25
14,000	June 23
326	June 23
365,000	June 23
360	June 23

7.46

14.69

V 969A5 12.60 13.76 4/967.1*1 8.05 17.81 11.21 7.49

3.82

4,100

19,600

5/237,980

25,900

21,500

5/72,830

6,080

32,600

9,980

404

205,000

357

779

780

781

782

783

784

785

786

787

788

789

790

791

792

793

794

795

796

797

03050000

03050500

03050650

03051000

03052000

03052300

030523to

03052500

03053500

03054500

03055020

03055500

03056600

03057000

03057500

03058000

03058500

03059000

03061000

798

799

800

801

802

803

804

805

806

807

808

809

810

811

812

813

814

815

816

817

818

819

820

821

822

823

824

03061500

03062400

03062500

03063600

03065000

03066000

03069000

03069500

03069650

03069850

03069880

03070000

03070500

03072000

03072500

03072590

0307281*0

03072880

03073000

03071*300

03074500

03075000

03075450

03075500

03075600

03076000

03076500

Tygart Valley Elver near Dailey, W. Va.-

Tygart Valley River at Elkins, W. Va.----

Unnamed Run at Gilman, W. Va.------------

Tygard Valley River at Belington, W. Va.,

Middle Fork River at Audra, W. Va.— Bridge Run near Buckhannon, W. Va.— Mud Lick Run near Buckhannon, W. Va.

Sand Run near Buckhannon, W. Va.-----

Buckhannon River at Hall, V. Va.----

Tygart Valley River at Philippi, W. Va.-

Bonica Run on U.S. Highway 250 near Philippi, W.

Tygart Lake near Grafton, W. Va.------------------

Right Fork Wickwire Run on U.S. Highway 119 near Grafton, W. Va.

Tygart Valley River at Colfax, W. Va.-----------—

Skir. Creek near Brownsville, W. Va.-

West Fork River at Brownsville, W. Va.— West Fork River at Butchsrville, W. Va.-West Fork River at Clarksburg, W. Va.— West Fork River at Enterprise, W. Va.—

Buffalo Creek at Barrackville, W. Va.-

Cobun Creek at Morgantown, W. Va. v-Deckers Creek at Morgantown, W. Va.,

Horse Camp Run at Barman, W. Va.----

Dry Fork at Hendricks, W. Va.-------

Blackwater River at Davis, W. Va.— Shavers Fork at Parsons, W. Va.-----

Cheat River near Parsons, W. Va.-----------

Right Fork Clover Run near Parsons, W. Va.

Long Run near Parsons, W. Va.--------------

Buffalo Creek near Rowlesburg, W. Va.------

Cheat River at Rowlesburg, W. Va.----------

Big Sandy Creek at Rockville, W. Va.

Dunkard Creek at Shannopin, Pa.—— Monongahela River at Greensboro, Pa.

Georges Creek at Smithfield, Pa.-----------

Tenmile Creek near Clarksville, Pa.--------

Browns Creek near Nineveh, Pa.-------------

South Fork Tenmile Creek at Jefferson, Pa.,

Lick Run at Hqpwood, Pa.-------------------

Redstone Creek at Waltersburg, Pa.---------

Monongahela River at Charleroi, Pa.--------

Little Youghiogheny River tributary near Deer Park, Ml.

Youghiogheny River near Oakland, Mi.---------------

Toliver Run tributary near Hoyes Run, Mi.

Deep Creek Reservoir near Oakland, Mi.----

Youghiogheny River at Friendsville, Mi.—

187  272	1916-72  1945-72	1932  1969	17.2  15.65  10.90  21.7	13,100	June 23	12.77
.38	1964-72	1964		13,100	June 2k	14.42
408	1888,	1888		310	June 23	4.25
	1908-72			21,200	June 23	17-52
149	1943-72	1967	12.68  U.4o			
2.60	1967-72	1969		10,900	June 23	13.67
2.33	1967-72	1969		330	June 23	9*50
14.5	1947-72	1950	7*90  15:0?	250	June 23	6.72
277	1908,	1967		2,000	June 23	6.07  14.42
	1916-72			13,000	June 2k	
916	1940-72	1967	li*93	43,000		
	1912	1912			June 23	24.67
.60	1965-72	1971		(1)		
1,184	1939-72	1958	4,15^	^43,600	June 23	,/ '*•9°
2.33	1965-72	1969			June 25	4.,155-22
				430	June 23	7-50
1,366	1940-72	1948	46.86  £A9.77			
	1946-72	1963		22,500	June 25	13-85
25.7		1957		—		
		1950	7.90  8.64  17.20  16.81  23.4°  28.05	2,280	June 23	4.85
102	1947-72	1950		—-		
181	1916-72	1950		6,420	June 23	9.89
384	1924-72	1967		18,000	June 23	6.21
7^9	1908-16,	1967		17,800	June 2k	9-36
	1934-72  1888	1888		36,500	June 2k	12.10
			33  18			
115	1908, 1912	,1912		(1)		
	1916-23,  1933-72			11,600	July 17	6.77
						
10.9	1965-72	1967	9.87			
63.2	1947-69	1956		983	June 23	12.80
6.57	1970-72	1970		5,680	June 23	9.40
3^5	1941-72	1954	15.23  ,13.20  7/ip 5	304	June 23	3.58
86.2	1922-72	1924		47,000	June 23	9.67
214	1888,1907,	1888		7,170	June 23	6.86
	19U.-26,  1941-72			25,000	June 23	10.15
718	1888-1972	1954	19.08			
2.21	1967-72	1968		52,100	June 23	13.79
.95	1967-72	1969		(1)	June 23	4.50
12.2	1968-72	1971	5.66	205	June 23	7.36
972	1844,1888,	1844		2,69°	June 23	4.56
	1912-18,  1921,  1925-72		J-O.7	89,000	June 23	13.**6
200	H88,  1910-72	1888	20	30,000	June 23	15.86
229	1941-72	1941	1>*.02  29.61			
4,407	1936,  1939-72	1967		16,800  13^,000	June 23 June 23	2?$
	1888	1888	36  6.80  10*8?	(1)		
16.3	1964-72	1967				
133	1969-72	1971		1,100	June 23	10.01
17.5	1963-72	1963		4,200	June 23	6.28
180	1932-72	1941	18.45  3.85	2,100	June 23	10.02
3.80	1959-72	1971		13,800	June 23	12.07
73.7	19i*3-72	1954		371	June 23	4.30
5,213	1887-1972	1888		4,400	June 23	14.83
		1967	11.63  5.05	156,000	June 2h	35->*
• 57	1965-72	1968		158,000		
131*	1942-72			32	June 29	5.31
		1954				
	1936	1936	J^.16	11,800	June 23	8.01
•53	1965-72	1971 k 1949 3	, v L	(1)		
64.7	19e6-72			, 60	June 23	/ 5 «°3
295	1898-1972	1924		5/93,258	July 6	£,460.3
				15,600	June 23	6.72

10,400

10,800

25

15,800

U,500

145

110

1,050

12,000

39,500

86

2/251,100

220

16,800

900

2,000

2,790

4,700

9,740

1,340

1,770

5,120

223

16,900

1,920

11,800

33,600

(1)

65

1,520

55,000

16,200

iol;ooo

1,640

6,620

1,420

6.980 690

8,660

110,000

40

4.980

5/86,700

7,250

(1)

(1)

6

50

<2

10

25

<2

(1)

<2

Ik

10

<2

15

90

<2

<2

1+

22

ko

3

2

<2

<2

<2

<2

<2

<2

60

ko

<2

k

<2

8

6

(1)

<2

15

15

22

7

4

3

2 12

>100

3

(1)

3

(1)

2

See footnotes at end of table﻿386

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE A1 .—Summary of flood stages and discharges—Continued

				Maximum previously known				Maximum June—July 1972			
Re-  port  No.	nent  station  No.	Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Mbnongabela River basin—Continued

82;

826

827

828

829

830

831

832

833 83J*

835

836

837

838

839

8I0

81*1

03076600

03077000

03077500

Bear Creek at Friendsville, Mi.-------------------—

Youghiogheny River Lake at Youghiogheny River Dam, Pa.

Youghiogheny River at Youghiogheny River Dam, Pa.---

03077700

03078000

O30785OO

03079000

03080000

03081000

03082200

03082500

North Branch Casselman River trihutary at Foxtown, Mi.

Casselman River at Grantsville, Md.----------------

Big Piney Run near Salisbury, Pa.------------------

Casselman River at Markleton, Pa.------------------

Laurel Hill Creek at Ursina, Pa.-------------------

Youghiogheny River below Confluence, Pa.——---------

Poplar Run near Narmalville, Pa.------—------------

Gist Run near Dunbar, Pa.--------------------------

Youghiogheny River at Connellsvllle, Pa.-----------

03083000

Green Lick Run at Green Lick Reservoir, Pa,

03083500

Youghiogheny River at Sutersville, Pa.-

03083600

03081*000

03085000

Gillespie Run near Sutersville, Pa. Abers Creek near Murrysville, Pa.--Monongahela River at Rraddock, Pa.-

I8.9	1965-72	1971	L/ 9«6	-/ 11,650	June	29	,/ 5.12	1,880	<2
1+34	19II-72	1967	^,1(57.23	2210,250	June	26	4,152.11	5/191,810	
1*36	191(0-72	195l(	6/19.05			June	27	8.39	6,710	3
	1965-72	191(8	11.25	13,700					
1.0		1971	6.31	81	June	23	1.92	51	a)
62.5	191(8-72	195l(	10.70	8,100	June	23	1.80	1,820	<2
2U.5	1933-72	1951	8.56	6,850	June	23	3.83	'686	<2
382	1915-72	195l(	ll.OC	50,000	June	23	8.83	11,300	3
121	1918-72	1951	10.6;	10,900	June	23	7.08	6,350	5
1,029	1936-72	1936	21.6	85,000	June	23	11.88	23,200	5
9.27	1962-72	1971	8.3'	1,890	June	23	6.76	L210	5
7.36  1,326	1860,1888,  1891-99,	1951	21.95	103,000	June  June	23  23	16.53	1,230  51,600	10  10
	1901-72								
3.07	191(2-72	19l(3  19U	5.1  5.1*2	1,100	June	23	3.13	818	17
1,715	1921-72	1951	32.5	108,000	June	23		83,000	30
l.ol		1969			June	23	•229.7		
	1959-72		6.2;	586	June	23	5.25	586	5
1(.39		1950	7.72	1,600	June	23	5.78	720	5
7,337	1936-72	1936	38.8	£10,000	June	24	31.39	180,000	22

Ohio River main stem

03086000		19,500  26,850  (1)  35,600  (1)	1931-72  1881-1972  1939-72	1936	31.7!  51.2  16.67  (1)	571.000 (1)  121.000	June 2)*	21.12		
									370,000	w
				1913  (1)			June 25	38.18	382,000	(1)
03150800  03160000			1969-72  1936-37,  19IO-72  1913			M	June 25	30.65	M	—
					31.7:  (1)  (1)	(1)  551,000  633,00c	June 26	36.09	1	—
				1913			June 26	13.71	(1)	

Kanawha River basin

817	03180500	Greenbriar River at Durbin, W. Va.				13U	19II-72	1956  1967
81£	03180680		1.52	1966-72	1970
81?	03181200	Indian Draft near Mar lint on, W. Va.		 ■ —	3.06	1969-72	1969
850	03181900	Moody Moore Hollow near Huntersville, W. Va.-		•55	1966-72	1969
851	03182500	Greenbriar River at Buckeye, W. Va.				5^0	1930-72	1932
852	03182650	Spring Creek at Spring Creek, W. Va.			120	1972	1972
853	03182700	Anthony Creek near Anthony, W. Va.		—	ill	1972	1972
85I		Dry Fork at White Sulphur Springs, W. Va.		23.0	—	—
855	03182950	Howard Creek at Caldwell, W. Va.				—		—	81.1	1972	1973
856	03183000	Second Creek near Second Creek, W. Va.—			80.8	191,6-72	1958
857	03183500	Greenbriar River at Alder son, W. Va.		—		1,357	1896-1972	1918
858	03183550	Griffith Creek near Alders on, W. Va.		—				3.81,	1966-72	1969
859	03181000	Greenbriar River at Hi 11 .dale, W. Va.—	—	1,625	1936-72	1936  1967
860	0318I200	Big Creek near Bellepoint, W. Va.-						8.27	1970-72	1972
861	03186500	Williams River at Dyer, W. Va.—			—	128	1930-72	1932
862	03187000	Gauley River at Camden Gauley, V. Va——			236	1909-16,  1930-72	1932
863	03189100	Gauley River near Craigs vllle, W. Va.		—	528	1965-72	1967
861	03189590	Summers vllle lake near Summer sville, W. Va.	—	803	1966-72	1966
865	03189600	Gauley River below Summer sville Dam, W. Va.		——	804	1967-72	1966
866	03193830	Gilmer Run near Marlinton, W. Va.		1.80	1969-72	1971
867	03191700	Elk River below Webster Springs, W. Va.		268	1960-72  1861	1967  1861
86£	03195100	Sutton Lake at Sutton, W. Va.		537	1961-72	1961
869	03195500	Elk River at Sutton, W. Va.				5^3	1918,  iato-72—	1918

Ohio River main stem

870	03201500	Ohio River at Point Pleasant, W. Va.	52,760	1896-1972  19U1-72	1913  19l(3  191(8
871	03202020	Ohio River at Point Pleasant, W. Va. (Auxilary gage)	(!)	191(1-72	
872	03205220		(1)	1935-72	—
873	03206000	Ohio River at Huntington, W. Va.		55,900	1935-72	1937

2/9.20	—	June	23	6.11	1,810	3
9.1!	12,200					3
7.0C	230	June	21	1.25	65	<2
5.26	1*28	July	1	5.87	266	2
l.lC	20	June	21	3.95	13	<2
17.5	11-500	July	5	13.35	21,800	•1
11.52	8,820	July	5	12.93	7,020	1
I6.9C	12,900	June	21	17.1	13,500	35
---	—	June	21	—	1,100	>100
13.»(5	6,710	June	21	18.6	11,000	>100
J-77	6,100	June	21	9.11	7,170	60
22.0	77,500	June	21	15.21	38,000	3
10.7c	120	-—		7.00	115	<2
21.8"	60,800	June	22	17-7S	39,300	3
22.6C	56,100					
1.6c	i,olo	June	17	1.19	971	8
18.1,'	22,000	June	23	9.21	6,770	<2
27.3!	12,500	June	23	15.19	12,900	3
	,10,700  2121,800	June  June	ti	,/ 18.73 4,658.80	21,700  5/211,300	2
19.3c	17,800	June	2h	18.I9	15,700	"(1)
6.5;	169	July	5	5.81	119	<2
13.3:	21,100	June	23	12.25	17,100	8
V950llC	2(11^300	June	21*	1/911.81	5/99,910-	
l5.2	19,000	June	21*	20.15	8,000	(1)

66.81	(1)	June 26	10.95	385,000	(1)
—	522,000				
55.00					
—	—	June 27	11.03	(1)		-
—	—	June 27	15.26	(1)	...
69.15	651,000	Jung 27	13.0^	375,000	(1)

See footnotes at end of table﻿APPENDIX A

387

TABLE Al.—Summary of flood stages and discharges—Continued

				Maximum previously known				Maximum June—July 1972			
Re-  port  No.	nent  station  No.	Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Streams tributary to Lake Erie

874	04213320	
875	04213490	South Branch Cattaraugus Creek near Otto, N. Y.-	—
876	04213492	South Branch Cattaraugus Creek near Cattaraugus, N.Y.
877	04213500	
878	04214200	Eighteenmile Creek at North Boston, N. Y.			
879	04214400	Buffalo Creek near Wales Hollow, N. Y.	
880	04214410	
881	04214500	
882	04215000	
883	04215500	Cazenovla Creek at Ebenezer, N. Y.			
Streams		
884	04220360	Springmills Creek at Springmills, N. Y.—			
885	0422037A	Cryder Creek at Genesee, Pa.					—	
886	04220384	
887	04220412	
888	04220418	Fullmer Valley Creek tributary near Andover, N. Y.	
889	04220420	Fullmer Valley Creek near Hgllspart, N. Y.	
890	04220422	Chenunda Creek tributary near Stannards, N. Y.		
891	04220431	Cbenunda Creek at Stannards, II. Y.		—-—
892	04220450	
893	04220455	Quig Hollow Brook near Andover, N. Y.-		
894	04220460	East Valley Creek tributary near Andover, N. Y.-	
895	04220465	Railroad Brook near Alfred, N. Y.-	—	
896	04220472	Indian Creek near Andover, N. Y.						—
897	04220478	Elm Valley Creek near Elm Valley, N. Y.		—
898	04220492	Trapping Brook near Wellsvllie, N. Y.		—
899	04220500	Dyke Creek at Wellsville, N. Y.	
900	04221500	Genesee River at Scio, N. Y.		—-—
901	04221510	Vandermark Creek near Scio, N. Y.	
902	04221518	Snowball Hollow Creek near Scio, N. Y.	
903	04221554	North Branch Riillips Creek at Witney, N.Y. 		
904	04221555	Riillips Creek at Witney, N. Y.	
905	04221561	Feathers Creek near Belmont, N. Y.			—
906	04221600	Van Campen Creek at Friendship, N. Y.	
907	04221640	Black Creek near Birdsall, N. Y.—		—		
908	04221700	Angelica Creek near Angelica, N. Y.	—		—	
909	04221710	Baker Creek near Angelica, N. Y.	
910	04221720	Angelica Creek at Transit Bridge, N. Y.	
911	04222510	Sixtown Creek at Higgins, N. Y.	
912	04222600	Wiscoy Creek at Bliss, N. Y.	
913	04223000	Genesee River at Portageville, N. Y.	
914	04224000	Mount Morris Lake near Mount Morris, N. Y.-		
915	04224550	Ewart Creek at Swain, N. Y.———				
916	04224650	Canaseraga Creek at Canaseraga, N. Y.	
917	04224700	Sugar Creek near Ossian, N. Y.	—
918	04224800	Stony Brook at South Dansville, N. Y.			
919	04224810	Sponable Creek near South Dansville, N. Y.		—
920	04224900	Mill Creek at ftrtchinville, N. Y.	—
921	04224965	Little Mill Creek near Dansville, N. Y.—			
922	04224970	Little Mill Creek tributary near Dansville, N. Y.	
923	04225000	Canaseraga Creek near Dansville, N. Y.	
924	04227500	Genesee River near Mount Morris, N. Y.			
925	04227980	Conesus Lake near Lakeville, N. Y.	—
926	54228500	Genesee River at Avon, N. Y.	—
927	54228845	
928	54228900	3pringwater Creek at Springwater, N. Y.	
929	54229500	Honeoye Creek at Honeoye Falls, N. Y.	
930	54230380	Datka Creek at Warsaw, N. Y.	
931	54230500	Oatka Creek at Garbutt, N. Y.	
932	54231000	Black Creek at Churchville, N. Y.-		—
933	54232000	Genesse River at Rochester, N. Y.	
934	54232050	Allen Creek near Rochester, N. Y.		
See	footnotes	at end of table.

36.0 25.6 70

1*32

37.2

80.1

14.0

144

94.9

134

1963-72	1967	7.23	2,780	June 23 June 23	7.34	7,730  2,910	>100  5
1940-72	1956	14.14	34,600	(1)  June 23	12.17	4,000  25,300	<2
1964-68,  1970-72	1967	12.50	5,790	June 23	11.05	4,670	10
1964-68,  1970-72	1967	11.61	9,260	June 23	u.37	8,830	19
1964-72	1967	6.66	1,680	June 23	5.81	1,160  12,000	
1939-72	1942	2/H.90	—	June 23	9.09		14
1939-68,	1955	9.43	13,000				
	1959	10.09	8,750	June 23	10.09	8,80c	35
1971-72	i960	2/12.58	—				
1941-72	1955	15.82	13,500	June 23	13.53	12,30c	19

Streams tributary to Xaloa Ontario

5.01

50.0

4.07

179

.72

11.8

.04

30.6

1.64

4.24

1-59

1.05

1.07

4.18

3.19 71.4

308

22.0

3.47*

7.16

24.1 3-69

45.8

19.4

61.3

22.4

86.5

17.8

21.8

981

1.075

3.90

58.2 9.83

2.23

.69

5.00

7.54

1.42

153

1,417

69.7

1,667

41.1

10.1

195

41.9

204

123

2,457

30.1

1964-69,

1971-72

1964-72

1964-68

1964-67,

1971-72

1956-60,

1964-67,

1969

1917-72

1964-68

1942

1964-68

1962-65,

1967-72

1909-72

1952-72

1964-65

1964-68

1964-72

1964-69

1964-67

1964-72

1911-12,

1916-68,

1971-72

1904-	05, 1909-13, 1916-72

1964-	72 1956-72

1965-	72 1965-68, 1970-72 1946-70 1964-72

1946-72

1946-72

1835-1972

1905-	72

1960-72

—					June 22	
—	—				June 22		
—	—	—	June 22		
—	—	—	June 22		
	—	—	June 22		
—	—-	—	June 22		
—	—	—	June 21		
—	---	—	June 22	—
1971	7.47	(1)	June 22	8.5
1964,	4.15	254	June 23	5.11
1971				
1966	3.38	920	June 22	3.04
1971	2.05	115	June 22	4.75
—	—	—	June 23		
—	—	—	June 23		
—	y —	—	June 23	
i960	1,508.28	5,230	June 23	—
1950	11.22	23,300	June 23	14.12
—	—	—	June 23	V —
—	—	—	June 21	1,552.29
—	—	—	June 22	4/ —
—	—	—	June 22	
—	y —	—	June 23	
1967	1,487.78	13,400	June 22	1,485.60
—	—	—	June 23	
1942	—	1,400	June 22	
—	—	—	June 22	
1967	—	9,560	June 22	
—	—	—	June 22	
1964	3.38	—	June 23	4.06
1967	3.21	1,050		
1967	22.94	47,300	June 23	,, 35.25 V755.46
i960	4/719.40	s/216,000	June 25	
1964	3.80	720	June 22	3.75
1967	—	5,480	June 22	
1964	6.45	—	June 23	6.85
1967	5.92	948		
1968	2.64	(l)	June 22	^.4fi
1967	2.04	(1)	June 22	3.03  3.01
1964	3.79	—	June 23	
1967	2.58	626		
—	—	—	June 22		
—	—	—	June 22	
1940	1/9.93	9,110	June 23	14.85
1916	25.44	55,100	June 24	24.50
1971  1956	20.53  37.20	15,600	June 24 June 25	22.50  40.67
1971	4.72	—	June 23	
1971	5.37	184	June 23	7.29
1950	4/616.40	4,630	June 23	
1967	7.28	1,760	June 23	9.75  6.89
i960	8.64	7,050	June 24	
i960	9.44	4,880	June 25	
1865	—	54,000	June 25	15.89
1916	1/15.3	48,300		
i960	6.06	5,040	June 23	4.82

595

6,6lC

96:

20,20C

17:

3,20C

2'

9,20C

(1)

9,208

70C

67C

92!

1,84C

63c

12,00c

4i,ooc

■8,67c

58c

1,73c

5,91c

933

9,40c

1,86c

6,12c

3,05c

8,40C

2,46C

1,85c

, 9O,00C 5/322,60C 70C 12, 40C 1,38C

49C

121

1,35C

835

11:

9,6oc

17,8oc

16,50c

1,18c

4,800

4,oic

3,840

60c

29,60c

1,280

>100

>100

ft

>100

(1)

>100

15

>100

>100

>100

>100

10

>100

(1)

>100

ft

(1)

(1)

ft

(1)

(1)

25

40

45

5

<2

(1)﻿388

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE A1 .—Summary of flood stages and discharges—Continued

	Perma-  nent  station  No.			Maximum previously known				Maximum June—July 1972			
Re-  port  No.		Stream and place of determination	age area (sq mi)	Period	Year	Gage  height  (ft)	Dis-  charge  (cfs)	Date	Gage  height  (ft)	Dis-  charge  (cfs)	Recur-  rence  interval  (years)

Streams tributary to Lake Ontario—Continued

935	01232100
936	0I232192
937	0I232198
93»	0I232I00
939	0I232I06
9I0	0I232I50
911	0I232I5A
9I2	0I232I68
9*»3	0I232I82
9ll	0I232I90
915	0I232630
946	OI232902
917	0I233000
918	0I233250
9*9	0I233255
950	OI233257
951	0I233310
952	0I23331I
953	01233317
951	0I233500
955	01233676
956	0I23I000
95 T	OI23IO18
958	0I23I200
959	01231250
960	0I23IIOO
961	OI23II28
962	0I23I5OO
963  96k	0I235000  01235150
965	0I235250
966	OI235276
967	01235300
968	01235396
969	OI235500
970	0I236000
971	0I237500
972	0I238500
973	0I239000
974	04240010
975	01210100
976	01210105
977	01210180
978	01210200
979	01210300
980	Ol2lpl95
981	01212500
982	01213500
983	01215000
981	01215200
985	01215236
986	OI2I58IO
987	01216000
988	01216500
989	OI2I9OOO

Sterling Creek at Sterling, N. Y.-------------

Catherine Creek tributary No. 4 near Montour Falls, N. Y.

Catherine Creek near Montour, N. Y.-----------

Seneca Lake at Watkins Glen, N. Y.------------

Hector Falls Creek at Burdett, N. Y.-------------

Keuka Lake at Hanmondsport, N. Y.-------------

Keuka Lake tributary No. 13 near Hammondsport, N. Keuka Lake tributary No. 12 near Pulteney, N. Y.-

Keuka Lake outlet at Dresden, N. Y.---------------

Kashong Creek near BeIlona, N. Y.-----------------

Kendig Creek near Mac Dougall, N. Y.--------------

West Branch Cayuga Inlet at Nevfield, N. Y.-------

Cayuga Inlet near Ithaca, N. Y.-------------------

Buttermilk Creek near Ithaca, N. Y.---------------

Cayuga Inlet at Ithaca, N. Y.---------------------

Coy Glen Creek at Ithaca, N. Y.-------------------

Sixmile Creek near Ithaca, N. Y.------------------

Sixmile Creek tributary near Ithaca, N. Y.--------

Sixmile Creek at Fotlers Falls near Ithaca, N. Y. Cayuga Lake at Ithaca, N. Y.----------------------

Virgil Creek at Dryden, N. Y.----—----------------

Fall Creek near Ithaca, N. Y.-----------------—

Salmon Creek at Ludlowville, N. Y.----------------

Mud Creek at East Victor, N. Y.—-----------------—

Ganargua Creek at Macedon, N. Y.------------—----

West River near Middlesex, N. Y.-----------------

Reservoir Creek at Naples, N. Y.—----------------

Canandaigua lake at Canandaigua, N. Y.-------------

Canandaigua Outlet at Chapin, N. Y.--------------

Flint Creek at Potter, N. Y.-----------------------

Flint Creek at Hielps, N. Y.---------------------

Black Brook at Tyre, N. Y.-----------------------

Owasco Inlet at Moravia, N. Y.-------------------

Owasco Lake near Auburn, N. Y.------------------—

Owasco Outlet near Auburn, N.Y.————————

Skaneateles Lake at Skaneateles, N. Y.-----------

Seneca River at Baldwinsville, N. Y.-------------

Onondaga Reservoir near Nedrov, N. Y.------------

Onondaga Creek at Darwin, N. Y.------------------

Onondaga Creek at Spencer Street, Syracuse, N. Y.

Harbor Brook at Syracuse, N. Y.—-----------------

Harbor Brook at Hiawatha Boulevard, Syracuse, N.

Ninemile Creek near Marietta, N. Y.--------—-----

Ninemile Creek at Camillus, N. Y.----------------

Ninemile Creek at Lakeland, N. Y.----------------—

Onondago Lake at Liverpool, N. Y.----------------

East Branch Fish Creek at Taberg, N. Y.----------

Oneida Creek at Oneida, N. Y.----------------------

Limestone Creek at Fayetteville, N. Y.—------——

Butternut Creek near Jamesville, N. Y.-----------

Meadow Brook at Hurlburt Road, Syracuse, N. Y.—

Scriba Creek near Constantia, N. Y.--------------

Oneida Lake at Brewerton, N. Y.--------------------

Oneida River at Caughdenoy, N. Y.------------------

Oswego River at Lock 7, Oswego, N. Y.------------

11.1	1958-72	i960
1.00	—	—
38.2					
701	1957-72	196I
11.8	1971-72	1971
	1935	1935
182	1961-72	1961
.23	—	—
• 85	—	—
207	1966-72	1971
30.7	1965-70	1967
13.8	1965-72	1968  1971
8.05	—	—
35-2	1937-72	19I2
11-3	—	—
86.7	1971-72	1971
3-55	—	—
12.0	1967-69,  1971-72	1967
■ 69	—	—
15-5	1935	1935
1,561	1906-25,  1957-72	1916
20.6	1966-70	1969
126	1926-72	1935  1971
81.7	1965-68,  1970-72	1966
	1935	1935
64.2	1959-68	1963
101	1965-69	1966
29.3	1965-72	1969
5.76	—	—
184	1929-72	1956
195	19I0-72	1912
31.0	196I-72	1961
102	1960-72	i960  1963
19.0	1966-72	1970
106	1961-68	1961  1961
205	1912-72	1936
206	1913-72	1936
72.7	1891-1972	1917
3,136	1950-72	i960
67.7	1953-72	I960
88.5	1952-72	1960  1961
109	1971-72	1971
9.63	1960-72	1969
11.3	1971-72	1971
15.5	1965-72	1971
81.3	1959-72	I960
115	1971-72	1971
285	1971-72	1971
188	1921-72	I9I5
113	1950-72	1950  1959
85-5	1910-72	1950  1961
32.2	1959-72	1961  1972
2.90	1971-72	1972
38.1	1966-72	1971
1,382	1952-72	i960
1,382	1903-12,  1948-72	1903
5,098	1901-06,	1936
	1931-72	19I0

5.13	1,190	June	22	3-63
—	—	June	22	—
				June	22		
U/8.56	—	June	25	10.17
2.73	(1)	June	23	5.10
—	1,600			
5-79	—	June	24	9.35
—	—	June	23	—
—	—	June	23	—
5-17	2,320	June	22	8.37
3.I9	(1)	June	23	3-19
6.14	713	June	23	1-93
2/6.23				
	—	June	23	—
7.58	1,110	June	23	8.10
—				22		
2/10.71	(1)	June	23	14.6
—	—	June	22	—
5.59	2,610	June	23	9.13
—			June	22		
—	1,330	June	23	—
8.4	—	June	26	9.76
5.09	(1)	June	23	3.90
. 9-52	15,500	June	23	5-38
2/11.16	—			
7.23	1,910	June	23	10.62
—	13,700			
6.6 5	1,370	June	22	7.85
5-91	1,520	June	22	6.75
5-77	1,530	June	23	6.82
—	—	June	22		
U/9-13	—	June	24	10.94
1161	1,100	June	24	5.62
6.87	920	June	23	10.15
5.83	2,910	June	24	5.75
2/6.20	—			
6.68	(1)	June	23	3.61
1/723-81	11,600	June	23	1/727-81
/S/72I.I0  5/716.91			June	25	1/716.88
1.88	2,090	June	23	6.28
63-75				June	25	65.20
9-21	7/17,200	June	28	—
I/I85.9		June	30	9.21
	5/5,960	June	24	4/480.43
5.06	2,130	June	23	6.12
5-11					
6.71	1,610	June	23	6/8.09
7.13	371	June	23	7.15
6.17	lio	June	21	6.55
5.36	313	June	22	8.65
8.25	2,760	June	23	8.73
6/7.12	1,600	June	23	8.58
1/367.11	—	June	30	1/369.21
10.90	13,600	June	22	11.71
13-78	7,110	June	22	u.61
2/l't-30	—			
7.78	7,010	June	23	7.56
7.95	—			
6.29	1,260	June	21	7.15
7.51	—			
3.61	179	June	21	3-35
6.I5	870	June	22	7.12
IO.69	—	June	26	11.84
—	2/13,800	June	25	—
—	37,500	June	29	11.87
13-16	—			

< Less than value shown.

> Greater than value shown.

1	Not determined.

2	Hurricane wave.

3	Result of ice jam.

U Elevation above mean sea level, in feet. 5 Contents, in acre feet.

6	Affected by backwater; see station description.

7	Site and datum then in use.

8	Contents, in millions of gallons.

9	Maximum dally discharge, In cubic feet per second.

10	Site and datum used prior to 1950.

11	Maximum daily gage height, in feet.

160	<2
296	(1)
3,150	18
- - -	—
1,500	4o
				
119	(!)
255	(l)
1,000	(1)
610	<2
117	<2
1,180	(1)
1,800	>100
1,060	(1)
11,800	>100
516	(1)
5,360	>100
187	u)
1,130	(1)
—	—
1,380	4
1,600	5
1,160	6
1,800	15
1,950	5
2,790	30
1,600	(1)
---	—
1,710	>100
5,010	(1)
2,820	21
530	<2
(1)	—
—		
3,250	>100
		
1/17,100	25
5/3,670		
3,200	>100
3,100	(1)
158	m
171	1
1,030	(i)
1,930  2,290	(1)
---	—
11,500	>100
9,260	>100
3,800	1
1,120	6
156	(1)
1,200	<2
	___
2/10,100	>100
29,500	24﻿APPENDIX A

389

TABLE A2 .—Flood-crest data, June 19, 1972, for streams in Westchester County, N.Y. , and southeast Connecticut

[Stationing is that used by U.S. Army Corps of Engineers in flood-plain information studies in the area]

Stream and location	Station-  ing  (ft)	Eleva-  tion  (ft)		Stream and location	Station-  ing  (ft)	Eleva-  tion  («)
East Branch Byram River:				Hutchinson River:		
Riversville, Conn., U. S. Geological	23,600	151*-1*		New Rochelle, N.Y., 80 ft upstream from	2,900	211.7
Survey gage.				Hutchinson Boulevard.		
Glenville, Conn., bO ft upstream from	8,800	35.5		New Rochelle, N.Y., 70 ft upstream from	350	197.6
Comly Avenue bridge.				Old Wilmot Road.		
Glenville, Conn., 30 ft downstream from	8,700	31+.0		Eastchester, N.Y., at New Wilmot Road--		0	191.5
Comly Avenue bridge.				Pelham, N.Y., upstream side of Lincoln	6,300	27.0
Port Chester, N.Y., just downstream from	2,300	10.0		Avenue bridge.		
U.S. Highway 1 bridge.				Pelham, N.Y., U.S. Geological Survey gage,	1*,000	17.1*
Blind Brook:				100 ft downstream from Pelham Lake.		
Rye, N.Y., downstream from Purchase Street	1^,930	35.0		Pelham, N.Y., 20 ft upstream from Sanford	500	6.0
bridge.				Avenue bridge.		
Rye, N.Y., 500 ft upstream from Highland	12,700	29.2		Saw Mill River:		
Avenue.				Eastview, N.Y., upstream side of River	12,500	196.1
Rye, N.Y., 65 ft downstream from Highland	12,100	29.6		Road bridge.		
Avenue.				Eastview, N.Y., downstream side of River	12,500	19*+. 5
Rye, N.Y., U.S. Geological Survey gage		11,000	25.5		Road bridge.		
Rye, N.Y., 60 ft upstream from Central	8,800	18.3		Elmsford, N.Y., 55 ft downstream from	1*,200	177.0
Avenue bridge.				Mine Brook.		
Rye, N.Y., 100 ft downstream from Central	8,600	16.8		Elmsford, N.Y-, Warehouse Lane (A&P	3,600	176.1*
Avenue bridge.				access road).		
Mamaroneck River:				Elmsford, N.Y., at downstream side of	2,000	175-1
Mamaroneck, N.Y., 6 ft upstream from	10,700	37.8		Penn Central Railroad bridge.		
Winfield Avenue bridge.				Elmsford, N.Y., upstream side of Tarry-	- 50	171*. 2
Mamaroneck, N.Y., kO ft downstream from	10,600	35.9		town Road bridge.		
Winfield Avenue bridge.				Elmsford, N.Y., downstream side of Tarry-	- 100	172.8
Mamaroneck, N.Y., 300 ft downstream from	8,500	32.2		town Road bridge.		
foot of Warren Street.				Ardsley, N.Y., at N.Y.C. water-supply	2,1*00	131.0
Mamaroneck, N.Y., 75 ft upstream from	5,500	25-5		blowoff.		
North Barry Avenue.				Ardsley, N.Y., 300 ft upstream from Old	2,000	130.1*
Mamaroneck, N.Y., upstream side of	3,560	23.8		Ashford Avenue.		
Jefferson Avenue bridge.				Ardsley, N.Y., at downstream side of Elm	200	127.6
Mamaroneck, N.Y., U.S. Geological Survey	2,700	21.2		Street bridge.		
gage, 113 ft downstream from Halstead				Yonkers, N.Y., 200 ft downstream from	21,1*00	Hi*. 9
Avenue bridge.				Tonqpkins Avenue bridge.		
Sheldrake River:				Yonkers, N.Y., 60 ft downstream from	19,800	113-1*
Mamaroneck, N.Y., 10 ft upstream from	12,500	83.8		Hearst Avenue bridge.		
Weaver bridge.				Yonkers, N.Y., downstream side of Odell	16,700	112.7
Mamaroneck, N.Y., 25 ft upstream from	10,900	78.5		Avenue bridge.		
Bonnie Briar Road bridge.				Yonkers, N.Y., 125 ft downstream from	12,000	109.1*
Mamaroneck, N.Y., 100 ft upstream from	10,200	77.1		Nepperhan Avenue bridge.		
Rockland Avenue bridge.				Yonkers, N.Y., at downstream side of Silk	10,500	107.8
Mamaroneck, N.Y., at downstream side of	9,300	71.0		Place bridge.		
Forrest Avenue bridge.				Yonkers, N.Y., at downstream side of	9,500	106.2
Mamaroneck, N.Y., 1+0 ft upstream from	9,000	70.1		Worth Avenue bridge.		
Briarcliff Road.				Yonkers, N.Y., at downstream side of Lake	8,000	101*.!*
Mamaroneck, N.Y., at confluence with	8,300	59-7		Street bridge.		
East Branch.				Yonkers, N.Y., 300 ft downstream from	6,500	102.2
Mamaroneck, N.Y., l8 ft upstream from	6,960	31A		Axminster Avenue bridge.		
Sheldrake Dam.				Yonkers, N.Y., upstream side of Ashburton	5,600	102.8
Mamaroneck, N.Y., 5 ft downstream from	6,9^0	30.1		Avenue bridge.		
Sheldrake Dam.				Yonkers, N.Y., downstream side of	5,500	100.5
Mamaroneck, N.Y., downstream side of	5,200	26.8		Ashburton Avenue bridge.		
Rockland Avenue bridge.				Yonkers N.Y., U.S. Geological Survey gage	1+.500	96.5
Mamaroneck, N.Y., 50 ft downstream from	3,1*00	25.1*		at Old Croton Aqueduct.		
Fenimore Avenue bridge.				Yonkers, N.Y., 20 ft downstream from	3,800	88.6
Mamaroneck, N.Y., 100 ft downstream from	1,800	2U.9		Nepperhan Avenue bridge.		
Waverly Avenue bridge.				Yonkers, N.Y., 100 ft upstream from Elm	1,300	63.O
Mamaroneck, N.Y., 200 ft downstream from	500	21*.3		Street bridge.		
Mamaroneck Avenue bridge.						﻿390

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE A3.--Flood-crest elevations, June 1972

Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)		Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)
Delaware River basin					Susquehanna River basin			
Schuylkill River:					Susquehanna River:			
River View Park, Pa., 500 ft upstream	80.2	23	2142.8		Athens, Pa., downstream side of high-	286.1	2b	766.5
from Ashebrown Street.					way bridge.			
River View Park, Pa., 100 ft down-	79-^	23	2141.2		Mouth of Chemung River				283.5	—	760.14
stream from Laurel Run.					Tioga River (head of Chemung River):			
Reading, Pa., 125 ft upstream from	76.8	23	225.5		Lawrenceville, Pa., U.S. Highway 15	114.19	23	1,002.5
Schuylkill Ave. bridge.					bridge•			
Reading, Pa., 1+50 ft upstream from	75.8	23	219.2		Lawrenceville, Pa., intersection of	13.50	23	1,001A
Reading Railroad bridge.					James and Main Streets•			
Reading, Pa., 800 ft upstream from	7^-5	23	215.8		Lawrenceville, Pa., Presbyterian	13.12-	23	1,000.7
Lancaster Ave. bridge.					Church•			
Reading, Pa., abandoned sewage dis-	72.8	23	207.2		Lawrenceville, Pa., 150 ft downstream	13.07	23	999-5
posal plant.					from highway bridge.			
Titus Power Station		70.8	23	197.3		Lawrenceville, Pa., upstream from	12.87	23	999-2
Neversink, Pa., under U.S. Highway k22	69.0	23	187-5		Cowanesque River.			
bridge •					Lawrenceville, Pa., downstream from	n.65	23	997-1
Gibraltar, Pa		67.2	23	182.7		Cowanesque River.			
Birdsboro, Pa., under State Highway 82	63.I4	23	173.2		Lindley, N.Y., U.S. Geological Survey	10.65	23	990. 2
bridge .					gagetjust downstream from County			
Monocacy, Pa., 600 ft upstream from	61.3	23	166.7		Highway 120 bridge.			
Monocacy School.					Leland Harris barn (right bank)		10.10	23	989.1
Monocacy Station, Pa., 1+50 ft upstream	60.8	23	165.0		No. 891 Presho-Lindley Road		9.>45	23	986.5
from Monocacy Creek.					Penn-Central Railroad track		8.65	23	983.2
Douglassville, Pa., 250 ft downstream	58.1*	23	158.5			8.25	23	980.8
from Reading Railroad station.						7.65	23	977.8
Douglassville, Pa., 1.5 miles down-	56.8	23	156.3			7.00	23	976.9
stream.					Upstream side of Presho-Lindley Road	6.35	23	9714.9
Pottstown, Pa., 0.3 mile upstream from	5b .b	23	150.2		bridge.			
State Highway 100 bridge.					Downstream side of Presho-Lindley Road	6.30	23	972.6
Pottstown, Pa., U.S. Geological Survey	53-6	23	II47.8		bridge.			
gage, at Hanover Street bridge.					Country Club building		5.145	23	968.8
Pottstown, Pa., at sewage disposal	52. b	23	H43.8		Mouth of Canisteo River				1+.05	23	
plant.					Canisteo River:			
Sanatoga, Pa., at highway bridge		14-9-1	23	I3I4.I4		Addison, N.Y., old water tower				6.05	23	991.5
Linfield, Pa., upstream side of Parker	146.8	23	130.3		Addison, N.Y., American Legion	5.90	23	989.14
Ford bridge.					building•			
Linfield, Pa., 0.2 mile downstream	bb.5	23	1214.9					
from Vincent Dam.					Between Addison, N.Y., and mouth		5A5	23	985.2
Spring City, Pa., 150 ft upstream from	b2.2	23	117.6			14.00	23	978.14
Bridge Street •						2.90	23	971.9
Spring City, Pa., at sewage treatment	>41.3	23	115-3			1.95	23	968.5
plant •					Near junction of State Highway 17 and	•76	23	9614.9
Mingo, Pa., mouth of Mingo Creek		140.8	23	113A		U.S. Highway 15•			
Cromby, Pa., powerplant		39-6	23	111.3		Downstream side of old U.S. Highway 15	.55	23	962.7
Phoenixville, Pa., waterworks		39-1	23	110.8		bridge.			
Phoenixville, Pa., railroad overpass,	35.6	23	100.1		Tioga River—Continued			
State Highway 29.					Erwins, N.Y., Gang Mills Diner		3-145	23	961.9
Oaks, Pa., 700 ft upstream from rail-	32.8	23	914.2		Erwins, N•Y., Cemetery		3-15	23	958.6
road bridge.					Erwins, N.Y., U.S. Geological Survey	2.95	23	958.0
Perkiomen Junction, Pa., downstream	31.7	23	92. 5		gage,20 ft downstream from			
from Paulingo Road bridge.					Mulholland Road bridge.			
Valley Forge, Pa., mouth of* Valley	30.6	23	90.1		Gang Mills, N.Y., 150 ft north of Mo-	2.30	23	956.2
Creek.					bil gas station on State Highway 17.			
Port Kennedy, Pa., at State Highway	28.3	23	80.5		Gang Mills, N.Y., No. 61+0 Addison R»d—	1.90	23	955.0
363 bridge.					Gang Mills, N.Y., corner of Forrest	1.50	23	953.3
Barbados Island, Pa., at powerplant	2b. 5	23	75.3		and Hamilton Streets.			
gage.					Gang Mills, N.Y., Corning Gas utility	1.05	23	952.6
Norristown, Pa., downstream side	23.8	23	714.1		building.			
DeKalb Street bridge.					Gang Mills, N.Y., Corning 1st Bank	.65	23	952.0
Norristown, Pa., sewage.treatment	23.2	23	72.0		and Trust Co.			
plant at Ford Street.					Confluence of Tioga and Cohocton	0	—	■	
Ivy Rock, Pa., at left end of railroad	21.9	23	67.2		Rivers.			
bridge.					Cohocton River:			
Conshohocken, Pa., 275 ft downstream	20.1	23	62.3		Kanona, N.Y., 0.2 mile downstream	2b.2	23	1,1141.2
from Fayette Street bridge.					from U.S. Highway 15 bridge.			
Spring Mill, Pa., at Reading Railroad	18.8	23	58.6		Kanona, N.Y., 0.9 mile downstream	23.6	23	1,1140.14
station.					from U.S. Highway 15 bridge.			
Miquon, Pa., 260 ft downstream from	16.7	23	52.0			23.0	23	1,136.5
small creek.						22.8	23	1,128.2
Shawmont, Pa		16.0	23	51.0		Bath, N.Y., 0.05 mile upstream from	22.1	23	1,1214.3
Philadelphia, Pa., Flat Rock Road		iu.8	23	143.0		Veterans Administration bridge.			
Philadelphia, Pa., 1,000 ft downstream	lb.0	23	39.6			21.7	23	1,123.14
from Green Lane bridge.						20.5	23	1,102.6
Philadelphia, Pa., at mouth of	12.8	23	32.6			19-7	23	1,096.1
Wissahickon Creek.						18.14	23	1,091.9
Philadelphia, Pa., at U.S. Geological	8.5	23	20.14			18.1	23	1,089.5
Survey gage, 150 ft upstream from					0.6 mile downstream from Morgan bridge,	17.0	23	1,082.6
Fairmont Dam.					southeast of Bath, N.Y.			﻿APPENDIX A

391

TABLE A3.—Flood-crest elevations, June 1972— Continued

Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)
Susquehanna River basin—Continued			
Cohocton River—Continued			
0.8 mile downstream from Stocking	16.6	23	1,079-0
Creek.	16.2	23	1,075-7
	11+.6	23	1,051*.!*
0.3 mile downstream from Erie Rail-	ll+.O	23	1,050.1
road bridge, west of Savona, N.Y.			
	12.1+	23	1,039.8
	11.6	23	1,032.8
Campbell, N.Y., U.S. Geological	11.1	23	1,027.7
Survey gage 1.9 miles upstream from			
Michigan Creek.			
Campbell, N.Y		10.6	23	1,021*.6
Campbell, N.Y., upstream side of	9.1	23	1,012.5
State Highway 333 bridge.			
	8.8	23	1,010.8
	7-8	23	1,007.0
	7.1*	23	1,002.1*
0.1+ mile upstream from Curtis Highway	6.5	23	991*.0
bridge.			
0.3 mile downstream from Curtis	5.8	23	986.7
Highway bridge.			
0.3 mile upstream from Meads Creek—	2.6	23	956.9
U.S. Highway 15 overpass west of	1.6	23	951*. 0
Painted Post, N.Y.			
Painted Post, N.Y., 57^ West High	1.2	23	950.8
Street.			
Painted Post, N.Y., church on	• 50	23	950.5
Hamilton Street, south of High			
Street.			
Painted Rock, N.Y., corner of Stanton	.10	23	950.0
and Rand Streets.			
Chemung River:			
Corning, N.Y., intersection of West	1+1+.2	23	91*5.8
William and Poultney Streets.			
Corning, N.Y., corner of Fuller	1*3.8	23	91*3.9
Avenue and Onondaga Street.			
Corning, N.Y., Grace Church on Bridge	1*3.2	23	91*1.1*
Street.			
Corning, N.Y., No. 21+7 E. Poultney	1*2.5	23	939-3
Street.			
South Corning, N.Y., 35 ft upstream	1*3-8	23	91*1*.7
from State Highway 17 bridge.			
South Corning, N.Y., corner of Chest-	1*3.0	23	939.5
nut and Market Streets.			
South Corning, N.Y., No. 119 East	1*2.6	23	932.0
Market Street.			
South Corning, N.Y., corner of East	1*2.2	23	929.6
Market and Columbia Streets.			
South Corning, N.Y., at sewage	1*1.2	23	928.3
treatment plant.			
South Corning, N.Y., Corning Saw and	1+0.6	23	921* .5
Supply Co. on State Highway 225.			
Along Erie-Lackawanna Railroad	1*1.8	23	931*.2
(left bank).			
Gibson, N.Y., Main Street			1*1.2	23	928.5
Gibson, N.Y., 0.6 mile downstream		1*0.6	23	924.9
Along right bank		39-1*	23	920.8
Rex Robertson property (left bank)		38.0	23	912.0
East Corning, N.Y., corner of Sidney	37-0	23	908.5
and Steele Streets.			
East Corning, N.Y., upstream side of	36.0	23	901*.6
Corning Road bridge.			
East Corning, N.Y., fire station		35.1*	23	903.1*
Along State Highway 352		31*.8	23	901.9
Along State Highway 352		33-0	23	898.7
Along State Highway 352		31.8	23	891.8
Harris Hill Manor, N.Y		30.2	23	881*.1
Golden Glow, N.Y., 11*85 Golden Glow	29.8	23	882.2
Drive.			
Elmira, N.Y., Woodland Apartments	29.6	23	881.9
(left bank).			
Elmira, N.Y., No. 67 Durland Avenue	28.2	23	871*. 0
(left bank).			
Elmira, N.Y., No. 901 Water Street	27.1*	23	868.1
(left bank).			
Elmira, N.Y., No. 303 Homewood Avenue	27.2	23	868.8
(right bank).			
Elmira, N.Y., No. 63I+ Water Street	26.9	23	866.8
(left bank).			
Elmira, N.Y., No. 306 West Hudson	26.1*	23	862.7
Street (right bank).			
Elmira, N.Y., No. 360 Water Street	26.1*	23	861*.1
(left bank).			

Stream and location

£hemung River—Continued

Elmira, N.Y., Chemung Canal Trust Co., State Street (left bank).

Elmira, N.Y., 101 Henry Street (right bank).

Elmira, N.Y., corner of Orchard and East Church Streets (left bank).

Elmira, N.Y., mouth of Newton Creek (left bank).

Elmira, N.Y., No. 1+58 Maple Avenue (right bank).

Elmira, N.Y., corner ctf* Luce Street and Baylor Drive (right bank).

Elmira, N.Y., on State Highway 17 (left bank).

Elmira, N.Y., on State Highway 17 (left bank).

Elmira, N.Y., No. 1301 Maple Avenue (right bank)

At dead end road by Seeley Creek (right bank).

Mouth of Seeley Creek-----------------

Seeley Creek:

Chemung River—Continued

1 mile downstream from Seeley Creek (right bank).

Along State Highway 1+27 (right bank) —

Wellsburg, N.Y., Methodist Church-----

Along Erie-Lackawanna Railroad (right bank).

Venturia Inn (left bank)--------------

At State Highway 17 bridge (right bank).

Left bank---------------------------—

Texaco gas station (left bank)--------

Chemung, N.Y., U.S. Geological Survey gage,100 ft upstream from State Highway 1+27 bridge (right bank).

Susquehanna River—Continued

Athens, Pa., at railroad bridge over Wolcott Creek.

Mouth of Sugar Creek------------------

Towanda, Pa., U.S. Geological Survey gage at Bridge Street bridge.

Wysox, Pa., 0.1+ mile downstream from Wysox Creek.

Mouth of Wyalusing Creek--------------

Skinners Eddy, Pa---------------------

Myobeach, Pa--------------------------

Mehoopony Station, Pa., former bridge site.

Vosburg, Pa---------------------------

Tunkhannock, Pa., 83O ft upstream from State Highway 309 bridge.

Tuckhannock, Pa., downstream side of State Highway 309 bridge.

Falls, Pa., 0.2 mile downstream from State Highway 92 bridge.

Ransom, Pa., mouth of Gardner Creek— Cox ton Yards, 1+00 ft downstream from railroad bridge.

Erie-Lackawanna Railroad bridge-------

West Pittston, Pa., east of York Avenue.

West Pittston, Pa., 0.2 mile downstrean from Ft. Jenkins Bridge.

West Pittston, Pa., National Guard Armory.

Exeter, Pa., streamward end of Schooly Street.

Port Blanchard, Pa., 0.5 mile upstream from Wyoming Bridge.

Kingston, Pa., railroad embankment at Pierce Street.

Wilkes-Barre, Pa., U.S. Geological Survey gage, 800 ft downstream from North Street.

Miles’		
upstream	Day	Eleva-
from		tion
mouth		(ft)
26.-0	23	861.1
26.0	23	860.5
25.6	23	859.0
21*.8	23	856.2
21*.8	23	853.5
21*. 6	23	850.2
21+.5	23	852.1*
2I+.0	23	81*9.8
23.5	23	81*7.5
22.1	23	81*2.9
21.1*5	23	839A
7-1*5		976.2
6.1*5	—	952.7
1+.91		909.5
			901*.5
1+.15			886.1*
3.20			865.3
1.60			81+2.1+
0	—	839-1*
20.1*	23	836.1
19-8	23	831*. 3
18.6	23	831.6
17-6	23	828.9
16.1+	23	827-3
15-6	23	821.2
ll*.5 13-8 12.1	23  23  23	821.8  817.9 810.2
283.1*	21+	759-7
273-2  270.2	21+  2l+	731.6  727.8
265-5	21+	716.9
250.3 239-2 233-1* 229-2	2l+  21+  2l+  2l+	679-7  658.1*  61*7-1*  61*0.2
221.6  217*8	21+  2l+	621-5  613-1*
217.1*	2l+	613-“*
206.1*	2l*	587.5
200.7  196.9	21+  21+	575-1  566.5
195-8  195-5	2l+  21+	561*.9 561*. 2
195.O	21+	563-0
191*.5	21+	562.0
193-7  193-1	2l+  21+	561.3  559-8
187.8	21+	551-3
187.6	2h	553-0﻿392

HURRICANE AGNES RAINFALL AND FLOODS, JUNE^IULY 1972

TABLE A3. —Flood-crest elevations, June 1972-- Continued

Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)		Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)
Susquehanna River basin—Continued					West Branch Susquehanna River—Continued			
						36.6	23	525.9
Susquehanna River—Continued					Railroad bridge over Loyalsock Creek--	36.3	23	525.1
Kingston, Pa., railroad embankment	186.9	24	551.1		Railroad bridge over Carpenters Dry	29.7	24	509.4
at Northampton Street.					Run.			
Wilkes-Barre, Pa., upstream side of	186.2	24	550.9		Muncy, Pa., junction State Highways	27.7	24	501.5
railroad embankment.					405 and 147.			
Plymouth, Pa., 500 ft upstream from	183.9	24	548.6		Montgomery, Pa., 700 ft downstream	22.6	24	491.5
Gaylord Avenue bridge.					from highway bridge.			
Breslau, Pa., Wilkes-Barre Avenue	183.8	24	548.3		Allenwood, Pa., downstream side of	18.2	24	481.9
at First Street.					highway bridge.			
Plymouth, Pa., 3^5 ft downstream from	183.8	24	548.4		Watsontown, Pa., upstream side of	15.8	24	477.4
Gaylord Avenue bridge.					highway bridge.			
Avondale, Pa., base of Sickler Hill--	181.8	24	546.3		Milton, Pa., near east end of 5th	12.1	24	471.5
Nanticoke, Pa., at Nanticoke Creek		180.9	24	545.4		Street.			
Nanticoke, Pa., upstream side of	179-9	24	545.0		Milton, Pa., 275 ft upstream from	11.6	24	470.8
highway bridge.					Broadway Street.			
Hunlock Creek, Pa				176.3	24	537-3		Milton, Pa., 100 ft upstream from	11.0	24	468.3
Shickshinny, Pa., 350 ft upstream	170.5	24	526.2		Reading Railroad bridge.			
from highway bridge.					Lewisburg, Pa., U.S. Geological Survey	7.5	24	462.4
Shickshinny, Pa., 650 ft downstream	170.3	24	525.6		gage at downstream side of Market			
from highway bridge.					Street bridge.			
Beach Haven, Pa., 1 mile downstream,	161.7	24	506.0		Winfield, Pa., mouth of Winfield	3.6	24	458.2
at mouth of Salem Creek.					Creek.			
Nescopeck, Pa., 1,000 ft upstream	159.5	24	503.5		Northumberland, Pa., 200 ft downstream	.1	24	453-9
from railroad bridge over Nescopeck					from bridge on U.S. Highway 11.			
Creek.					Susquehanna River—Continued			
Mifflinville, Pa., downstream side of	155.0	24	493.2		Sunbury, Pa., downstream side of	122.0	24	448.8
highway bridge.					highway bridge.			
Bloomsburg, Pa., bridge on State	147.6	24	482.8		Mouth of Shamokin Creek		121.2	24	447.6
Highway 1+87.					Sunbury, Pa., U.S. Geological Survey	120.2	24	444.4
Bloomsburg, Pa., railroad station		146.8	24	481.5		gage at Shamokin Dam powerplant.			
Rupert, Pa., Reading Railroad bridge-	145.6	24	479.6		Selinsgrove Junction, Pa., 200 ft up-	117.8	24	440.2
Catawissa, Pa., upstream side of	144.3	24	477-6		stream from Pennsylvania Railroad			
highway bridge.					bridge.			
Boyd, Pa., 1.6 miles upstream from	137.0	24	463.8		Confluence of Penns Creek and Middle	115.9	24	435.0
Danville gage.					Creek.			
	135.4		463.6			114.1	24	
gage, 200 ft upstream from Mill					Penns Creek:			
Street bridge.					Glen Iron, Pa., 150 ft downstream	29.0	23	605.1
Wolverton, Pa., 0.8 mile downstream--	128.1	24	456.9		from bridge on State Highway 235.			
Packers Island, Pa., downstream side	124.2	24	453-5		Penns Creek, Pa., U.S. Geological	20.3	23	521.6
of railroad bridge.					Survey gage, 200 ft downstream from			
Mouth of West Branch Susquehanna	123.9	24			bridge on State Highway 104.			
River.					New Berlin, Pa., 100 ft upstream from	16.0	23	496.2
West Branch Susquehanna River:					highway bridge.			
Bower> Pa., U.S. Geological Survey	199.8	23	1,225.8		Mouth of Monongahela Creek		8.1	23	,454.6
gage at downstream side of highway					Mouth of Middle Creek		1.9	23	435.0
bridge.					Middle Creek:			
Curwensville, Pa., U.S. Geological	183.8	25	1,135.9		Middleburg, Pa., downstream side of	12.7	23	497.7
Survey gage, downstream side of					bridge on State Highway 104.			
highway bridge.					Kreamer, Pa., 250 ft upstream from	7-7	23	472.2
Karthaus, Pa., U.S. Geological Survey	132.4	23	849.2		bridge on U.S. Highway 522.			
gage,900 ft upstream from bridge on					Susquehanna River—Continued			
State Highway 879*					Mouth of Mahanoy Creek		112.2	24	428.4
Renovo, Pa., U.S. Geological Survey	97.6	23	660.8		Mahanoy Creek:			
gage, upstream side of Eighth Street					Gowen, Pa., 1.5 miles southwest on	22.3	23	607.7
bridge.					downstream side of bridge on State			
Mouth of Young Womans Creek		93.8	23	648.0		Highway 125.			
Hyner, Pa.* upstream side of State	90.8	23	633.8		Domsife, Pa., 125 ft upstream from	8.0	23	498.7
Highway 120 bridge.					bridge on State Highway 225.			
Glen Union, Pa., 0.7 mile upstream		84.8	23	608.8		Herndon, Pa., 1.5 mile northeast		1.2	23	432.5
Mouth of Tangascootack Creek		77-3	23	585.7		Susquehanna River—Continued			
Pennsylvania Railroad bridge		74.0	23	580.1		Dalmatia, Pa		106.7	24	418.9
Lock Haven, Pa., Lock Haven State	70.9	23	568.3			102.9		
College.					East Mahantango Creek:			
Lock Haven, Pa., U.S. Post Office on	70.2	23	566.8		Klingerstown, Pa., upstream side of	17.4	23	535.0
Main Street.					highway bridge.			
Lock Haven, Pa., 300 ft upstream from	69.3	23	565.9		Mouth of Pine Creek		16.8	23	543.9
U.S. Highway 220 bridge.					Pine Creek:			
Mouth of Bald Eagle Creek at down-	67.6	23	564.8		Sacramento, Pa., at highway bridge,	12.2	23	674.9
stream side of railroad bridge.					1 mile east.			
McElhattan, Pa., downstream side of	64.8	23	560.1		Sacramento, Pa., 450 ft upstream from	12.1	23	661.8
highway bridge.					highway bridge.			
Avis, Pa., junction State Highway 44	58.7	23	558.9		Klingerstown, Pa., upstream side of	.4	23	534.9
and old U.S. Highway 220.					highway bridge.			
Jersey Shore, Pa., downstream side	55.4	23	551.4		Klingerstown, Pa., 425 ft downstream	.3	23	534.9
of highway bridge (left channel).					from highway bridge.			
Mouth of Larrys Creek		53.2	23	542.3		East Mahantango Creek—Continued			
Linden, Pa., 500 ft downstream from	46.6	23	539-2		Pillow, Pa., 50 ft upstream from	9-35	23	482.6
Quineshakeny Run.					highway bridge.			
Duboistown, Pa., upstream side of	41.9	23	535.6		Pillow, Pa., 250 ft downstream from	9-3	23	480.7
Arch Street bridge.					highway bridge.			
Williamsport, Pa., U.S. Geological	39-3	23	529.7		Dalmatia, Pa., U.S. Geological Survey	2.2	23	427.1
Survey gage on upstream side of					gage, 3*2 miles south of Dalmatia			
Market Street bridge.					at highway bridge.			

See footnotes at end of table.﻿APPENDIX A

393

TABLE A3.—Flood-crest elevations, June 1972— Continued

Stream and location

Miles

upstream

from

mouth

Day

Eleva-

tion

(ft)

Stream and location

Miles

upstream

from

mouth

Day

Eleva-

tion

(ft)

Susquehanna River basin—Continued

Susquehanna River—Continued

Paxton, Pa., 1.1 miles downstream---

Millersburg, Pa., mouth of Wiconisco Creek.

Wiconisco Creek:

Williamstown, Pa., downstream side of highway bridge.

Lykens, Pa., east end of North Street.

Lykens, Pa., 100 ft upstream from Market Street.

Lykens, Pa., 516 North Street--------

Mouth of Rattling Creek-------------

Rattling Creek:

Downstream side of railroad embankment at railroad station.

Downstream side of railroad embankment.

Wiconisco Creek—Continued

Elizabethville, Pa., upstream side of highway bridge.

Susquehanna River—Continued

Halifax, Pa--------------------------

Clarks Ferry, Pa., 0.3 mile upstream from highway bridge.

Mouth of Juniata River---------------

Juniata River:

Huntingdon, Pa., U.S. Geological Survey gage, 170 ft downstream from Smithfield Bridge.

Mapleton Depot, Pa., U.S. Geological Survey gage,0.3 mile downstream from bridge on State Highway 655* Mount Union, Pa., downstream side of highway bridge.

Mouth of Aughwick Creek--------------

Ryde, Pa., upstream side of railroad bridge.

Lewistown, Pa., upstream side Penn-Central railroad bridge.

Lewistown, Pa., 500 ft downstream from Penn-Central railroad bridge. Lewistown, Pa., downstream side of railroad bridge.

Mifflin, Pa., upstream side of bridge on State Highway 35*

Port Royal, Pa., at bridge on State Highway 75.

Vandyke, Pa., 0A mile upstream------

Thompsontown Station, Pa., downstream from highway bridge. Ihompsontown Station, Pa., 700 ft upstream from highway bridge. Millerstown, Pa., mouth of Raccoon Creek.

Newport, Pa., U.S. Geological Survey gage, at downstream side of highway bridge.

Trimmers Rock, Pa., 0.35 mile downstream.

Power line crossing-----------------

Susquehanna River—Continued

Duncannon, Pa., railroad station----

Mouth of Sherman Creek---------------

Sherman Creek:

Landisburg, Pa., 300 ft upstream from bridge on State Highway 233. Bridgeport, Pa., upstream side of bridge on State Highway 'Jb• Bridgeport, Pa., 1.2 miles southeast-— Falling Spring, Pa., mouth of Perry Furnace Run.

Dromgold Corners, Pa., upstream side of highway bridge.

Shermans Dale, Pa., U.S. Geological Survey gage, on downstream side of bridge on State Highway 3*+* Dellville, Pa., upstream side of covered bridge.

Downstream side of truss bridge-----

Upstream side of old U.S. Highways 11, 15 bridge.

100.6  96.5  32.2  27.95  27.85  27.7  26.9  .85	21.  21.  23  23  23  23	1.01.5  389.9  700.0  682.3  680.1.  673.9
	23	699.8
.55	23	683.8
15 A	23	526.0
91.1	21+	376.6
85.0	21+	365.8
81.-3	21+	
9k.2	23	619.7
85.0	23	590.1.
82.3	23	571-8
77-7	23	551.6
67-*+	23	520.2
1+9.1+	23	1+91-5
U9.3	23	1+90.2
1.6.8	23	186.9
31.-6	23	1.1.8-3
31-7	23	V.2.3
26.5	23	1+21+ .2
22.9	23	1+23.2
22.8	23	1+22.1+
17.2	23	109.8
IS. 3	23	397.9
10.75	23	396.0
•7	23	366.1+
83*	21+	361.3
83.0	21+	
26.0	22	530.6
23.0	22	508.0
21.1.	22	196.5
16.8	23	168.6
15.6	23	157-6
13-5	23	H0.7
7-5	23	1+02.9
3-1.	23	376.7
•15	23	318.1

Susquehanna River—Continued

Dauphin, Pa., 0.2 mile downstream from Stony Creek.

Rockville, Pa., upstream side of railroad bridge.

Lucknow, Pa., 100 ft downstream from State Highway 39 underpass.

Harrisburg, Pa., intersection McClay and Susquehanna Streets.

Mouth of Conodoguinet Creek----------

Conodoguinet Creek:

Plainfield, Pa., 0.55 mile downstream from Grieder bridge.

Meadowbrook Road, downstream side of bridge.

Spring Road (State Highway 3I+), upstream side of bridge.

Middlesex, Pa., upstream side of highway bridge.

Rich Valley Road, downstream side of bridge.

Hogestown, Pa., U.S. Geological Survey gage, 0.1+ mile downstream from Hogestown Run.

Lambs Gap Road, downstream side of highway bridge.

Sporting Hill Road, upstream side of highway bridge.

Orrs' Road, downstream side of highway bridge.

Upstream side of railroad bridge-----

Susquehanna River—Continued

Wormleysburg, Pa., 200 ft downstream from bridge on U.S. Highways 11 and

15.

Wormleysburg, Pa., 100 ft upstream from Locust Street.

Harrisburg, Pa., upstream side of Walnut Street bridge.

Harrisburg, Pa., City Island at Market Street.

Harrisburg, Pa., southeast corner of Front and Tuscarora Streets. Harrisburg, Pa., U.S. Geological Survey gage at Nagle Street.

Mouth of Paxton Creek-----------------

Paxton Creek:

Harrisburg, Pa., Progress Avenue bridge, upstream side.

Harrisburg, Pa., Progress Avenue bridge, downstream side.

Harrisburg, Pa., Crooked Hill and Paxton Church Roads.

Harrisburg, Pa., Wildwood Lake Dam, upstream side.

Harrisburg, Pa., Wildwood Lake Dam, downstream side.

Harrisburg, Pa., Harrisburg Community College campus.

Harrisburg, Pa., farm show-grounds garage.

Harrisburg, Pa., Maclay Street--------

Harrisburg, Pa., PP and L steamplant--Harrisburg, Pa., Paxton and Cameron Streets.

Harrisburg, Pa., Shaonis and Cameron Streets.

Harrisburg, Pa., mouth of Paxton Creek.

Susquehanna River—Continued

Harrisburg, Pa., south city boundary—

Mouth of Yellow Breeches Creek------

Yellow Breeches Creek:

Mount Holly Springs, Pa., 1.1 mile upstream from State Highway 3^*

Mouth of Mountain Creek-------------

Mountain Creek:

Mouth of Hunters Run----------------

1200 ft upstream from State Highway

3k-

Yellow Breeches Creek—Continued

Boiling Springs, Pa., municipal park, 200 ft upstream from highway bridge. Brandtsville, Pa., 250 ft upstream from State Highway 'Jb bridge.

76.9	21+	338.2
75-3	21+	332.1
71.8	21+	331.0
71.2	21+	326'. 6
71.1	21+	326.7
1+6.1+	22	155.1
11.8	22	1+1+1.5
31.0	22	in. 9
31.8	22	111.3
21.7	22	390.7
18.0	23	368.0
15A	23	360.9
11.7	23	318.2
8.5	23	310.0
0.15	21+	’326.7
70.3	21+	326.6
69.8	21+	325.9
69.5	21+	321.1
69*	21+	323.3
68.9	21+	323.1
68.8	21+	322.6
67.7	21+	320.0
8.39	22	358*
8.37	22	356.8
6.02	22	332.6
1.91	22	331.2
1.88		325.6
1+.05		321.0
3.1+0		322.6
3-09  1.81  1.01	21+  21+	322.2  322.2  321.9
.1+7	21+	320.8
0	21+	320.0
67.6  66.9	21+	318.6
		
31-7  32.6	22  22	526.7
		
1.85  2.85		622.5  587.8
28.7	22	175.6
21.3	22	139-3

See footnotes at end of table﻿394

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

TABLE A3 .--Flood-crest elevations, June 1972-- Continued

Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)		Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)
Susquehanna River basin—Continued								
						Codorus Creek—Continued			
					Indian Rock Dam, upstream		15.1	22	
Yellow Breeches Creek—Continued					York, Pa., U.S. Geological Survey	13.1	22	382.7
Rose Garden, Pa., 150 ft upstream	20.8	22	1*17.5		gage, 0.5 mile upstream from Rich-			
from highway bridge.					land Avenue bridge.			
Lisburn, Pa., upstream side of high-	13-1	22	370.2		York, Pa., upstream side George Street	10.1+	22	365.8
way bridge.					bridge.			
Lisburn, Pa., 0.1 mile downstream	13.0	22	369.4		Pleasureville, Pa., upstream side Emig	6.8	22	351*. 7
from highway bridge.					Mill Road bridge.			
Spanglers Mill Road, downstream side	5.1*	22	336.7		Pleasureville, Pa., 1,000 ft downstream	6.6	22	351.8
of railroad bridge.					from Emig Mill Road bridge.			
Camp Hill, Pa., U. S. Geological	3-1	22	325.8		Sherman Road, waste-water plant		5-0	22	31*7.1
Survey gage, 50 ft downstream from					Codorus Furnace, Pa., 300 ft down-	0.6	22	277.7
highway bridge.					stream from highway bridge.			
Susquehanna River—Continued					Susquehanna River—Continued			
New Cumberland, Pa., New Market	66.8	21+	316.8		Marietta, Pa., 0.25 mile upstream------	1*6.7	23	268.9
School.					Marietta, Pa., U.S. Geological Survey	1*1*. 3	23	265.1
Steelton, Pa., U.S. Highway 230 at	65.3	21+	3H+.2		gage, 1+20 ft upstream from Chickies			
railroad underpass.					Creek.			
Middletown, Pa., corner Union and Ann	60.0	21+	306.1*		Mouth of Chickies Creek		1*1*.2	21+	263.1
Streets.					Columbia, Pa., U.S. Highway 30 bridge—	1*2.2	21+	21+5.0
	59.9	21+				39-3  39-2		237.2  236.8
Swatara Creek:					Washington, Pa., mouth of Stamans Run—		21+	
Pine Grove, Pa., East Pottsville	56.7	22	516.9		Cresswell Station, Pa., mouth of	37-2	21+	23l*.8
Street, downstream side of bridge.					Wisslers Run.			
Pine Grove , Pa., 1,200 ft upstream	55.5	22	506.0		Safe Harbor Dam, tailrace		31.9	21+	196.3
from State Highway 61+5 bridge.					Mouth of Conestoga Creek		31.7	21+	195.9
Pine Grove, Pa., downstream side State	55.3	22	505.2		Conestoga Creek:			
Highway 61+5 bridge.						1*0.0		331.7
Suedberg, Pa., upstream side of high-	50.8	22	1*80.9		from State Highway 322 bridge.			
way bridge.						32.1*		301*.3
Green Point, Pa., mouth of Trout Run—	1+5 A	22	1*51*.6		highway bridge.			
Inwood, Pa., downstream side of high-	w*.3	22	1*1*1*.8		Bushong Road, downstream side of	29.7	23	296.6
way bridge.					bridge.			
Lickdale Pa., upstream side State	1*1.8	22	1*28.1		Hunsecker, Pa		27.1	23	288.1
Highway 3I+3 bridge.					Lancaster, Pa., U.S. Geological Survey	22.5	23	273.1*
West Jonestown, pa., 300 ft upstream	38.2	22	1+14.6		gage at Penn-Central Railroad bridge.			
from highway bridge.					Mill Creek, 300 ft upstream from mouth—	11+.1+	23	21*5.1
Mouth of Little Swatara Creek			37-5				Mill Creek, 200 ft downstream from	A.3	23	21+1+.1+
Little Swatara Creek:					mouth.			
Freeport Mills, Pa		5-1	22	1+25.1		Rockhill, Pa., downstream side of high-	3.6	23	210.6
Southeast corner of Jonestown, Pa		.75	22	1*11*. 8		way bridge.			
Swatara Creek—Continued					Downstream side of Safe Harbor bridge—	.05	23	195.9
Upstream side of State Highway 72	37-2	22	1+10.7		Susquehanna River—Continued			
bridge.					Mouth of Pequea Creek				29.5	21+	195.2
Abandoned powerplant				35.8	22	1+05.0		Pequea Creek:			
Harper Tavern, Pa., U.S. Geological	28.3	23	380.1*		Byerland Church, 50 ft upstream from	11.2	22	280.6
Survey gage,at downstream side of					wooden bridge.			
State Highway 93I+ bridge.					Martic Forge, Pa., downstream from	3-3	22	230.1
Mouth of Quittapahilla Creek		21.7	23	365.6		bridge at Martic Forge Hotel.			
Hummelstown, Pa., filter plant		10.2	23	31*1.3		Susquehanna River—Continued			
Pleasant View, Pa., 0.1 mile down-	8.8	23	336.6			21.2		
stream from railroad bridge.					Muddy Creek:			
Fiddlers Elbow, Pa., Logan residence—	7-1*	23	333-6		Muddy Creek Forks, Pa., 200 ft down-	16.8	22	373.8
Railroad bridge, 250 ft upstream		.6	23	307.8		stream from highway bridge.			
Susquehanna River—Continued					Bridgeton, Pa., 100 ft downstream from	11.9	22	316.1
South Royalton, Pa		59.5	21+	301*.9		highway bridge.			
Hill Island, Pa., on left bank across	59-0	21+	301.8		Castle Fin, Pa., 150 ft upstream from	1+.7	22	211.5
from Hill Island.					State Highway 7*+ bridge.			
Threemile Island, Pa., radio shack		58.1*	21+	301.1+		Castle Fin, Pa., U.S. Geological Survey	3A	22	196.0
Threemile Island, Pa		58.1	21+	300.3		gage, 200 ft upstream from Legis-			
Threemile Island, Pa., north side of	56.1+	21+	298.1*		lative Route 66062 bridge.			
railroad crossing.					Susquehanna River—Continued			
Falmouth, Pa., south of Falmouth		55.2	21+	287.6		Peach Bottom power facility				19.0	2l+	115.7
	55.05	21+	286.0			18.1*	21*	in*.7
								
Mouth of West Conewago Creek		55.0				Peach Bottom power facility, discharge	17-1+	2l+	113.8
West Conewago Creek:					control structure.			
Detters Mill, Pa., 300 ft upstream	26.6	22	377.1		Conowingo Power Plant, Pa		9.6	2l+	112.3
								
Alpine, Pa., upstream side of Kunkle's	18.7	22	361.8		Potomac River basin			
Mill bridge.								
Strinestown, Pa., upstream side State	6.8	22	307.3		Conococheague Creek:			
Highway 295 bridge.					Pennsylvania, upstream side of bridge f	27.1	23	1+1+3-6
Manchester, Pa., U.S. Geological	3.0	22	293-9		0.3 mile upstream from West Branch.			
Survey gage,500 ft upstream from					Downstream side of bridge,0.3 mile	27.1	23	1*1*2.5
bridge on State Highway l8l.					upstream from West Branch.			
Susquehanna River—Continued						26.8		
Mouth of Conoy Creek		51.6	21+	277.9		West Branch:			
Mouth of Codorus Creek		50.2	21+			Upstream side of highway bridge		0.2	23	1*1*3.5
Codorus Creek:					Downstream side of highway bridge		0.2	23	1*1*2.7
Spring Grove, Pa., U.S. Geological	21+.6	22	1*1*6.1*		Conococheague Creek—Continued			
Survey gage, at downstream side of					J.0. Elliot Farm, Pa., 0.3 mile up-	25.9	23	1*39.1*
county bridge.					stream from Diehls Run.			
Grayblll, Pa., 0.1 mile downstream	18.2	22	1*37-0		J.0. Elliot Farm, 0.1 mile downstream	25.5	23	1*38.5
from highway bridge.					from Diehls Run.			﻿APPENDIX A

395

TABLE A3.—Flood-crest elevations, June 1972-- Continued

	Miles		
Stream and location	upstream  from	Day	Eleva-  tion
	mouth		(ft)

Potomac River basin—Continued

Conococheague Creek—Continued			
Adam Martin Farm, Pa., 2.0 miles upstream from Pennsylvania-Maryland State line.	23.7	23	1*30.6
Upstream side of Maryland State Highway 58 bridge.	21.1	23	1*21.1*
Fairview, Mi., U.S. Geological Survey gage, 0.7 mile upstream from highway bridge.	19.1	23	1*16.3
Fairview, Md., upstream side of State Highway I49I4 bridge.	18.k	23	1*11* ,1
Fairview, Md., downstream side of State Highway 1+9^ bridge.	i8.u	23	U12.3
Upstream side of Broadfording Road		15.8	23	1*05.7
Downstream side of Broadfording Road—	15.8	23	1*01*.2
Spade Road, Md., 1.1 miles upstream from Rush Run.	13.9	23	399.5
Mount Tabor Road, Md., 0.5 mile downstream from Rush Run.	12-3	23	392.5
Upstream side of private drive, Maryland.	10.k	23	387.2
U.S. Highway kO bridge, Maryland		8.8	23	383.7
Off Walnut Point Road, Md., 2.5 miles upstream from Meadow Brook.	7-fc	23	380.2
Kemps Mill Road, Mi. (bridge washed out).  Off Kemps Mill Road, 0.8 mile downstream from Meadow Brook.	5.0	23	371*. 2
	k.l	23	372.7
Junction of Kemps Mill Road and Maryland State Highway 398.	3-b	23	370.8
Upstream side of Western Maryland Railway bridge.	0.9	23	366.8
Downstream side of Western Maryland Railway bridge.	0.9	23	365.7
Williamsport, Mi., State Highway 68 bridge.	0.5	23	365.0
C&0 canal aqueduct	  Monocacy River (river miles furnished by U.S. Army Corps of Engineers):	0.1	23	361*. 3
Bridgeport, Mi., U.S. Geological Survey gage, 60 ft downstream from State Highway 97 bridge.	52.6	22	361*.9
Keysville, Mi., Keysville Road bridge-	1*9.6	22	2256.6
Tom Creek at Sixes Road, Ml		1*8.1	22	351.9
Sixes Bridge, Mi		1*6.9	22	31*6.2
Momma Ford, Md		1*3-8	22	338.1*
Rocky Ridge, Mi., upstream side of Western Maryland Railway bridge.	1*2.2	22	335-9
Rocky Ridge, Md., downstream side of Western Maryland Railway bridge.	142.2	22	331*. 9
Rocky Ridge, Md., State Highway 77 bridge.	I4I.6	22	331*. 1*
LeGore Bridge, Mi., upstream side of bridge.	38.1*	22	323.8
Le Gore Bridge, Md., downstream side of bridge.	38.1*	22	321.9
Creagerstown, Md., upstream side of State Highway 550 bridge.	35.1*	22	316.6
Creagerstown, Md., downstream side of State Highway 550 bridge.	35-1*  31*. 0  31.9  29.9	22  22  22  23	311*.8  310.2 301.1*  293.2
			
			
Biggs Ford, Md., upstream side of bridge.	26.8	23	288.5
Biggs Ford, Mi., downstream side of bridge.	26.8	23	287.2
Penn-Central Railroad bridge, upstream side of bridge.	25.5	23	281*.8
Penn-Central Railroad bridge, downstream side of bridge.	25.5	23	283.1
Ceresville, Ml., State Highway 26 bridge.	23.9	23	280.1*

Stream and location	Miles  upstream  from  mouth	Day	Eleva-  tion  (ft)
Monocacy River—Continued			
Frederick, Md., filtration plant		21.5	23	276.1*
Frederick, Md., Gashouse Pike bridge---	20.3	23	273.6
Frederick, Md., U.S. Geological	16.9	23	267.8
Survey gage, 0.2 mile upstream from			
Jug bridge.			
Frederick, Mi., upstream side of Jug	16.7	23	265.7
bridge.			
Frederick, Md., downstream side of	16.7	23	261*. 3
Jug bridge.			
Reich Ford, Mi	-|	15.7	23	263.1
B&0 Railroad bridge		II4.O	23	260.0
Upstream side of Maryland State High-	13.8	23	259.0
way 355 bridge.			
Downstream side of Maryland State	13.8	23	257.1
Highway 355 bridge.			
Upstream side of Interstate Highway	13-2	23	256.0
70S bridge.			
Downstream side of Interstate Highway	13.2	23	253.2
70S bridge.			
Buckeystown, Md		10.2	23	250.9
Buckeystown Md., State Highway 80	9.6	23	21*8.5
bridge.			
Lilypons, Md., highway bridge		6.3	23	21*3-8
Greenfield Mills, Md., (bridge washed	k.O	23	239.3
out).			
Furnace Ford, Mi., upstream side of	1.9	23	23l*.8
State Highway 28 bridge.			
Furnace Ford, Md., downstream side of	1-9	23	231*.1
State Highway 28 bridge.			
C&0 Canal		0	23	231.7
Allegheny River basin			
Allegheny River:			
0.1 mile upstream from Pennsylvania-	260.2	23	1M0.1
New York State line.			
0.14- mile upstream from Dodge Creek		257-8	23	1,1*38.1
Olean, N.Y., at Mobile gas station		251+.2	23	1,1*30.8
Olean, N.Y., 0.8 mile downstream from	253-1	23	1,1*29.2
Haskell Creek.			
Olean,N.Y., 0.2 mile upstream from	251.6	23	1,1*27.5
Union Street bridge.			
Olean, N.Y., 0.3 mile downstream from	251.2	23	1,1*26.6
Union Street bridge.			
Olean, N.Y., Olean sewage plant		250.3	23	1,1*25.5
Olean, N.Y., Gargoyle Park.building		21*9-3	23	1,1*21.8
Olean, N.Y., across from St. Bona-	21*7-9	23	1,1420.0
venture College.			
Olean N.Y., 0.h- mile upstream from	21*6.8	23	1,1*17-9
Five Mile Creek.			
Olean, N.Y., 0.7 mile downstream from	21*5.8	23	1,1415-0
Five Mile Creek.			
Vandalia, N.Y., at peat moss plant		21*2.3	23	1,1410.0
Baltimore and Ohio Railroad bridge	238.3	23	1,399-1*
abutment.			
Erie Railroad bridge		237.2	23	1,398.1
2.1 miles upstream from Tunungwant	231**7	23	1,395-0
Creek.			
Along railroad track north of	232.8	23	1,390.6
Carrolton, N.Y.			
Salmonica, N.Y., 0.6 mile downstream	231.5	23	1,388.3
from State Highway 17 bridge.			
Salmonica, N.Y., upstream side of	230.0	23	1,383.8
State Highway 17 bridge.			
Salmonica, N.Y., downstream side	230.0	23	1,383-1
of State Highway 17 bridge.			
Salmonica, H.Y., U.S. Oeological	229-5	23	1,382.0
Survey gage, 23O ft upstream from			
Main Street bridge.			
Salmonica, N.Y., 0.1 mile upstream	229.14	23	1,380.8
from Main Street bridge.			
Salmonica, N.Y., 1.5 miles upstream	228.0	23	1,373-1*
from Main Street bridge.			

Backwater from Susquehanna River.

2About 2 to 2.5 ft higher than 1933 flood,﻿396

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972﻿APPENDIX A

397

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1 Construction not completed at time of flood﻿398

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

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					i		co !		i		i		VO	1	i/N i i			i	1 b- 0J		l		co i i i			rH H ON
a	ft		CQ			1  1		1  1		i  i		i  i			1  1		1 l 1 l		i  i	1 rH rH 1		i		i i i i i i			i—1 rH
0  0  2		2	0  bD		1  1		1  O l		i  0		i  i		o	1  1	o	1 l 1 1		i  i	1  i o o		i  i		i i  O O 1 1			o o o
CQ	a	P	, 2		1  1		O l  CO 1		i  i		I  i		o  o	1  1	o  o	1 1 i l		i  i	1 Q o 1 vo o		l		O O l l O O I l			o o o o o o
	2	H			1				i		i			1									•s I 1			
		2 0 0 0					CVI 1		i		i		b-	1	ft	l l		i	1 OJ LTN				CO O 1 1			O CVJ IA
					i		ft- 1		i		i		ft-	1	cc	i l		i	1 COO				O rH I 1			b-CO b-
	8	0  2	•H  ft		1  i  i		1  1  1		i  i  i		i  i  i		t—1	1  1  1	1—	l l l l i l		i  i  i	I 0J  1  1		1  i		rH t—1 1 1 1 1 1 1			CO CO 00
	"2																									
	ft	0	ft		i		O i		i		i		o	1	o	l i		i	I o o		1		O O 1 i			O O O
			2		1		O 1		i		i		c >	1	c:	1 l		i	I o o				O O I I			o o o
		—1	.M a m		1		ft- 1		i		I		o	1	o	l l		i	1 LTN O				O O 1 l			o o o
					1				i														•N *\ 1 I			
		30	0 O O		1		ON 1		i		i		o	1	LTN 1 1			i	1 0J oo				OO OJ 1 1			ft- Q O ON VO CO
					i				i		i		ft	1	CC	1 l		i	1 CO rH				CO LTN 1 1			
	0	2	•H		l		rH 1		i		i		CM	1	cv	l 1		i	l H ft				i—1 rH 1 1			LTN LTN LTN
	W		ft		1  i		1  1		i  l		i  i			1  1		l l l l		i  i	1  1		l		1 1 1 1			
			g —		o		I o		O		O		,	O	1	O 1		o	O 1 l		o		1 1 I o			1 1 1
	ft  0		rH 0 <H «P		o  o		i On 1 CO		CO  CO		rH  CO		1  1	CVI  CO	1	LTN 1 CO 1		8c	CO 1 1 O 1 1		a		I I 1 ft III b—			1 1 1 1 1 1
																										
			o		LTN  OJ		1 CO  i  i		OJ		i—1		1  1  1	b-	!	LTN 1 1 1		LTN  CM	vo 1 1 1 1 1 1		vo 1—1		1 1 1 VO 1 1 1 1 1 1			1 1 1 1 1 1 1 1 1
					o		• Q		o		o		1	o	1	O l		i—1	O i 1		o		1 1 1 O			1 1 1
		,			o		i O		<)		CO		l	o	1	O 1		O	O 1 1		o		1 1 1 O			1 1 1
					o		i i—1		o		CM		1	ON	1	ft 1		i—1	LTN 1 1		o		1 1 1 LfN			1 1 1
			tH <H		CO						b^			CO	1			ON	b- 1 1		•X  0J		1 1 1 O			1 1 1
2			•H ^		CO		1 OJ		1—1				1	CM	1	rH 1		ON	OJ 1 I	2	LTN		1 1 1 rH			1 1 1
•H																				ra					s	
O																				$					0	
t>															1				1 1	ft					+3	
2					o		I o		o		&			o	1	O O		O	O I 1		o		i i O O		0	1 1 1
	bD 0 ch 0 O ft 1 2 0 0 0				ON		I o		LTN				1	GO	1	rH LTN		LTN	b- 1 1	2	o		1 1 O CO			1 1 1
0  ft				2  >	1—1  VO		1 ft  1 »x		i—1  a?		CO  ON		1	CO  ft		O OJ VO ft		i—1  CO	ft 1 1 co i i	0  >  •H	CO  ft		1 1 0J O 1 1 rH CO		.3  g	1 1 1 1 1 1 1 1 1
	+3  CQ	0 2 0 0		xH  ft  S	OJ  LTN		1 VO  1  1		CM		rH		1  1	VO	1  1  1  1	LTN		CO  0J	VO 1 1 1 1 1 1 I 1	ft  a	CO  rH		1 1 H CO 1 1 1 1 1 1		a  2  0	1 1 1 1 1 1 1 1 1 1 1 1
				2																						
																				ft					•H	
	0 bD H 0+3 2 >2 +3			a	o  o		1  I o  1 OJ		o  CO		O  CO		J	o	1  1	s i		o  b-	1 1 O 1 1 ft 1 1	8)  2	o  &		1 1  1 i Q O  i i vo ft		ft  O	1 1 1 1 1 1 1 1 1
					CVI				VO		VO		1	CM	1	ft i		b-	ON 1 1	O			1 1 LTN OJ		•H	1 1 1
													1							2					ft	
	rH 8	0 S rH 0					1 OJ		t—		00		l	(Tn	1	CO 1		00	O I i	o	O		1 1 CO b-		o	1 1 1
					CO		1 OJ						l	VO	1	co i		VO	ON 1 1	S	b-		1 1 OJ ON			1 1 1
					LOx										1			OJ								
	p> 0		ft 0 CH 0																							
	<3	0 ft O v—'					1								1				1 1				1 1			1 1 1
							1  1  1  1		2				1  1  1  1			a			1 1 1 1 1 1 1 1 1 1 1 1				1 1 1 1 1 1 1 1 1 1 1 1			1 1 1 1 1 1 1 1 1 1 1 1
							1												1 1 1				1 1 1			1 1 1
							1		(1)				l			0 CD		2	1 1 1		2		1 1 1 >>			1 1 1
					2		1		2		P>		1			0 +3		0			0		1 1 * f?			
		O			>		1		ft		0		1	ft  0		O 0  +3		>  •H	aa i		0  2		1	1 ft 0  a ■. sa Ph 0 *x O ft ft -H  O *x 0 ■§)  2	-H rH 2 O O ft o			1 1 1 1 1 1
		-P			•H  ft		& +3		0  0		w			0  2		ft CQ 0		ft	i  •x *x 1		2					1 1 1 1 1 1
		o			}>>		0		2  O		-p		j	O	a	0 ft 2 0		a	!« i		>					1 1 1 1 1 1
					2		£ ft					•	l	bD		O 0		2	Pi *h *		•H					
					0		2 0 O 0		ft  o		0  ft  cd	a	a	2  •H	•x 2 bD ft O			P	cd bD		ft					1 • 0  1 0 >
							■s a		2					2	2	0. .		0	2 2				ft 2 0 >H CQ 0 o			• > P
									(1)		ft			O	•r	ft 15		2	2 0		0					ap*
							•H		2			pj		ft		O O		O	0 TJ 0		i—1		2 rH +3			
		.			1—1		ft 0		ft		2		2	0		O rH		o	ft 2 g		i—1		0 2 2 0			•X
		H			<q		+3				(1)	|	|	0	S	CC	2 i 1			h .a P				0 0 0			
		0					+3 0		2		f>		ft		+3	O 0		+3	0 > 2		>		2 ft 0 0 O O 2 ft			CQ O
					2		0 0		o		•H	2	2	+3	+3	>H										0 t>5 -P H 2 bD
					o		.0 2				ft	0	a	0	•r	+3			q -p a		+3					
		■P					Es o		2			>			w	0 +3		0	ft 0 S		2		+3 +3 ft			ft 2 2
		UJ			2		•H		•H		2	•H		(1)				ft  cd			%					o S -H
					•H	•	+3 EH		O		O	ft	+3	ft	+3	0			+3 2+3				O 2			•H 43
		2			O  >	a	03 2		s>  2	Pa.	•H  2	2	0	a	0	AJ 0)  a		ft	0^0		&		2 2 >0 0 0 2 >	a		Isl
		1 *			2		2 O		0		0	O	2		2			2	0 *H 2				> > 0 *H	a		
					0		0		0		i—1	•H	(1)	ft	a			0	ft ft 0		2	>	•H *H CQ £2			
					0		!> 0		(1)		O	2	>	(i)	!>			>	qj f>		O		ft ft 0			+3+3+3
					0	2	•H ft		ft	ft		g	•H	a)	•H	0 ft		•H	ft CQ *H			Uc	ft >»	•X		
					ft	N				+3	ft		ft	8	ft	0 0		ft	0 ft		0)		0 0 2	p		
						2		0			o	O				2 0	a		0 +3		ft			0		2 2 2
		ft			&	•H  «	& a	+3  0	-P  •H	o	2  0	ft	&	bD	p >?0 2  2 2 O			a a	2 0 >s 2 2 2		a	2  O	0 0 0ft ft ft 0 bD			i> > >
					0		0 +3	0	O	2	2	o	(1)	2	a	ft		2	0 «H 0			£ fi) S) 6 -2  0 2 2 ft		2		•H «H *H
					■ft	2	as	2  O	2	O  •H	ft	2  0	a	•H  2	g		ft  2		a sa		t			g		ft ft ft
							0 2	•H	O	2	+3	2	0	O	jj a	O rH	a	0 fij	0 ft 0		a	2	O O ft bD	•H		o o o
					i—1	2	rH O	H	•H	ft	0	ft H		ft	H t—	O rH		2 P	>> m H			O	2 2 0 2	ft		•H *H *H
									2				i—1	0	r—	2 0 O >H		O	Q :H. ft		£		.O .Q 0 O			ft ft ft
					<S		<$ ^		P		W			s	<3			O	ft w <				S (H			o o o
4-  J-																										
			•				OJ LTN		On		CO		t— co		ir\ b—vo			ON	0J ft b-		&		0J ON CO vo			CVJ CO CO
							OJ OJ		(VI		CM		ft	LTN	LTN LTN VO			vo	b- b- b-				rH ft 0J CVJ			
ft					b-		b- b—		b-		b-		b- b-		b- b- b-			b—	b- b- b-		b-		CO CO CO co			co co oo

2 -P o 0 I—I

W

cd

•H

2

>»

ft

*2

0

,2

ft

2

O﻿Table A8.--Comparative summary data of historical and June-July 1972 water and sediment discharge

400

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

			•H		00	o	CO	vo	CO	r^-		Mt	CO	CO	CO	CM	o	
			w e		r—1	vO	00	o	VO	o		<r	o		o	1—4		
			C U O d) c		CM	*"*							CM		<r	CO	ON	
		'co	H CL co															
		4-J																
		o			O	o	O	o	o	o		o	O	o	o	O	o	
	■u	H	CO		o	o	r-*	o	O	o		o	O	o		O	o	
	c		c		m	CM	<r	o	vO			00	O	rH	CO	O	o	
	E		H		n*	CO	<r	On	ON	CO		o	o'	CO		o	m	
	•H				r^.	co		vo		CO			00	m		CM	ON	
	T3												vO			in	CM	
	CU																	
	CO																	
		44			o	O	o	o	O	o		o	o	in	o	o	o	
		C0			m	CM	o	vO		r-^		vO	oo	00	m	CM	vo	
		CU  CL	00  e		00	•d-	as	o	co	CM		m	ON	in		O	CM	
'g						H	i—i	CM	1—4	tS					CO	rH	CO	
																		
			E															
CU					n-	r^	m	CM	r^.	CO		oo		<r	o	CM	00	
a			co  CM		on	rH	CM	00	oo	m		m	o	CM	n.	n»	00	
TO			O		n-	00	00	i—4	i^.			CO	<r	vO	00		ON	
§		i—I			cn	CO	r“l	CM	CM	CO		i—i	CM	CM	ON	1—4	m	
		C0																
		4J																
		o																
		E-	co		o	o	o	o	O	o		o	O	O	CM	o	o	
	Ll		>N		o	o	VO	o	o	o		o	O	O	m	o	o	
	CU		co		<r	CO	as	o	o	00		VO	O	O	i—i	o	VO	
	CO		1		r-'.	1—1	r—4	00	vO	ON		vO	in	<r		o'		
	&		CO		vO	CM			r—l	1—1		CO	VO				r-.	
			CM					CM					in			CM		
			O															
																		
					O	O	o	O	o	o		O	o	o	<r	o	o	
					o	O		O	o	o		in	o	o	o	o	o	
		44	CO  CM		00	00	CM	O	00	o		1—4	o	r^.	vO	o	co	
		<U	O		CM	m	m	CO	CO	ON		P-.	r'*	co		o"	00	
		CL			mt	co		o	CM	CM			00	co		CM	00	
								1—1					rH			o		
																l—1		
			'o ^  O d)		m	co	co	r-'	CO	CO		CM		vo	CM	o	-d-	
			•H C		CM	CM	CM	CM	CM	CM		O	CM	CM	CM	CO	CM	
			U 3 CU *-J		i	1  CM	1  CM	1  CM	1  CM	1  CM		l  CM	1	1	1  i—4		i  r—4	
			CL v-/		CM	CM	CM	CM	CM	CM		CM	CM	CM	CM	CM	CM	
			•H															
			co U E		r^.	CO	00	CM	00	<r		O	VO		Mf	VO	in	
	■u		C CU		on	oo	Mt		n-			vO	ON	in	00	o	m	
	c		o cl a			r-4				i—i	Z						i—4	
	(U		H co	Z							H							
	e  •r-l  XI			M  9	O	O	o	O	o	o	S3  PQ	O	O	o	m	o	o	z  1-4  CO
	CU		co	PQ	O	O	o	O	o	o		O	O	o	vo	o	o	<
'co	CO		c		vo	r-l	i—i	o	rH	vD	Crf	r^-	O	ON		o	CM	PQ
o			H	W	mt	i—l	mt	ON	,_r	<r	g	«d-	CM	CO		o	o'	Crf
c				6	co	m	CM	VO	m	m	M	■—i	CM	CM		m	m	
c								CM			Prf		CO			m		
CO				Crf														
<U  w			S								<					CM		crf  u
CO					<r	co	vO	r-»	r-4	o	<	CM	m	o	vo	o	m	
Ll			co	&	00	CO	CM	<r	CO		03		CM	CM	r—4	<r		
cu  >			CM  o		l—i	i—i	i—4	1—4	i—4		S		t—4		l-H	i—i		g
<	Ll			W							o*							
	CU			Q							CO							
	■u		CO		o	o	o	o	o	o	Co	o	o	O	m	o	o	
	co		>•>		o	o	o	o	o	o	CO	o	o	o	CM	o	o	
			CO		o	o	vo	o	o	o		o	o	o	CO	o	o	
			l		a	m	Mt	o'	r*	,_T		I-"	o	f'-		o'	m	
			CO		CO	CO	CM	i—4	co	vo		CM	CO	o		o	CO	
			CM		CM	rH1		o	r—l			r—l	m	CM		co	i—i	
			O													CM		
																1-1		
		CU																
		00					n-											
		CO	CO *tH															
		c	cu E		m	as oo	co	CO	1".	mT		m	<T	o		O	<f	
		•rH	U		m	o	m	ON	00	1—1		<r	m	r"-		o	CM	
		co	co cr		CO	CM CM		00	CM	CO		CM	CO	<r		r—4	CO	
		H	co			CO												
		Q	v—'					1—1					CO			<r		
																CM		
														co				
							CO							CL				
			c				CL		CO	i—4						CO		
			o						CL	<u						CL		
			•M			CO				Q				c				
			■M			CL	CU										co	
			CO				i—4		*o					o	o	00	CL	
			c				r-4		L4	C		44		44	z	D		
			•H		co	'V	•r4		o	O		cu		co		P		
			e		CL	In	>	44	Pn	4-J		cu	CO	cu	>v	43	Li	
			u			O	CU	c		00		LI	fL	oo	Ll	CO	CU	
			<U			CM	00	3	CO	c		O 43		o	CO	•rl	44	
			4-1		<u	M	CU	>s	X>	•iH					44	Ll	CO	
			CU		c	CU		CO	X)	E		00 co	4-J		O	Ll	CO	
			T3		M	4-1		C	CO	r—4		C PL	u	Li	43	CO	O	
					CU	CO	o	CO	43	•H		•iH	o	CO	•rH	ffi	c	
			CM		PQ	M	u	2	O	s		C «	CL	(U	Ll		CO	
			O			O						o 00	?	C	H	44	|4)	
					4-1		M	4-J •	4-J	4-J		43 C	CU			CO		
			<U		co	4-J	CO	co CO	CO	co		CO *H	Z	44	44		44	
			o			CO	CU	CL				S C		(U	<u •	Ll	CO	
			CO		U		c	U	44	44		CU O	44	CU	CU CO	CU		
					cu	44		CU «	cu	cu		C 43	CO	Ll	Li CL	>	44	
			CL		>	CU	44	> CO	dJ	cu		C CO		O	O	•rH	CU	
					•H	cu	CU	•H t4	Li	M		•<h E	u			Crf	<u	
			X3		Crf	M	cu	Crf 4=	O	O		CO d)	cu	44	44 CO		Ll	
			c			U	Ll	CL				, c	c*	d)	CU r-l	CO	O	
			CO				CJ	i—4 r—4	d)	cu		44 C	•rH	c	c o	C		
			E			c		i—4 CU	c	c		L4 -H	(rf	•H	•rH C	c	CO	
					•M	cu	44	•i-4 X)	•H	•iH		O CO		O	2J W	CO	00	
			CO		44	E	O	44 CO	£				CO	00	00	43	o	
			CU		i—i	o	CO	r-4 t—4	>>			Li	44	o	O Ll	CU	44	
			u		to	•rH	CL	>, *.-4	X)	•o		4J CO	CO	TJ	T3 CO	D	CO	
			4-1		a	44	CL	a 43	c	C		CO d)	•rH	O	O CU	cr	dJ	
			C/D		43	M	•r4	43 CL	CO	CO		Li C	C	c	c c	CO	c	
					O	<U	44	O	u	V4		•H	a	o	o	3	o	
					CO	PL	CO	CO	PQ	PQ		PH	*-)	o	o	CO	o	
			4-)															
			U															
			O •		co	CM	<r	ON	Mf			CM	<r	o	1—1	co	00	
			CL O		CM	CO	co	CO	VO	vo		1—1		00	oo	00	ON	
			CU Z									CM	CM	CM	CM	CM	CM	

<r

<r

o

o

<y>

CO

CO

i-'*

o

MI-

NO

o

o

o

IT)

vO

CM

o

I

CM

O

o

o

VO

m

o

o

o

co

m

oo

r''.

vo

co

CO H O co O cu C C

m

CM

vo

o

o

CM

CM 1—I CM

00

VO

o

CO

CM

CO

CM

I

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CM

CM

CO

O

VO

•rH in

co r-~ u • Q O

CO 43

Northwest Branch Anacostia River	21.1	7,810 1.02	14,200	672	21-23	11,000	3,200	50.47	4,150	13,000	616

near Colesville, Md.﻿APPENDIX B

401

DATA SOURCES

METEOROLOGIC DATA

The original records of observations provide the most detailed information about weather events, and such records were the sources of the wind, pressure, and temperature data presented in this report. Examples of these records are presented in R. M. DeAngelis and W. T. Hodge, “Preliminary Climatic Data Report, Hurricane Agnes June 14-23, 1972,” NOAA Tech. Memo. EDS NCC-1, Aug. 1972.

Precipitation data used in constructing the mass curves of rainfall and the isohyetal maps were obtained from the monthly publications “Hourly Precipitation Data” and “Climatological Data.” These data were supplemented by the bucket-survey measurements listed in table 4.

Information on deaths and property damage was obtained from R. M. DeAngelis, “North Atlantic Tropical Cyclones,” 1972, Climatological Data National Summary, Annual 1972, pp. 62-69.

The above records and publications, as well as radar photographs of storm precipitation and cloud patterns, may be obtained from the NOAA-EDS National Climatic Center, Federal Building, Asheville, N.C. 28801. Satellite photographs like those presented herein may be obtained from the NOAA National Environmental Satellite Service, Washington, D.C. 20233. Government regulations require payment for providing copies of unpublished and published data and other material, and a cost estimate should be requested before placing an order.

FLOOD DATA

This report contains the most frequently used types of information on the floods of June, July 1972, but much detailed additional information was not published owing to space limitations. These additional data consist of continuous-stage records, miscellaneous water-surface readings, measurements of flow, cross sections of channels and surveys of stream reaches, floodmarks, and other direct observations. Though applying only to a relatively small number of places, the data greatly augment those presented here.

Additional streamflow data may be obtained by contacting the U.S. Geological Survey at the following addresses:

State	Address

Connecticut_______P.O. Box 715

Room 235 Post Office Building 135 High Street Hartford, Conn. 06101

New York__________P.O. Box 948

Room 343, U.S. Post Office and Court House Broadway & Albany Streets Albany, N.Y. 12201

Pennsylvania _____P.O. Box 1107

4th Floor Federal Building 228 Walnut Street Harrisburg, Pa. 17108

West Virginia_____Room 3303 Federal Building

500 Quarrier Street, East Charleston, W. Va. 25301

Maryland__________8^09 Satyr Hill Road

Parkville, Md. 21234

Virginia__________Room 304, 200 West Grace Street

Richmond, Va. 23220

North Carolina —P.O. Box 2857

Room 440 Century Station Post Office Building

Raleigh, N.C. 27602

State agencies concerned with such activities as highways, health, planning, and public works frequently collect information on outstanding floods. Counties, towns, cities, and villages are possible sources of local area information.

Among the Federal agencies where flood data may be obtained are: Civil Defense Administration; Department of the Army, U.S. Corps of Engineers; Soil Conservation Service, U.S. Department of Agriculture.

The U.S. Geological Survey and its cooperating state agencies have published many reports on the floods of June-July 1972. These publications consist primarily of hydrologic atlases and open-file reports. The publications are available for inspection in the offices of the Geological Survey previously listed and in offices of cooperating state agencies. Copies of many of the reports can be obtained. The following reports have been published:

Hydrologic atlases.—Flooded areas are delineated on 7.5' topographic maps at scales 1:24,000. Darmer, K. I., and Wagner, L. A., 1973, Flood of June 1972 at Elmira, New York: U.S. Geol. Survey Hydrol. Inv. Atlas HA-518.

------- 1973, Flood of June 1973 at Corning, New

York: U.S. Geol. Survey Hydrol. Inv. Atlas HA-519.

Flippo, H. N., Jr., and Lenfest, L. W., Jr., 1973, Floods of June 1972 in Wilkes-Barre area, Pennsylvania: U.S. Geol. Survey Hydrol. Inv. Atlas HA-523.

Page, L. V., and Shaw, L. C., 1973, Floods of June 1972 in the Harrisburg area, Pennsylvania: U.S. Geol. Survey Hydrol. Inv. Atlas HA-530. Open-file flood maps.—Flooded areas are delineated on 7.5' topographic maps at scale 1:24,000.﻿402

HURRICANE AGNES RAINFALL AND FLOODS, JUNE-JULY 1972

Quadrangle Name	Map Title

Addison, N.Y.------------Canisteo River, Tuscarora Creek

and Tioga River near Addison, New York.

Angelica, N.Y. ----------Genesee River near Belfast, New

York.

Bath, N.Y. --------------Cohocton River at Bath, New York.

Belmont, N.Y.------------Genesee River at Belmont, New

York.

Big Flats, N.Y.----------Chemung River at Big Flats, New

York.

Borden, N.Y.-------------Canisteo River near Rathbone, New

York.

Burdett, N.Y. -----------Seneca Lake Inlet at Watkins Glen.

New York.

Caledonia, N.Y.----------Genesee River at Avon, New York.

Cameron, N.Y.____________Canisteo River at Cameron, New

York.

Campbell, N.Y.-----------Cohocton River at Campbell, New

York.

Canisteo, N.Y.-----------Canisteo River at Canisteo, New

York.

Caton, N.Y.-Pa.__________Chemung River at Corning Manor,

New York.

Corning, N.Y.____________Chemung, Tioga, and Cohocton

Rivers at Corning, New York.

Elmira, N.Y._____________Chemung River and Newton Creek

at Elmira, New York.

Fillmore, N.Y.___________Genesee River at Fillmore, New

York.

Geneseo, N.Y. ___________Genesee River at Geneseo, New

York.

Genesee Junction, N.Y.____Genesee River near Rochester, New

York	,

Harrisburg West, Pa._____Susquehanna River, Paxton Creek,

and Conodoguinet Creek at Harrisburg, Pennsylvania.

Hornell, N.Y. ___________Canisteo River and Canacadea Creek

at Hornell, New York.

Houghton, N.Y.___________Genesee River at Houghton, New

York.

Ithaca West, N.Y.________Cayuga Inlet and Cayuga Lake at

Ithaca, New York.

Kingston, Pa. ___________Susquehanna River at Kingston,

Pennsylvania.

Knapp Creek, N.Y.________Allegheny River at Allegany, New

York.

Lemoyne, Pa._____________Susquehanna River at Lemoyne,

Pennsylvania.

Limestone, N.Y. _________Alleghenv River near Limestone,

New York.

Lock Haven, Pa.----------West Branch Susquehanna River

and Bald Eagle Creek at Lock Haven, Pennsylvania.

Middletown, Pa. _________Susquehanna River and Swatara

Creek at Middletown, Pennsylvania.

Mill Hall, Pa.___________BaH Fao-le and Fishing Creeks at

Mill Hall, Pennsylvania.

Montour Falls, N.Y.______Catharine Creek and S°neca Lake

Inlet at Montour Falls, New

Moravia, N.Y.____________Owasco Inlet at Moravia, New

York.	,

Mount Morris, N.Y._______Genesee River near Mount Morris,

New York.

Olean, N.Y. _____________Allegheny River and Olean Creek

at Olean, New York.

Pittston, Pa.____________Susquehanna River in the vicinity

of Wilkes-Barre and Pittston, Pennsylvania.

Portageville, N.Y. ______Genesee River at Portageville, New

York.

Portville, N.Y.__________ Allegheny River at Portville,

New York.

Rathbone, N.Y.-----------Canisteo River at Rathbone, New

York.

Rush, N.Y. ______________Genesee River near Avon, New

York.

Quadrangle Name	Map Title

Salamanca, N.Y.___________Allegheny River at Salamanca, New

York.

Savona, N.Y. _____________Cohocton River at Savona, New

York.

Seeley Creek, N.Y.-Pa.____Chemung River near East Coming,

New York.

Steel ton, Pa. ___________Susquehanna River and Yellow

Breeches Creek at Steelton, Highspire, and New Cumberland, Pennsylvania.

Syracuse West, N.Y._______Onondaga Lake and Leg Creek at

Syracuse, New York.

Towlesville, N.Y. ________Canisteo River near Canisteo, New

York. ,

Waverly, N.Y.-Pa._________Chemung River near Waverly, New

York.

Wellsburg, N.Y.-Pa._______Chemung River at Wellsburg, New

York.

Wellsville North, N.Y.____Genesee River at Scio and Dyke

Creek at Wellsville, New York.

Wellsville South, N.Y.____Genesee River and Dyke Creek at

Wellsville, New York.

Wilkes-Barre West, Pa.____Susquehanna River at Wilkes-Barre

and Plymouth, Pennsylvania.

Open file flood maps delineating flooded areas were prepared for the flood of June 1972 using aerial photographs obtained at or near the flood crest. The delineation is shown directly on the photomosaics compiled from the photography. These maps have been prepared for selected reaches on the following streams:

Potomac River near Washington, District of Columbia

Susquehanna River at Harrisburg, Pennsylvania

Yellow Breeches Creek near Harrisburg, Pennsylvania

Occoquan Creek near Occoquan, Virginia Four Mile Run at Alexandria, Virginia Patuxent River near Laurel, Maryland Seneca River near Seneca, Maryland Rappahannock River near Fredericksburg, Virginia

James River at Richmond, Virginia Anacostia River near Washington, District of Columbia

Patapsco River near Hollofield, Maryland

Other technical information available on the June-July 1972 floods include:

Tropical Storm Agnes, Hydrologic Study, Reports, 1, 2, 3, by Department of the Army, U.S. Corps of Engineers, North Atlantic Division, New York, New York 10007.

Pictorial reports were prepared on the June-July 1972 floods by many magazines and newspapers. These reports can generally be inspected at the publication offices from which they originate.﻿APPENDIX B

403

The U.S. Geological Survey and its cooperating state agencies have published many reports on previous floods in the areas of the East that experienced the June-July 1972 floods. These reports provide much detailed peak-flow information on previous floods for comparison with June-July 1972 data. The following is a selected list of such publications :

The New England Flood of November 1927, U.S.

Geol. Survey Water-Supply Paper 636-C.

The New York State Flood of July 1935, U.S. Geol.

Survey Water-Supply Paper 773-E.

The Floods of March 1936 (Part 1) New England Rivers, U.S. Geol. Survey Water-Supply Paper 798.

The Floods of March 1936 (Part 2) Hudson River to Susquehanna River, U.S. Geol. Survey Water-Supply Paper 799.

The Floods of March 1936 (Part 3) Potomac, James and Upper Ohio Rivers, U.S. Geol. Survey Water-Supply Paper 800.

Hurricane Floods of 1938 in North Atlantic States, U.S. Geol. Survey Water-Supply Paper 966.

The Floods of August-October 1955 New England to North Carolina,, U.S. Geol. Survey Water-Supply Paper 1420.

New Year Flood of 1949 in New York and New England, U.S. Geol. Survey Circular 155.

Floods of August and September 1972 in New Jersey, New Jersey Dept, of Environmental Protection, Div. of Water Resources, Special Report No. 37.

Floods of August 1967 in Maryland and Delaware, U.S. Geol. Survey open-file report.

Flood of August 24-25, 1967 in the Washington Metropolitan Area, U.S. Geol. Survey open-file report.

Flood of July 22, 1969 in the Northern Virginia Area, U.S. Geol. Survey open-file report.

Flood of August 1969 in Virginia, U.S. Geol. Survey open-file report.

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Sedimentation and Tectonics in the Early Tertiary Continental Borderland Of Central California

GEOLOGICAL SURVEY PROFESSIONAL PAPER 925

DOCUMENTS DEPARTMENT MAY 3 1 1975

LIBRARY

I	V ../if,,﻿﻿Sedimentation and Tectonics in the Early Tertiary Continental Borderland Of Central California

By TOR H. NILSEN and SAMUEL H. CLARKE, Jr.

GEOLOGICAL SURVEY PROFESSIONAL PAPER 925

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1975﻿UNITED STATES DEPARTMENT OF THE INTERIOR ROGERS C. B. MORTON, Secretary

GEOLOGICAL SURVEY

V.	E. McKelvey, Director

library of Congress catalog - card No. 7 5-7624

For sale by the Superintendent of Documents, U.S. Government Printing Office

Washington, D.C. 20402﻿CONTENTS

Page

Abstract __________________________________________________ 1

Introduction_______________________________________________ 1

Acknowledgments_________________________________________ 3

Summary of Mesozoic tectonic history_______________________ 3

Lower Tertiary stratigraphic units ________________________ 4

Northwestern area_______________________________________ 6

Gualala area________________________________________ 6

Point Reyes_________________________________________ 7

Point San Pedro_____________________________________ 7

Santa Cruz Mountains________________________________ 7

San Juan Bautista area ___________________________ 11

Point Lobos________________________________________ 11

Northern Santa Lucia Range________________________ 11

Adelaida area______________________________________ 12

La Panza, southern Santa Lucia, and Sierra Madre

Ranges___________________________________________ 12

Patti way Ridge area_______________________________ 12

Mount Pinos area __________________________________ 13

Northeastern area______________________________________ 13

Sierra Nevada______________________________________ 13

Franciscan assemblage in the northern Coast Ranges_14

Round Valley area__________________________________ 14

Rice Valley area___________________________________ 14

Middle Mountain area_______________________________ 15

Clear Lake area____________________________________ 15

Mount Diablo area and Sacramento Valley area------ 15

San Leandro Hills__________________________________ 17

San Jose area______________________________________ 17

Tesla area_________________________________________ 18

Orestimba area ____________________________________ 19

Laguna Seca area___________________________________ 19

Bolado Park area __________________________________ 19

Vallecitos area ___________________________________ 20

Northern Temblor Range, southern Diablo Range,

and adjacent San Joaquin Valley_________________ 21

San Emigdio and western Tehachapi Mountains

and adjacent southern San Joaquin Valley ________ 22

Southern Tehachapi Mountains_______________________ 23

El Paso Mountains__________________________________ 24

Page

Lower Tertiary stratigraphic units—Continued

Southeastern area_____________________________________ 24

Cajon Pass area____________________________________ 24

Orocopia Mountains_________________________________ 24

Southwestern area_____________________________________ 24

Ortega Hill, Pine Mountain, Santa Ynez Mountains,

and Topatopa Mountains areas_____________________ 25

Piru Creek area____________________________________ 29

Las Llajas Canyon, Simi Hills, and Santa Susanna

Mountains areas__________________________________ 29

Santa Monica Mountains_____________________________ 30

Elsmere Canyon and Gold Creek areas --------------- 30

Elizabeth Lake Canyon and Valyermo areas------------30

Channel Islands____________________________________ 30

Santa Ana Mountains and San Joaquin Hills ----------31

San Nicolas Island__________________________________31

Western Peninsular Ranges _________________________ 32

Lake Elsinore, Lake Henshaw, and Jaccumba

Valley areas_____________________________________ 32

Northern Bqja California-------------------------   33

Early Tertiary history of the San Andreas fault___________ 33

Early Tertiary paleogeography______________________________36

Introduction__________________________________________ 36

Source areas _________________________________________ 36

Eastern nonmarine deposits ___________________________ 39

Shallow marine shelf deposits _________________________40

Continental slope and ocean floor deposits_____________42

Introduction________________________________________42

Hemipelagic deposits _______________________________42

Deep-sea fans deposited east of the borderland and

derived from eastern source areas_________________43

Continental borderland deposits _______________________45

Deep-sea trench deposits_______________________________46

Sedimentology of the borderland deep-sea fans--------------47

Tectonic framework of borderland sedimentation-------------48

Summary and conclusions __________________________________ 52

References cited__________________________________________ 54

ILLUSTRATIONS

Page

Figure 1. Index map of California showing major geomorphic and tectonic provinces, major faults, and informal geographic divisions—	2

2. Index map of California showing outcrops of lower Tertiary sedimentary rocks______________________________________ 4

3. Index map of the western Transverse Ranges showing outcrops of lower Tertiary sedimentary rocks___________________ 26

4.	Diagram showing inferred history of offset along the San Andreas fault in central California--------------------- 34

5.	Schematic maps showing Mesozoic and Cenozoic plate relations in the western Pacific Ocean________________________ 35

6.	Diagrammatic sketch showing the early Tertiary tectonic development of central California------------------------ 37

7.	Generalized paleogeographic map of early Tertiary California_____________________________________________________ 38

8.	Generalized map showing tectonic activity within the early Tertiary continental borderland of western C alifomia -50

III﻿IV

CONTENTS

TABLES

Page

Table 1. Lower Tertiary megainvertebrate and foraminiferal stages in California_________________________________________________ 5

2.	Sedimentary structures and features reported from inferred deep-sea fan deposits of the early Tertiary continental bor-

derland and adjacent areas of California_________________________________________________________________________ 8

3.	Comparison of thicknesses and depositional intervals of inferred deep-sea fan deposits of the early Tertiary continental

borderland and adjacent areas of California _____________________________________________________________________ 10﻿SEDIMENTATION AND TECTONICS IN THE EARLY TERTIARY CONTINENTAL BORDERLAND OF CENTRAL CALIFORNIA

By Tor H. Nilsen and Samuel H. Clarke, Jr.

ABSTRACT

We infer that the most prominent early Tertiary paleogeographic features of central California were the Sierran landmass to the east and the Salinian island area or peninsula to the west, both underlain by granitic crust, and a trough-shaped deep marine basin which separated the two, underlain by oceanic crust. These elongate elements trended approximately north-south, parallel to the edge of the North American continent. Clastic sediment from erosion of the Sierran landmass was transported westward and deposited in adjacent fluvial, nearshore, shallow marine, and deep marine environments. The Salinian area was probably detached from the Sierran landmass by pre-Eocene right-lateral faulting along its eastern edge; it formed a continental borderland consisting either of irregular island uplands separated by deep marine basins or a very irregularly shaped peninsula.

Detritus eroded from the borderland was deposited primarily as submarine fans at bathyal to abyssal depths within the borderland basins and on the sea floor to the east and west. These early Tertiary submarine fan deposits are similar throughout the central Coast Ranges and contain assemblages of proximal and distal turbidites, deep-sea conglomerates, grain-flow deposits, and hemipelagic shales. They differ from most modem deep-sea fan deposits and typical flysch sequences in that they are very thick but limited in areal extent, and consist mostly of coarse terrigenous detritus. The conglomerates commonly contain clasts as large as boulders, are very thickly and irregularly bedded, and are generally not laterally persistent. Sandstones deposited in more proximal parts of the fans consist primarily of conglomeratic Bouma ae channel deposits that are very thickly bedded, amalgamated, poorly graded to ungraded, without prominent current-generated sedimentary structures, and containing large mudstone rip-up clasts, diffuse parallel laminae, and dish structures. Sandstones deposited in more distal parts of the fans generally contain more complete Bouma sequences, are more thinly bedded, have a greater variety of current-generated sedimentary structures, and are graded. Hemipelagic shales and thin Bouma cde sequences were deposited at and beyond the margins of the deep-sea fans and locally in the interchannel areas of the more proximal parts of the fans.

The borderland region was tectonically active during sedimentation, so that island or peninsula source areas and depositional basins formed and changed abruptly. Submarine fan sedimentation was rapid, but the supply of sediment was probably not continuous for long periods of time. Paleocurrent directions are varied, reflecting the irregular distribution of source areas and depositional basins.

INTRODUCTION

The lower Tertiary marine sedimentary rocks that crop out in geographically restricted areas of the Coast and Transverse Ranges of western California have at-

tracted the attention of many geologists during recent years (fig. 1). These rocks form sequences as much as 25,000 ft (7,600 m) thick in some areas. The rocks consist primarily of thickly bedded to massive, medium- to coarse-grained sandstone with subordinate amounts of conglomerate, siltstone, and mudstone. Ungraded sandstone beds as much as 75 ft (23 m) thick or more have been noted; other thick beds may be reverse-graded in the lowermost part or normally graded in the uppermost part, with sandstone grading sharply upward into thin siltstone or mudstone layers. These sandstones typically lack internal structures except for large irregularly shaped mudstone clasts, diffuse parallel laminations, and dish structures, which were first recognized in these rocks by Wentworth (1967).

The origin of these sandstone sequences has been the subject of considerable controversy, and in the past they have been interpreted as shallow marine transgressive and regressive shelf deposits, deltaic deposits, a type of flysch, a type of turbidite, grain-flow deposits, and more recently, as deep-sea fan deposits. The few megafossils found in these rocks are generally individual abraded and broken mollusk shells that probably have been transported considerable distances. Microfossils are generally common in both interbedded mudstones and in thicker mudstone and shale sequences. These microfossils, particularly benthonic and planktonic foraminifers, permit reasonably reliable age assignments and provide some information about depths of water and access of the depositional site to the open ocean.

The sandstones are generally good reservoirs for oil and gas and detailed subsurface data are locally available to permit definition of the areal extent and lateral facies changes in the units. Although most of the lower Tertiary sequences have been mapped in some detail, sedimentological and paleontological studies have been completed for very few.

Detailed sedimentologic studies by other workers during the past 10 years have greatly clarified and facilitated our understanding of the depositional proc-

1﻿2

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Figure 1.—Index map of California showing major geomorphic and tectonic provinces, location of some major faults, and the four informal

geographic divisions used in this paper (modified from Bailey, 1966).

esses and sedimentary history of these lower Tertiary rocks. In particular, we depend heavily on studies by Stauffer (1965, 1967) in the Santa Ynez Mountains, Wentworth (1966, 1968) in the Gualala area, Yeats (1968), Cole (1970), Merschat (1971) and Parsley (1972) in the central Transverse Ranges, Channel Islands, and San Nicolas Island, Chipping (1970a, b, 1972a) in the

southern Coast Ranges, and Link (1971,1972) and Sage (1973, 1974) in the southern Coast Ranges, Transverse Ranges, and Peninsular Ranges. By adding to their conclusions the results of our work in the Santa Cruz Mountains (Nilsen and Simoni, 1973), central Coast Ranges (Nilsen and others, 1974), and southern Coast Ranges (Clarke, 1973; Nilsen, 1973c; Nilsen and﻿SUMMARY OF MESOZOIC TECTONIC HISTORY

3

Clarke, 1973), we here synthesize the available data about the early Tertiary history of California. We emphasize the area extending from the Transverse Ranges on the south to the San Francisco Bay region on the north (fig. 1).

Studies of these lower Tertiary rocks, because they are located at the western margin of the North American lithospheric plate, can provide valuable information about the early Tertiary history of the San Andreas fault and the interactions between the continental North American plate and oceanic plates to the west. Of particular interest is the inferred change in tectonic style at the plate boundaries at the western edge of North America, from subduction of the ocean floor in Mesozoic time to right-lateral slip along transcurrent faults in Cenozoic time. The purposes of this paper are

(1)	to describe these unusual deposits in some detail, (2) to present our interpretations of their depositional processes and environments, (3) to outline our conclusions concerning the early Tertiary paleogeography of western California, and (4) to summarize the relations between early Tertiary tectonic activity and sedimentation in the region.

Before discussing the lower Tertiary sedimentary rocks in detail, we shall briefly summarize the Mesozoic tectonic history of California, because it influenced the framework of early Tertiary sedimentation and tectonics.

ACKNOWLEDGMENTS

Work by Nilsen has been partly funded by a U.S. Geological Survey Post-Doctoral Research Associate-ship. Clarke’s contribution is based partly on his doctoral research, conducted under the direction of Drs. F. A. F. Berry and C. M. Gilbert, and funded in part by grants from the Penrose Bequest Fund of the Geological Society of America, the Amoco Production Company, and the Graduate Division of the University of California, Berkeley. We thank W. R. Dickinson, J. G. Vedder, T. W. Dibblee, Jr., J. C. Crowell, D. G. Howell, and E. E. Brabb for helpful and thought-provoking reviews of the manuscript, and R. H. Campbell, D. L. Durham, R. F. Yerkes, G. W. Moore, and G. L. Peterson for helpful discussions.

SUMMARY OF MESOZOIC TECTONIC HISTORY

The three main rock units of Mesozoic age in central California are the Franciscan assemblage, the Great Valley sequence, and granitic and related intrusive rocks. Interpretations by others of the structural, stratigraphic, and chronologic relations between these units indicate the presence of a deep-sea trench and subduction zone along the Mesozoic continental margin. Within this framework, the Franciscan rocks are thought to have been underthrust eastward beneath the

Great Valley sequence concurrently with the intrusion of granitic plutons in the Sierra Nevada (Bailey and others, 1964; Hamilton and Myers, 1966; Hsu, 1968; Bailey and Blake, 1969; Hamilton, 1969; Page, 1970b; Ernst, 1970; Bailey and others, 1970; Dickinson, 1971). Granitic intrusions of similar age are present in the Klamath Mountains, Salinian block, Mojave Desert, Transverse Ranges and Peninsular Ranges (Evernden and Kistler, 1970; Ross, 1972). The faulted contact of the Great Valley sequence and the Franciscan assemblage has been designated the Coast Range thrust (Bailey and others, 1970), and includes the South Fork Mountain, Stony Creek, Tesla-Ortigalita, and Sur-Nacimiento faults. The Coast Range thrust may represent a Mesozoic Benioff zone (Ernst, 1970). Bailey and Blake (1969) inferred that the Franciscan and Great Valley rocks were deposited concurrently in essentially parallel but separated linear belts, both underlain by oceanic crust. The Great Valley sequence, and possibly the Franciscan assemblage, were derived from source areas to the east in the Sierra Nevada area (Ojakangas,

1968). Deposition continued through the middle Cretaceous, followed by underthrusting and penecontem-poraneous sedimentation until the latest Late Cretaceous. Dickinson (1971) interpreted the history as representing concurrent deposition of the Great Valley sequence in an arc-trench gap and deformation of the Franciscan rocks in an adjacent trench to the west.

Beginning probably late in Cretaceous time, this inferred tectonic framework, which had previously been dominated by underthrusting of oceanic crust, apparently changed to one dominated by right-lateral faulting subparallel to the coast. The postulated offsets of Cretaceous rocks along the San Andreas fault suggest that as much as 350 miles (560 km) or more of right-lateral slip has accumulated along the fault since Cretaceous time (Dibblee, 1966b; Wentworth, 1968; Hill and Hobson, 1968; Ross and others, 1973). If this conclusion is correct, the Salinian block was sheared off the southern end of the Sierra Nevada and displaced 350 miles (560 km) to the northwest, where it is presently bounded on both east and west by Franciscan rocks. The old Mesozoic subduction zone was thus split into two separate segments. At the beginning of Tertiary time the Salinian block was probably in motion and must have had a major effect on early Tertiary sedimentation. It was deformed so that basins formed locally within it and parts of it also became source areas for sediment. At about the same time, east-west tectonic trends began to develop in the area of the Transverse Ranges, and the Sierra Nevada, Mojave Desert, and other areas to the east were uplifted to form a mountainous terrain that served as a source area for sediment. Thus, earliest Tertiary sedimentation in central﻿4

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

I20°W

Figure 2.—Index map of California showing the distribution of outcrops of lower Tertiary sedimentary rocks.

California took place within a general tectonic framework dominated by strike-slip faulting. An uplifted continental landmass lay to the east and a partly uplifted sliver of continental crust, the Salinian block, jutted out to the northwest from the otherwise regular continental margin, with a marine trough or marginal sea separating the two areas.

LOWER TERTIARY STRATIGRAPHIC UNITS

Lower Tertiary sedimentary rocks are irregularly

distributed in California. Marine rocks are most widespread in the Coast Ranges, beneath younger sediments of the Great Valley, in the Transverse Ranges, and along the western flanks of the Peninsular Ranges (figs. 1, 2). Nonmarine rocks are most abundant along the western flank of the Sierra Nevada, in subsurface along the east side of the Great Valley, and in scattered outcrops in the Great Basin, eastern Transverse Ranges, and along the western flanks of the Peninsular Ranges. Eocene rocks are missing from or only locally present in﻿LOWER TERTIARY STRATIGRAPHIC UNITS

5

Table 1.—Lower Tertiary megainvertebrate and foraminiferal stages in California

[Megainvertebrate stages from Weaver and others (1944); benthonic foraminiferal stages from Kleinpell (1938) and Mallory (1959); planktonic foraminiferal, nannoplankton and coccolith age modifications from Bukry and Kennedy (1969), Schmidt (1970, 1971), Brabb, Bukry, and Pierce (1971), Steineck and Gibson (1971), Steineck, Jervey and Gibson (1972), and Gibson and Steineck (1972a, b). The standard megainvertebrate and benthonic foraminiferal stages are used in this report]

				Pacific Coast provincial stages		Tentative classifications
System	Sub-  system	Series	Sub-  series			based on planktonic Foraminifera, coccoliths,
				Megainvertebrate marine fossils	Benthonic	
					Foraminifera	and nannoplankton
		O  £				
	rQ CO  g'-e	o  o  bO		Refugian	Refugian	Upper  Eocene
		o				
			n 2			
			Oh 9 £•8	'Tejon”	Narizian	Middle  Eocene
		0)		"Transition”		
		£  CD	=2 £  2 <L>		Ulatisian	
						
£  2g	£	o  W	a °	"Domengine”		
	a					
H						
05						Lower
W  H	o>		u 2  CD £	"Capay”	Penutian	Eocene
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the Klamath Mountains, Cascade Range, Modoc Plateau, Great Basin, Mojave Desert, and Salton Trough provinces (figs. 1, 2).

Volcanic rocks are generally not present in the Paleocene and Eocene deposits, although scattered occurrences of tuffaceous sediments and bentonites attest to some volcanic activity. The Lovejoy Formation of Durrell (1959), a basaltic unit in the northern Sierra Nevada, is considered by Durrell (1959, 1966) to be of late Eocene age; however, Dalrymple (1964) suggested a younger age on the basis of radiometric age determi-| nations. No lower Tertiary volcanic rocks have been mapped in the central or southern Sierra Nevada (Slemmons, 1966). Minor amounts of greenstone that may be early Tertiary in age are reported to be present

in the "coastal belt” sequence of the Franciscan assemblage (Bailey and others, 1964; O’Day and Kramer,

1972).

The lower Tertiary System of California has been ( divided into provincial stages on the basis of megainvertebrate and benthonic foraminiferal fossils (table 1).

We shall refer in the text to the time-rock correlations of Kleinpell (1938), Weaver and others (1944), and Mallory (1959) in discussing the ages of various units, although recent studies of planktonic foraminifers, nannoplankton, and coccoliths have indicated that the older correlations are in need of revision; these tentative correlations are indicated in the right-hand column of table 1, but will not be referred to in the text.

We have divided California into four areas for a gen-﻿6

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

eral review of the nature and distribution of the lower Tertiary stratigraphic units (fig. 1). The four areas, bounded by major faults, are distinctive early Tertiary paleogeographic provinces characterized by somewhat different styles of sedimentation and tectonic activity. The San Andreas fault is used as the major boundary between the areas partly because of the inferred large amount of post-early Tertiary right-lateral offset along it. The stratigraphic sequences within each area are described in ascending order and from north to south. The sedimentary structures and bedding features, and the thickness and age of most of the units inferred to be deep-sea fan deposits are summarized in tables 2 and 3, respectively.

NORTHWESTERN AREA

The northwestern area, the Salinian block, extends approximately from Point Arena on the north to near the southern end of the Coast Ranges (fig. 1). Its eastern boundary is the San Andreas fault except in the San Francisco Bay region, where the Pilarcitos fault is the boundary. Its western boundary is formed genetically by the Sur-Nacimiento and southern Rinconada faults and the southern boundary arbitrarily is the Big Pine fault. The northern boundary of the Salinian block is in the Point Arena area, the northernmost offshore extent of granitic rocks (Silver and others, 1971). Thus, the Salinian block lies wholly within the Coast Ranges province and is underlain by a granitic basement complex.1

Within the Salinian block, the lower Tertiary rocks are distributed very unevenly as restricted outcrop areas with large intervening areas in which such rocks are missing. Thick sequences of lower Tertiary marine sedimentary rocks crop out in the Gualala area, the Santa Cruz Mountains, and in the southern Santa Lucia, La Panza, and Sierra Madre Ranges (fig. 2). A sequence of moderate thickness crops out in the northeastern Santa Lucia Range. Isolated thinner sequences are present locally at Point Reyes, near San Juan Bautista, and at Point Lobos. The three thick sequences contain both Paleocene and Eocene units, while the thin sequences contain either Paleocene or Eocene units. Because the Salinian block and the Transverse Ranges to the south formed the early Tertiary continental borderland of central California, this area will receive primary emphasis in this paper.

Lower Tertiary marine strata in the central and southern parts of the northwestern area are overlain conformably or unconformably by nonmarine strata of late Eocene, Oligocene, and early Miocene age. These nonmarine strata consist generally of coarse-grained

'The lower Tertiary rocks of the Gualala area are a possible exception, as they rest on a spilite which may possibly be part of the Franciscan assemblage (Wentworth, 1966, 1968). Thus, this area may not be part of the Salinian block; however, for convenience this area is here considered part of the Salinian block.

clastic rocks that were deposited in a variety of fluviah environments. They include the Zayante Sandstone of Oligocene and early Miocene (?) age in the southern Santa Cruz Mountains (Clark, 1966); the red beds of Kerr and Schenck (1925) in the San Juan Bautista area (Clark and Reitman, 1973); the Berry Formation of Oligocene (?) age in the northern Santa Lucia Mountains (Durham, 1974); the Tierra Redonda Formation of early and middle Miocene age in the Adelaida area (Durham, 1968, 1974); a variety of Oligocene and Miocene strata in the La Panza, southern Santa Lucia, and Sierra Madre Ranges (Chipping, 1972a); the Simmler Formation of Oligocene (?) age in the Patti way Ridge area (Dibblee, 1973c; Bartow, 1974); and the Plush Ranch Formation of Carman (1964) of Oligocene (?) age on the south flank of Mount Pinos.

GUALALA AREA

Paleocene and Eocene marine sedimentary rocks of the German Rancho Formation of Wentworth (1968) crop out near Gualala in the northern Coast Ranges, where they rest conformably on similar Upper Cretaceous marine sedimentary rocks and are overlain by a basalt thought to be of Miocene age (Weaver, 1944; Wentworth, 1966,1968). The lower Tertiary sequence is at least 10,000 ft (3,000 m), and possibly as much as

20,000	ft (6,000 m) thick. Sparse "Martinez” megafossils are present 2,400 ft (730 m) above the base, and "Capay” or "Domengine” megafossils are present in the upper part of the formation, although the top of the sequence may be as young as late Eocene. The German Rancho Formation consists mostly of medium- and coarse-grained sandstone and conglomerate sequences that are irregularly distributed and difficult to correlate or subdivide into members; subordinate amounts of rhythmically interbedded fine- to medium-grained sandstone and mudstone are also present, as well as some unusual red mudstone.

Conglomerate clasts in the German Rancho Formation are composed of granite, amphibolite, biotite schist, gneiss, quartzite, marble, and intermediate and felsic porphyritic volcanic rocks. The arkosic sandstone was described by Wentworth (1968) as being rich in potassium feldspar; however, Nilsen, Dibblee, and Simoni (1974) found that 15 sandstone samples from the southern part of the outcrop area were 18-37 percent quartz, 12-38 percent potassium feldspar, 33-58 percent plagioclase feldspar, and 1-7 percent lithic fragments. Paleocurrent directions indicate sediment transport toward the northwest from source areas presumably located within the Salinian block. Wentworth (1966, 1968) inferred deposition by turbidity currents in a northwest-trending basin at water depths of one to several thousand feet (300-1,000 m), with an active fault scarp along the western margin of the basin.﻿NORTHWESTERN AREA

7

POINT REYES p6	v,

The Laird Sandstone is exposed in three separate fault blocks at Point Reyes (Weaver, 1949, p. 65; Galloway, 1962, 1966), where it unconformably overlies quartz diorite and is overlain unconformably by Pliocene strata. Its maximum thickness is about 100 ft (30 m). It consists of massive, coarse-grained sandstone and subordinate amounts of conglomerate, with some shale in the upper part. It is thought to be Ynezian in age on the basis of sparse Foraminifera (Galloway, 1961). Conglomerate clasts as much as 2 ft (60 cm) in diameter are composed primarily of quartz diorite from the underlying basement complex. Scant data are available regarding paleocurrent directions, sedimentary structures, and inferred depositional environments of the Laird Sandstone; in addition, its original areal extent is difficult to estimate.

Eocene shales have been penetrated by wells drilled for oil about 17 miles (27 km) east-southeast of Point Reyes (John West, written commun., July 1973), but their thickness and relation to other lower Tertiary stratigraphic units are not known.

POINT SAN PEDRO /«& •	'

Paleocene marine conglomerate, sandstone, and shale about 1,300 ft (400 m) thick crop out on the San Francisco Peninsula southeast of Point San Pedro (Dar-row, 1963). These strata rest unconformably on a flyschlike Upper Cretaceous sequence and are overlain by Quaternary alluvium. Dickerson (1914) concluded that the Tertiary rocks were Paleocene, and Clark (1968) indicated their age as Ynezian(?). The lower Tertiary strata consist of alternating thinly bedded sandstone and shale and locally abundant thickly bedded sandstone and conglomerate (Chipping, 1972b). The sandstones are arkosic and contain more potassium feldspar than plagioclase feldspar; lithic fragments are composed of volcanic, quartzitic, and argillaceous material. Chipping (1972b) inferred that the thinly inter-bedded sandstone and shale were deposited by turbidity currents and that the thickly bedded sandstones and conglomerates were deposited by high-density turbidity currents, grain flows and slurries. He inferred that these sediments were derived from a source area to the southeast, probably in the area of the present northern Santa Cruz Mountains, and were deposited on the upper portion of a submarine fan.

SANTA CRUZ MOUNTAINS

Lower Tertiary marine sedimentary rocks of the Santa Cruz Mountains are a widely distributed sequence of strata as much as 10,000 ft (3,000 m) or more in thickness. The sequence is subdivided into three parts.

(1)	The Ynezian Locatelli Formation of Brabb (1960),

which is 900 ft (270 m) thick. It rests unconformably on granitic basement rocks and is informally divided into two members, a lower sandstone and siltstone member 100 ft (30 m) thick that contains shallow marine mol-lusks, and an upper siltstone member 800 ft (240 m) thick that contains arenaceous foraminifers. It was deposited in progressively deeper marine conditions, the lower part at neritic depths and the upper part at bathyal to abyssal depths, in a basin with unrestricted access to the open ocean (Cummings and others, 1962; Clark, 1968). It contains granitic and metamorphic detritus derived from source areas similar to the underlying basement rocks and well-rounded volcanic clasts that were probably recycled from older conglomerates (Cummings and others, 1962).

(2)	The Butano Sandstone, which is at least 5,000 and possibly as much as 10,000 ft (1,500-3,000 m) thick, of Penutian to Narizian age. It rests unconformably on the Locatelli Formation and is informally divided by Clark (1966,1968) into three members, (a) a lower conglomerate and sandstone no less than 1,500 ft (460 m) thick of Penutian age, (b) a middle siltstone 250-750 ft (75-230 m) thick of Penutian age, and (c) and upper sandstone more than 3,200 ft (980 m) thick of Penutian, Ulatisian, and Narizian age. The conglomerate contains clasts of granite, gneiss, schist, quartzite, and volcanic rocks; the sandstone is arkosic, with 35-60 percent quartz, 20-37 percent potassium feldspar, 5-17 percent plagioclase feldspar, and lesser amounts of biotite and lithic fragments (Brabb, 1960). Beveridge (1958) identified a large suite of heavy minerals including apatite, clinozoisite, epidote, garnet, ilmenite, leucoxene-anatase, magnetite, rutile, sphene, and tourmaline. The Butano Sandstone was deposited at bathyal and abyssal depths in a basin that had unrestricted access to the open ocean (Sullivan, 1962; Cummings and others, 1962; Clark, 1966; Fairchild and others, 1969; Smith, 1971). Paleocurrent and paleoslope patterns and the areal distribution of conglomerate clasts indicate northward-directed sediment transport; deposition is inferred to have been by turbidity currents, grain flows, fluidized sediment flows, slumping and the slow settling out of pelagic detritus (Nilsen, 1970,1971;Nilsen andSimoni,

1973). Nilsen (1971) inferred that the Butano was deposited as a deep-sea fan and was derived from a source area to the south, within the Salinian block, underlain by granitic and metamorphic basement rocks and older conglomerates (Brabb, 1960; Cummings and others, 1962; Nilsen and Simoni, 1973; Nelson and Nilsen, 1974).

(3)	The San Lorenzo Formation, which is 1,720-3,000 ft (525-900 m) thick, of Narizian, Refugian, and Zemor-rian age. It rests conformably on the Butano Sandstone and was divided by Brabb (1964) into two members: the﻿Table 2.—Sedimentary structuresandfeaturesreportedfrominferreddeep-seafandepositsof the early Tertiary continental borderland and adjacent areas of California

[x = reported in literature; R = rare; C = common]

8

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

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NORTHWESTERN AREA

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[See text for sources of nomenclature and data. Provincial benthonic foraminiferal stages from Kleinpell (1938) and Mallory (1959).~^unconformable contact;-conformable contact; -nature of contact unknown;

? position of contact in stage uncertain]

10

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

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<	uoijbuiioj opoq  JO J9qUJ3JV 9UO}SpUBS BHJUB3 ‘B9IB SOjp9flBA						4,500'	J			
as  <  Z  as  w	(8361)  apuoips PUB II9}J JO 9UOJSPUBS SOUIJ S9IJ B9IB >|IBJ OpB|Og						o  o  OS				
m  <  w  X  H  as	(£i6I)  “!W*n»T>W ‘(££61) nsuusg ‘(0161) re)«D ‘(0Z.6I) nagnsag jo sauojspuBS ‘boib osof ubs	r			3,750'-  4,000'			j			
Z	sjjnBj sBgjpuy ubs PUB SOjpiBJIJ U99A\J9q 9UOJSpUBS ‘B9JB 9SOf UBS							i  L	1,200'-  1,700'	i  	I	
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2  u	SJlUn P9UIBUUQ 9§UE3 9jpBJ\ BJJ9IS	)			16,000'-  20,000'			T			
u  hJ  aa  Z  <	SJIUn P9UIBUUQ  S9SUB3 bzubj bj puB Bpnq bjubs uiaqjnos				}			20,000'		{	
<  in  <	(1^61) dmoqi jo auojspuBS sapotf aqi 93ub3 Bpnq bjubs uiaqjiON		o  o	1,450'	J.						
as  <  Z  as  w	(BJ96I) U9MOg JO UOIJBUIIOJ 0I9UIJB3  soqoq juioj							f	o  o  00	“1  J	
in  W  £  X  H	ouojspuBS ouBjng suiBjunoj^ zni3 bjubs		{		5,000'  (possibly  10,000')			*  ?			
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Narizian	Ulatisian	Penutian	Bulitian	Ynezian	Cretaceous
S9SBJS JBJ9JIUIUIBJOJ JBpUIAOJJ					﻿NORTHWESTERN AREA

11

Twobar Shale Member, 650-790 ft (200-240 m) thick, of Narizian age, and the overlying Rices Mudstone Member, 1,030-1,700 ft (310-520 m) thick, of Refugian and Zemorrian age (Brabb, 1960, 1964; Cummings and others, 1962; Clark, 1966, 1968; Smith, 1971). The Twobar Shale Member is a hemipelagic shale deposited at lower bathyal or abyssal depths in a basin with unrestricted access to the open ocean. The Rices Mudstone Member was deposited at bathyal to neritic depths in a [ basin with restricted access to the ocean (Brabb, 1964).

SAN JUAN BAUTISTA AREA ^

Strata of Eocene to Miocene age crop out south and east of San Juan Bautista; they rest unconformably on mafic crystalline basement rocks to the north and are in fault contact with granitic basement rocks to the south (Allen, 1946; Ross, 1970, 1972; Clark and Reitman, 1973).The lower unit of this sequence, the San Juan Bautista Formation of Kerr and Schenck (1925), is of Penutian or Ulatisian to Zemorrian age. The lower part of this formation consists of foraminiferal siltstone 600 ft (180 m) thick that was deposited at bathyal depths. It is overlain by fine-grained sandstone and siltstone 1,200 ft (370 m) thick that contains molluscan and foraminiferal fossils indicative of deposition in shallow marine conditions (Castro, 1967). The foraminiferal faunas near the base of the sequence indicate a Penutian or Ulatisian age and those 1,250 ft (390 m) above the base indicate a Refugian age (Castro, 1967; Waters, 1968; Clark and Reitman, 1973).

POINT LOBOS

A sequence of marine conglomerate, sandstone, siltstone and shale of the Paleocene Carmelo Formation of Bowen (1965a) crops out in a small area broken by numerous faults near Point Lobos at the northwest end of the Santa Lucia Range. The sequence is probably as much as 800 ft (240 m) thick, although the thickest continuous section measures only 725 ft (220 m) (Bowen, 1965a, b). The sequence rests unconformably on porphyritic biotite granodiorite; the upper contact is not exposed. Scattered mollusks, foraminifers and plant remains indicate a Paleocene age. The conglomerate clasts are composed primarily of andesite, rhyolite, granodiorite, chert, and quartz; the sandstones are feldspathic. Paleocurrents are variable but suggest a source area to the east (Nili-Esfahani, 1965). Nili-Esfahani (1965) and Bowen (1965a) suggested that deposition was by turbidity currents, subaqueous sliding and slumping, and traction currents on a submarine fan.	NORTHERN SANTA LUCIA RANGE ~ ^7^1

Lower Tertiary strata in the Church Creek area of the northern Santa Lucia Range consist of (1) Paleocene conglomerate, sandstone, siltstone, and mudstone at

least 750 ft (230 m) thick resting unconformably on granitic and metamorphic basement rocks with the upper contact eroded; (2) the Junipero Sandstone of Thorup (1941), 0-150 ft (0-45 m) thick of Penutian age, also resting unconformably on basement rocks; (3) the Ulatisian Lucia Mudstone of Dickinson (1965), 0-250 ft (0-75 m) thick, resting either conformably on the Junipero Sandstone or unconformably on basement rocks; (4) The Rocks Sandstone of Thorup (1941), 400-800 ft (120-240 m) thick of Ulatisian and Narizian age, resting either conformably on the Lucia Mudstone or unconformably on basement rocks; and (5) the Church Creek Formation, 1,250-1,500 ft (390-450 m) thick of Refugian age, consisting of conglomerate, sandstone, siltstone, and mudstone that rest conformably on The Rocks Sandstone (Herold, 1936; Wardle, 1957; Masters, 1962; Waters, 1963; Dickinson, 1965; Kleinpell and others, 1967; Brabb and others, 1971).

In the Reliz Canyon area farther to the southeast, the conformable lower Tertiary sequence has been divided by Durham (1963, 1964, 1965, 1974) into (1) the Reliz Canyon Formation (Eocene), which he subdivided into three unnamed members: (a) conglomerate and sandstone (the Junipero Sandstone of Thorup, 1941), 180 ft (55 m) thick, probably Penutian and resting unconformably on basement rocks; (b) massive siltstone with thin sandstone beds near the top (the Lucia Shale of Thorup, 1941), 150-350 ft (45-110 m) thick and Ulatisian ; and (c) thickly bedded sandstone (The Rocks Sandstone of Thorup, 1941), 1,450 ft (440 m) thick and probably Narizian; and (2) the Berry Formation, nonmarine conglomerate and sandstone 650-1,100 ft (200-340 m) thick, probably Refugian and Zemorrian and possibly disconformably overlying the upper sandstone member of the Reliz Canyon Formation (Thorup, 1941, 1943; Durham, 1963, 1974).

The Paleocene rocks in the Church Creek area grade upward from thickly bedded feldspathic sandstone and conglomerate containing primarily plutonic clasts to thinly interbedded sandstone and mudstone (Dickinson, 1965). The massive and cross-stratified Junipero Sandstone includes conglomerate lenses and some bio-clastic limestone; its sandstones—arkosic arenites containing more potassium feldspar than plagioclase feldspar—are inferred to be shallow marine deposits (Dickinson, 1965). The Lucia Mudstone, which contains abundant pelagic foraminifers, was probably deposited in quiet waters having unrestricted access to the open ocean. Dickinson (1965) interpreted the Junipero-Lucia sequence as representing a marine transgression from east to west.

The Rocks Sandstone consists of massive sandstone beds from 2 to 15 ft (0.6-4.6 m) thick that are separated by thin mudstone layers; it increases in grain size and﻿12

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

bedding thickness toward the southeast (Link, 1975). Compositionally it is arkosic arenite, with three to five times as much potassium feldspar as plagioclase feldspar and conglomerate clasts composed of granite, quartzite, volcanic rocks, amphibolite, schist, and gneiss (Dickinson, 1965). Although some sandstones near the base of The Rocks Sandstone have been interpreted by Dickinson (1965) as shallow marine deposits, the unit has many sedimentary features in common with inferred deep-sea fan deposits of the Salinian block (table 2). Link (1975) concluded that it had been deposited as a submarine-fan complex by turbidity currents, fluidized sediment flows, and grain flows that transported sediments northwestward into a moderately deep basin. Nannoplankton from the overlying Church Creek Formation suggest deposition at outer-shelf or slope depths (Brabb and others, 1971); sandstones in The Rocks are arkosic arenites with four to six times as much potassium feldspar as plagioclase feldspar (Dickinson, 1965). Eastward, The Rocks Sandstone may grade laterally into nonmarine conglomerate of the Berry Formation (Dickinson, 1965).

ADELAIDA AREA

Taliaferro (1944, p. 513) assigned Paleocene sedimentary rocks in two small areas north of Adelaida to the Dip Creek Formation; he concluded that the 1,320-ft-thick (400 m) sequence rests unconformably on similar Upper Cretaceous rocks and is overlain unconformably by Oligocene or Miocene nonmarine sedimentary rocks. Durham (1968, 1974) includes these strata in an unnamed formation of Late Cretaceous and Paleocene age, does not recognize any unconformities within the sequence, and concludes that they are over-lain unconformably by Oligocene or Miocene nonmarine sedimentary rocks. The Paleocene part of the sequence consists primarily of sandstone with some conglomerate, siltstone, and mudstone. Molluscan faunas of "Martinez” age indicate that deposition occurred in a shallow, inner neritic marine environment; however, foraminiferal faunas indicate deposition in outer neritic or deeper environments (Durham, 1974).

LA PANZA, SOUTHERN SANTA LUCIA, AND SIERRA MADRE

RANGES

A continuous Upper Cretaceous to Ulatisian (?) sequence of strata about 20,000 ft (6,000 m) thick crops out in the southern Santa Lucia and La Panza Ranges. The sequence has been informally divided in ascending order into conglomerate, sandstone, shale, and sandstone units. It rests unconformably on granitic basement rocks and is overlain unconformably by Miocene(?) sedimentary rocks. Thick sequences of Penutian to Narizian strata crop out in the Sierra Madre Range to the south, a dominantly sandstone and

conglomerate sequence about 16,000 ft (4,900 m) thick in the northern part, and a dominantly shale and sandstone sequence more than 20,000 ft (6,000 m) thick in the southern part. The base of these sequences is not exposed; they are overlain unconformably by Oligocene and Miocene strata (Hill and others, 1958; Gower and others, 1966; Vedder and others, 1967; Vedder, 1968; Vedder and Brown, 1968). Stratigraphic units have not been formally named, ages are only approximately known, and correlations between the three ranges have not been well established to date. Sage (1973) classified Paleocene sandstone in the northern La Panza Range as arkose, with more potassium feldspar than plagioclase feldspar; he also identified conglomerate clasts composed of granite, rhyolite, andesite, gneiss, quartzite, and quartz.

Chipping (1969, 1970a, b, 1972a) inferred that these rocks were deposited in a single large basin which he called the Sierra Madre basin. He determined southward-directed paleocurrents in the lowest part of the sequence in the southern Santa Lucia and La Panza Ranges, northward-directed paleocurrents in the uppermost part of the sequence in the Sierra Madre Range, and westward- and northwestward-directed paleocurrents in the other parts of the sequence in each range. He inferred that source areas were located to the north, east, and south, and that the basin shoaled eastward. Deposition was inferred to have been by turbidity currents, grain flows, and gravity slumping and sliding on a submarine fan. The basin was deepest during the Penutian and Ulatisian Stages. Sage (1973) also determined southward-directed paleocurrents from Paleocene strata in the northernmost lower Tertiary outcrops in the La Panza Range. Both he and Chipping (1972a) concluded that these rocks were deposited in very nearshore or nonmarine environments, probably at the northern edge of the Sierra Madre basin. Chipping further concluded that during most of its depositional history the Sierra Madre basin was separated from the Santa Ynez basin to the south except during Ulatisian time, when they were connected by a seaway in the east.

PATTI WAY RIDGE AREA - ” '	4

Lower Tertiary rocks crop out in the southeastern Caliente Range and along Patti way Ridge about five miles (8 km) to the southeast. Paleocene molluscan and P Ynezian foraminiferal faunas have been reported from the Pattiway Formation in the Caliente Range (Hill and J others, 1958; Vedder and Repenning, 1965; Vedder, 1970a). Although the age of the rocks along Pattiway Ridge is uncertain, they have been lithologically correlated with the Pattiway Formation by Sierveld (1957) and Van Amringe (1957). Basal contacts are not exposed in either area; both sequences are overlain uncon- ~j formably by nonmarine sedimentary rocks of probable﻿NORTHEASTERN AREA	13

j_01igocene age. The Caliente Range deposits consist of interbedded conglomerate, sandstone, siltstone, and shale as much as 3,500 ft (1,100 m) thick; the Pattiway Ridge deposits consist of 800 ft (240 m) of fine-grained to pebbly sandstone with subordinate amounts of shale and siltstone (Sage, 1973). The sandstone in both areas is arkosic in composition, containing more potassium feldspar than plagioclase feldspar, with minor amounts of biotite and lithic fragments that include granitic, metamorphic, volcanic, and quartzitic rocks; the conglomerate clasts include granite, rhyolite, andesite, gneiss, quartzite, and quartz (Sage, 1973). On the basis of paleocurrent measurements and sedimentological analyses, Sage (1973) inferred that (1) the Caliente Range sequence was derived from a source area underlain by volcanic, granitic, and gneissic rock located to the north-northwest, and was deposited as a relatively shallow submarine fan built out to the south-southwest;

(2)	the Pattiway Ridge sequence was derived from a source area underlain by granitic and metamorphic rocks to the north, and was deposited as proximal turbidites in a south- or southeast-trending basin.

MOUNT PINOS AREA

Unnamed Eocene strata about 2,200 ft (670 m) thick crop out in a narrow fault wedge along the south flank of Mount Pinos and locally rest unconformably on granitic basement rocks (Carman, 1964). The strata consist primarily of shale but include limestone, siltstone, mudstone, thinly bedded arkosic sandstone, and pebble conglomerate containing granite, chert, mudstone, siltstone, and silty limestone clasts. The sandstone is about 70 percent quartz, 25 percent feldspar (mostly plagioclase and microcline, but with orthoclase and perthite common), and minor amounts of chlorite, mica, and lithic fragments. Rare molluscan fossils suggest a "Capay” age. Carman (1964) inferred, in the absence of graded bedding and slump structures, that deposition occurred in shallow marine, nearshore environments, but did not indicate the location or orientation of the shoreline.

NORTHEASTERN AREA

A great variety of lower Tertiary sedimentary rocks crop out in this area (figs. 1 and 2). Nonmarine deposits are present in the western foothills of the Sierra Nevada, in subsurface beneath the eastern Great Valley, and in the Tehachapi and El Paso Mountains along the southern edge of the area. Marine deposits are present in the western foothills and southwestern edge of the Sierra Nevada, in subsurface beneath the Great Valley, and in the northern and southern Coast Ranges. Recent studies in the western part of the northern Coast Ranges indicate that the "coastal belt” Franciscan rocks, previously thought to be of Mesozoic age, contain

fossils diagnostic of an early Tertiary age (Berkland and others, 1972, p. 2295).

SIERRA NEVADA	-

Plant fossils from the prevolcanic auriferous gravels of the northwestern Sierra Nevada indicate Eocene and Oligocene ages; the gravels are inferred to have been deposited by large westward- and southwestwardflowing streams; (Lindgren, 1911; MacGinitie, 1941; Bateman and Wahrhaftig, 1966; Wolfe and others, 1961; Dalrymple, 1964; Durrell, 1966; Peterson and others, 1968; Clark, 1970; Yeend, 1974). The gravels are generally less than 50 ft (15 m) thick except along the ancestral Yuba River, where they are 500-600 ft (150-180 m) thick. They typically consist of (1) "blue gravels” in the bottoms of channels which contain clasts of adjacent bedrock types and small amounts of granitic clasts; and (2) overlying "white gravels,” which are mainly quartz, chert, and quartzite clasts. The gravel clasts are generally of pebble and cobble size. Sands associated with the "blue gravels” are arkosic and contain biotite, hornblende, and epidote; sands associated with the "white gravels” contained quartz, anauxite, and biotite, a mineral assemblage commonly attributed to deep chemical weathering in a tropical climate. The uppermost sandstones contain fresh feldspar and biotite indicative of less intense chemical weathering.

Other lower Tertiary nonmarine and marine sedimentary rocks in the westernmost foothills of the Sierra Nevada include (1) the Dry Creek Formation of Allen (1929), which rests unconformably on Cretaceous sedimentary rocks in a small area near Oroville; it is as much as 80 ft (24 m) thick, contains a "Meganos” age megafauna, and consists of interbedded shale and sandstone with abundant feldspar, hornblende, and biotite; and (2) the lone Formation, which is more widespread and possibly as much as 1,000 ft (300 m) thick locally; it rests unconformably on crystalline basement rocks with as much as 1,000 ft (300 m) of local relief or without angular discordance on the Dry Creek Formation (Allen, 1929; Creely, 1965; Bateman and Wahrhaftig, 1966; Durrell, 1966). The lone Formation has been divided informally into (1) a lower member which typically rests on a deeply weathered lateritic surface and includes (a) sandstone as much as 415 ft (125 m) thick and composed of quartz, anauxite, biotite, hornblende, heavy minerals, and little or no feldspar, (b) clay beds composed mostly of kaolinite and halloysite, and (c) lignite beds as much as 24 ft (7.3 m) thick; and (2) an upper member consisting primarily of feldspathic sandstone containing biotite, chlorite, and kaolinite, characterized by cross-strata, gravel lenses, and abundant channels. The upper member rests unconformably on the lower. Locally abundant megafossils indicate a "Capay” age and shallow marine and nonmarine depos-﻿14

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

ition, including deltaic, lagoonal, and fluviatile environments. The unusual composition of the lower member suggests deep chemical weathering in a tropical climate.

Allen (1929) proved that sediments of the lone Formation and the nonmarine prevolcanic gravels were transported and deposited by the same streams, and that the Eocene shoreline lay between the two units. According to Hackel (1966, p. 227), the late Eocene lone Formation grades laterally northward into the nonmarine Butte Gravel Member of the Sutter Formation, which overlies granitic rocks along the northeastern edge of the Great Valley. A possible nonmarine partial equivalent of the lone in the southeastern Great Valley is the Walker Formation, which is poorly dated but may contain strata as old as Paleocene or Eocene in its lower part and early Miocene in its upper part. It is thought to have been deposited by westward-flowing streams and may be partly equivalent to the prevolcanic gravels of the northern Sierra Nevada (Hackel, 1966).

FRANCISCAN ASSEMBLAGE IN THE ^ t*'* NORTHERN COAST RANGES

Although the Franciscan assemblage has traditionally been considered to be of Mesozoic age, probably Late Jurassic to Late Cretaceous (Irwin, 1957; Bailey and others, 1964), recently discovered fossils in the northern Coast Ranges indicate that much or most of the "coastal belt,” or westernmost sequence of Franciscan rocks (Bailey and Irwin, 1959), is early Tertiary (Berkland and others, 1972; O’Day and Kramer, 1972). These "coastal belt” rocks consist mostly of interbedded flysch-like sandstone and shale; the sandstones are feldspathic graywackes with more potassium feldspar (4.5 percent average) than other Franciscan rocks and very little chert, greenstone, serpentine, or high-pressure metamorphic rocks (Bailey and others, 1964; Raymond and Christensen, 1971; O’Day, 1974).

The "coastal belt” sequence contains zones with disturbed and broken bedding (melanges) and also pebbly mudstone (Kleist, 1974); it contains large exotic blocks of sandstone, limestone and volcanic rocks, but almost no blocks of the high pressure-low temperature metamorphic rocks characteristic of older Franciscan strata.

Sedimentary features of the "coastal belt” rocks indicate deposition by turbidity currents, debris flows and grain flows; the chaotically bedded zones probably indicate submarine slumping and gravity sliding (Chipping, 1971; Kleist, 1974). The "coastal belt” rocks probably are a complex comprising deep-sea fans deposited on the floor of an elongate offshore trench, and gravity-slide and debris-flow materials deposited on the lower slopes of the trench.

In addition to the lower Tertiary "coastal belt” sequence, lower Tertiary strata are also preserved on

some outliers of Great Valley sequence rocks that are thought to have been thrust westward over the Franciscan assemblage along an active subduction zone; these relations suggest that subduction along the offshore trench in which the "coastal belt” rocks were probably deposited continued into the early Tertiary in the northern Coast Ranges (Berkland, 1969, 1971, 1972, 1973). There is little evidence in the early Tertiary stratigraphic record of central and southern California, however, for continued subduction; rocks of the Franciscan assemblage and the Catalina Schist in these areas seem to be restricted in age entirely to the Mesozoic (Page, 1970b).

% ROUND VALLEY AREA

A sequence of lower Tertiary strata up to 2,000 ft (600 m) thick disconformably overlies Cretaceous rocks in a large klippe that rests on Franciscan rocks southwest of Covelo in Round Valley. The klippe, like others in the Middle Mountain, Rice Valley, and Clear Lake areas, is inferred to be part of a thrust sheet detached from the main outcrop belt of Mesozoic and lower Tertiary sedimentary rocks along the west side of the Sacramento Valley and thrust westward, without significant rotation, over the Franciscan assemblage (Swe and Dickinson, 1970). Clarke (1940) divided this sequence into (1) the Martinez Formation, fine-grained sandstone about 130 ft (40 m) thick containing biotite, muscovite, chert, shale chips, and carbonaceous material, that locally has asymmetrical ripple marks; (2) the Meganos Formation, carbonaceous sandstone about 300 ft (90 m) thick that locally contains conglomerate composed of shale, quartz, and dacite or rhyolite clasts; and

(3)	the Capay Formation, dark shale and fine sandstone about 1,500 ft (450 m) thick with fragments of chert, slate? shale, and volcanic rocks and a heavy mineral assemblage consisting principally of epidote, garnet, ilmenite-leucoxene, titanite, magnetite, tourmaline, and clinozoisite-zoisite. The contacts between these units are apparently conformable although poorly exposed. Clarke (1940) noted shallow marine molluscan faunas of Paleocene age in the Martinez and Meganos Formations and of "Capay” age in the Capay Formation.

'	1	RICE VALLEY AREA

Lower Tertiary marine sedimentary rocks more than 1,150 ft (350 m) thick unconformably overlie Cretaceous marine sedimentary strata in a small, synclinally folded klippe of Great Valley sequence rocks that rest on Franciscan rocks near Rice Valley (Berkland, 1971, 1973). The lower Tertiary sequence consists of (1) unfos-siliferous, cross-stratified sandstone 200 ft (60 m) thick,

(2)	unfossiliferous pebble conglomerate 150 ft (45 m) thick that is more than 60 percent clasts of Franciscan rock types, (3) unfossiliferous quartz grit 150 ft (45 m)﻿NORTHEASTERN AREA

15

thick with minor coal seams, (4) calcareous sandstone 150 ft (45 m) thick containing a "Meganos” molluscan fauna indicative of deposition in shallow marine conditions, and (5) glauconitic sandstone and greenish silt-stone 500 ft (150 m) thick that contains a sparse molluscan fauna questionably assigned to the "Capay” stage. The entire sequence is overlain unconformably by Quaternary sediments. The abundant Franciscan detritus in the second unit indicates rapid, local uplift of Franciscan blueschists in the early Tertiary (Berkland, 1973).

MIDDLE MOUNTAIN AREA

Lower Paleocene sandstones are reported to conformably overlie the Great Valley sequence in a klippe that rests on Franciscan rocks near Middle Mountain (Berk-land, 1969,1972). However, detailed stratigraphic data have not been published to date.

CLEAR LAKE AREA	- n '*

A conformable sequence of lower Tertiary sedimentary rocks about 5,500 ft (1,700 m) thick is faulted against (but may locally be in depositional contact with) the Great Valley sequence in a large imbricated klippe near Clear Lake (Swe and Dickinson, 1970). The lower Tertiary sequence is overlain by Quaternary volcanic and sedimentary rocks. Brice (1953) divided the lower Tertiary sequence into (1) the Paleocene Martinez Formation, 2,200-4,200 ft (670-1,300 m) thick, subdivided into (a) a lower fine- to medium-grained, thickly bedded, massive arkosic wacke unit 1,400 ft (430 m) thick containing moderate amounts of chert and a heavy mineral assemblage of tourmaline, zircon, epidote, hypersthene, garnet, rutile, brookite, clinozoisite, and staurolite; (b) a middle feldspathic sandstone 700 ft (210 m) thick with thick lenses of pebble and cobble conglomerate composed of rounded clasts of dark chert, quartzite, and fine-grained porphyritic igneous rocks; (c) an upper fossiliferous well-bedded, silty shale 2,150 ft (660 m) thick containing some interbedded sandstone in the lower part and inferred to have been deposited in warm, quiet, shallow marine conditions; and (2) the Eocene Tejon Formation, about 1,000 ft (300 m) thick, consisting of locally fossiliferous medium-grained arkosic to lithic wacke containing a heavy mineral assemblage similar to the underlying Martinez Formation, and beds and lenses of granule and cobble conglomerate of dark chert, quartz, and volcanic rock clasts. The Tejon is inferred to have been deposited in shallow marine to continental conditions. Clark and Vokes (1936) assigned the youngest strata, mistakenly referred to the Tejon Formation by Brice (1953), to the "Meganos” stage on the basis of molluscan fauna.

MOUNT DIABLO AREA AND SACRAMENTO VALLEY AREA

Lower Tertiary marine sedimentary rocks more than

9,000	ft (2,750 m) thick crop out in the Mount Diablo area where they have been mapped as the Martinez Formation, Meganos Formation, Capay Formation, Domengine Sandstone, Nortonville Shale Member of the Kreyenhagen Formation, and the Markley Formation. This sequence unconformably overlies Upper Cretaceous sedimentary rocks and is unconformably over-lain by Oligocene and Miocene sedimentary rocks (Colburn, 1961; 1964). Major unconformities within the sequence are present at the base of the Domengine Sandstone on the north flank of Mount Diablo (Colburn, 1961) and at the base of the Capay Formation farther north in the Sacramento Valley (Pacific Section, American Association of Petroleum Geologists, 1960; Lachen-bruch, 1962; Safonov, 1962). A related lower Tertiary sequence in the Pacheco syncline area to the west has been described by Weaver (1953) and Smith (1957).

The Ynezian Martinez Formation is 900-1,000 ft (270-300 m) thick on the north flank of Mount Diablo but absent on the south flank. The lower half is poorly bedded, medium- to coarse-grained, locally pebbly sandstone with a thin fossiliferous basal conglomerate of limestone pebbles and cobbles apparently derived from the underlying Cretaceous rocks. The upper half is massive mudstone and siltstone (Colburn, 1961; Berry, 1964).

The Bulitian Meganos Formation is more than 4,000 ft (1,200 m) thick on the north flank of Mount Diablo (Mallory, 1959; Colburn, 1961; Berry, 1964). The base is marked by a 20- to 50-ft-thick (6-15 m) conglomerate (member A) that contains angular boulders of sandstone and limestone up to 1 ft (30 cm) long, and rounded pebbles and cobbles of chert, quartzite, and vein quartz (Colburn, 1961). The remainder of the Meganos consists of thick alternating sandstone and shale units, with sandstone predominating in the lower and upper parts (members B, C, and D of Clark and Woodford, 1927 and Colburn, 1961). A 20-ft-thick (6 m) bed in the upper part of the formation contains abundant thick-shelled mol-lusks, thin beds of orbitoidal limestone, and, toward the east, thin lignite seams (Colburn, 1961). The composition and heavy mineralogy of upper Meganos sandstones suggest a source area of felsic plutonic rocks (Clark and Woodford, 1927). Colburn (1961, 1964) inferred that the Martinez and Meganos Formations were deposited in shallow marine conditions during a southward transgression onto an area of low relief.

Both the Martinez and Meganos Formations extend northward in subsurface for about 60 miles (100 km) beneath the Sacramento Valley, where they conformably overlie Upper Cretaceous strata; farther north and east they are truncated by pre-middle Eocene unconformities (Pacific Section, American Association of Petroleum Geologists, 1951,1960; Safonov, 1962; Lachen-bruch, 1962; Hackel, 1966). Abrupt lateral facies﻿16

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

changes from sandstone to siltstone in the Meganos about 25 miles (40 km) northeast of Mount Diablo have been interpreted by Safonov (1962) as the result of deltaic sedimentation, by Silcox (1962) as siltstone-filled channels cut into sandstone, and by Fischer (1971) as submarine canyon and fan deposits. In any case, the distribution of sandstones in the Meganos indicates that they were transported southwestward and apparently derived from the Sierran landmass. The combined thickness of the Martinez and Meganos Formations increases abruptly from about 2,000 ft (600 m) to nearly

3,500	ft (1,100 m) westward across the Midland fault zone (fig. 2), which is downthrown to the west, indicating early Tertiary movement of the fault (Pacific Section, American Association of Petroleum Geologists, 1951).

Strata referred to the Capay Formation, the Meganos E shale, or the Marysville Claystone Member of the Meganos Formation, of Penutian to Ulatisian age, are about 700 ft (210 m) thick on the north flank of Mount Diablo (Berry, 1964; Johnson, 1964). They extend north of Mount Diablo as far as 130 miles (210 km) into the northern Sacramento Valley as a 200- to 300-ft-thick (60-90 m) blanket of glauconitic siltstone and claystone that unconformably overlies Paleocene and older rocks (Pacific Section, American Association of Petroleum Geologists, 1951,1960). Sandstone and conglomerate to the north and east suggest source areas in those directions (Safonov, 1962). To the northwest beneath the Sacramento Valley, shales of the Capay Formation are truncated by the "Capay” or "Princeton” gorge, a north-south-trending erosional feature that has been interpreted as a submarine canyon cut into Cretaceous strata and filled by 2,000 ft (600 m) or more of sediments of "Capay” age (Pacific Section, American Association of Petroleum Geologists, 1960; Safonov, 1962; Redwine, 1972). The deposits filling this postulated submarine canyon are sparsely fossiliferous silty to sandy mudstones with some interbedded sandstone and conglomerate (Hackel, 1966). The original type section of the Capay Formation in Capay Valley may represent canyon-fill deposits; Stewart (1949) reported that molluscan fossils in this section are abraded and larger than those from the underlying mudstones, and suggested that they were transported from shallow marine environments.

The Capay Formation contains various fossils suggestive of moderate depths and stagnant bottom conditions (Stewart, 1949) and records the greatest extent of the marine transgression begun earlier in "Meganos” time. The formation thickens abruptly west of the Midland fault zone, indicating that vertical displacement on this fault continued into the Eocene (Pacific Section, American Association of Petroleum Geologists, 1951).

The Domengine Sandstone, of Ulatisian age, is about 800 to 1,200 ft (240-360 m) thick on the north flank of Mount Diablo (Colburn, 1961; Johnson, 1964; Berry, 1964). It consists of a lower member of massive, medium- to coarse-grained, quartzose arenite with interbedded coal seams, a middle member of silty mudstone and fine sandstone, and an upper member of interbedded mudstone and very thickly bedded, medium-to coarse-grained sandstone (Colburn, 1961). Nearshore deposition in an area of possible low-lying beaches and swamps similar to the modern Florida coast is suggested by the presence of thick-shelled mollusks, coal, and silicified wood in the lower Domengine; an eastward increase in abundance of coals suggests that a landmass lay in that direction (Colburn, 1961). Shallow marine depositional environments are also indicated by molluscan faunas in the upper Domengine (Colburn, 1961).

The Domengine crops out along the southwestern edge of the Sacramento Valley and extends in subsurface northward from Mount Diablo for about 80 miles (130 km). It records the last major early Tertiary marine transgression of the Sacramento Valley area and deposition in a complex of marginal marine, littoral and sublittoral environments (Pacific Section, American Association of Petroleum Geologists, 1960; Todd and Monroe, 1968). It is about 500 ft (150 m) thick throughout this region and may be partly nonmarine to the north and east, where it partly correlates with the lone Formation of the Sierra Nevada (Safonov, 1962; Pacific Section, American Association of Petroleum Geologists, 1951, 1954, 1960).

The Nortonville Shale Member of the Kreyenhagen Formation, of late Ulatisian and early Narizian age, consists of mudstone with some interbedded sandstone. It is about 500 ft (150 m) thick on the north flank of Mount Diablo, where it is included in the upper part of the Domengine Sandstone by Colburn (1961), and as much as 2,500 ft (760 m) thick on the south flank (Pacific Section, American Association of Petroleum Geologists, 1960; Johnson, 1964; Berry, 1964). It extends in subsurface northward from the Mount Diablo area for about 45 miles (72 km) beneath the Sacramento Valley; along its northern and eastern margins it is truncated by a post-Eocene unconformity (Johnson, 1964; Pacific Section, American Association of Petroleum Geologists, 1951 and 1960). The Nortonville "represents a deepening water phase of the Domengine transgression” (Johnson, 1964), and is similar in age, lithology and faunal content to the lower part of the Kreyenhagen Formation of the San Joaquin Valley (Fulmer, 1964). It contains some volcanic ash northeast of Mount Diablo (Safonov, 1962).

The Narizian Markley Sandstone Member of the﻿NORTHEASTERN AREA

17

Kreyenhagen Formation is as much as 4,500 ft (1,400 m) thick on the north flank of Mount Diablo, where it is a massive, medium- to coarse-grained sandstone with £,_some interbedded thin shale (Stewart, 1949; Colburn, 1961; Berry, 1964; Mallory, 1959). Thick sections are also present farther north in the Vacaville area (Bailey, 1930; Day, 1951; Weaver, 1953). However, it is absent on the south flank of Mount Diablo. The sandstones are arkosic, with 50-65 percent quartz, 10-25 percent potassium feldspar, 5-25 percent plagioclase feldspar, and minor biotite, muscovite, and glauconite; heavy minerals include much green hornblende, tremolite-actinolite, and epidote, lesser amounts of garnet, sphene, zircon, and tourmaline, and small amounts of glaucophane and andalusite (Morris, 1962). Paleocur-rent directions from outcrops in the Mount Diablo area indicate transport of sediment to the west. Foramini-feral faunas from the lower part of the Markley in the Vacaville area indicate deposition at bathyal or greater depths and in a basin connected to the open ocean; faunas from the 700-ft-thick (210 m) late Narizian Sidney Shale Member of the Markley Formation of Clark and Campbell (1942) on the north flank of Mount Diablo indicate deposition at neritic to mid-bathyal depths (Mallory, 1959).

<T The Markley Sandstone Member extends in subsurface northward into the Sacramento Valley where it is truncated on the north and east by a post-Eocene unconformity (Pacific Section, American Association of Petroleum Geologists, 1951 and 1960). An eastern Sierran source for the Markley is indicated by paleocurrent directions, sandstone composition, and the eastward transition from deep marine to shallow marine and nonmarine depositional environments (Safonov, 1962). The "Markley gorge,” which extends in subsurface from north of Sacramento southwestward for 60 miles (100 km) to the vicinity of Rio Vista, may be an early Tertiary submarine canyon; it is cut as deeply as 1,200 ft (370 m) into Upper Cretaceous to lower Eocene shale and is filled with upper Eocene and Oligocene shale, sandstone, and conglomerate (Safonov, 1962; Almgren and Schlax, 1957).

SAN LEANDRO HILLS

Lower Tertiary marine sedimentary strata about

1,500	ft (450 m) thick crop out in a small area of the San Leandro and Berkeley Hills near Oakland. The sequence consists of (1) the Pinehurst Shale of Ynezian age, about 500 ft (150 m) of interbedded siliceous shale and thinly bedded sandstone that contain abundant radiolarians and sparse foraminifers; and (2) unnamed Eocene strata of Ynezian to "Domengine”(?) age, about

1,000	ft (300 m) of glauconitic sandstone with subordinate shale, conglomerate, and fossiliferous limestone


iU>

(Case, 1963, 1968). The Pinehurst Shale rests conformably on Upper Cretaceous marine shales. The unnamed Eocene strata are not found in contact with the Pinehurst Shale and are either in faulted contact with or unconformably overlain by Miocene marine sedimentary rocks.

SAN JOSE AREA


Lower Tertiary marine sedimentary rocks crop out in separate areas located east of the San Andreas and Pilarcitos faults in the general vicinity of San Jose. They have not been studied in great detail in this structurally complex area and their stratigraphic relations to one another are not known. Relatively thick sequences of sandstone that were probably deposited in deep marine environments and resemble the type Butano Sandstone of the Santa Cruz Mountains have been mapped and named the Butano or Butano(?) Sandstone by workers in this area. However, these sandstones overlie Franciscan rocks, and it is probable that they were originally deposited well over one hundred miles (300 km) southeast of the type Butano Sandstone and reached their present position by large amounts of right-lateral slip along the nearby San Andreas fault.

The lower Tertiary strata that crop out between the Pilarcitos and San Andreas faults about 30 miles (48 km) northwest of San Jose are 1,200-1,700 ft (360-520 m) thick and have been mapped as Butano Sandstone by Esser (1958), Mack (1959), Burtner (1959), and Brabb and Pampeyan (1972). These strata rest unconformably on the Franciscan assemblage and are overlain unconformably by Miocene marine sedimentary rocks. They are mostly thickly bedded, internally structureless, fine- to coarse-grained arkosic sandstone with some interbedded thin- to medium-bedded fine-grained sandstone, siltstone, shale, and locally abundant pebble conglomerate. A basal conglomerate contains angular fragments of Franciscan graywacke and diabase (Burtner, 1959). The sandstone is 40-50 percent quartz, 20-25 percent plagioclase feldspar, 5 percent potassium feldspar, and smaller amounts of biotite, muscovite, glaucophane, zircon, sphene, and other heavy minerals (Mack, 1959). Pebble clasts are primarily volcanic rocks and chert, with very small amounts of quartzite (Mack, 1959). Foraminiferal faunas indicate an Ynezian or Bulitian age for at least part of the sequence and deposition at depths greater than 600 ft (180 m) in a basin with access to the open ocean (Esser, 1958). Deposition by turbidity currents and slumping was inferred by Esser (1958) and Mack (1959).

Lower Tertiary strata about 4,000 ft (1,200 m) thick that crop out east of the San Andreas fault about 20 miles (32 km) northwest of San Jose and west of Palo Alto have been mapped as the Butano(?) Sandstone by﻿18

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Dibblee (1966c) and Brabb and Pampeyan (1972), as unnamed Eocene sandstones by Page and Tabor (1967), and as informally named sandstones by Beaulieu

(1970). These strata rest unconformably on the Franciscan assemblage and are unconformably overlain by Miocene sedimentary rocks. Planktonic foraminiferal faunas indicate a late Paleocene to late Eocene age for these rocks and benthonic foraminiferal faunas indicate a Penutian to Narizian age (Graham and Classen, 1955; Graham, 1967; Page and Tabor, 1967; Clark, 1968; Beaulieu, 1970). The sequence consists mostly of inter-bedded arkosic sandstone, siltstone, and mudstone with locally abundant conglomerate lenses. A basal breccia and conglomerate that contains fragments of Franciscan graywacke up to 15 ft (4.5 m) long is locally present. Chaotically bedded zones are abundant throughout the rocks; they consist of large blocks of sandstone set in a sheared mudstone matrix and are probably of both tectonic and synsedimentary origin (Page and Tabor, 1967; Beaulieu, 1970). The sandstone composition averages 55 percent quartz, 25 percent plagioclase feldspar, 17 percent potassium feldspar, and lesser amounts of mica, glauconite, and heavy minerals such as zircon, tourmaline, staurolite, anatase, sphene, and garnet. Chert accounts for about half of the conglomerate clasts, the remainder being quartzite and volcanic rocks. Beaulieu (1970) concluded that the basal breccia and conglomerate were deposited at neritic depths, after which the basin subsided rapidly and the overlying sandstone, siltstone, and mudstone were deposited at upper to lower bathyal depths by turbidity currents. He also determined southward-directed paleocurrents and suggested that the source area consisted primarily of the granitic and metamorphic rocks of the Sierra Nevada to the east. A Sierran rather than a Salinian block source was also inferred by Tieh (1965, 1973), on the basis of the abundance of staurolite in the heavy mineral suite.

Lower Tertiary rocks also crop out southwest of San Jose in the southern Santa Cruz Mountains and have been mapped and described by Bauer (1971), McLaughlin, Simoni, Osbun, and Bauer (1971), McLaughlin (1973), Dibblee (1973a), and Simoni (1974). This sequence comprises (1) a lower shale and mudstone unit that contains some interbedded sandstone and a conglomeratic sandstone near the base, of Late Cretaceous to middle Eocene age and 170-1,800 ft (50-550 m) thick, and (2) an upper sandstone unit, mapped as the Butano(?) Sandstone by Bauer (1971), probably of middle and late Eocene age and 1,300-1,800 ft (400-550 m) thick. The sandstones are fine- to coarse-grained and thin- to thick-bedded, but become more massive higher up in the sequence; they are arkosic, about 55-65 percent quartz, 18-25 percent

potassium feldspar, 15-20 percent plagioclase feldspar, 5 percent rock fragments, primarily chert, siltstone, schist, and quartzite, and minor amounts of apatite, magnetite, and biotite (Bauer, 1971; McLaughlin, 1973; Simoni, 1974; E. Osbun, written commun., September 1973). McLaughlin (1973) concluded that the lower unit had been deposited at bathyal depths in a basin with unrestricted access to the ocean, and that the upper unit had been deposited at outer neritic to bathyal depths in part by turbidity currents. Farther east in this area, Bailey and Everhart (1964) described a lower middle Eocene sequence in the Santa Teresa Hills that consists of shale and overlying sandstone containing scattered lenses of fossiliferous limestone.

Lower Tertiary marine sedimentary rocks that crop out along the western edge of the Diablo Range about 15 miles (23 km) southeast of San Jose have been described by Gilbert (1943), Ortalda (1950), Frames (1955), Carter (1970), Bennett (1972), and Dibblee (1973b). They rest both conformably or unconformably on similar Upper Cretaceous marine sedimentary rocks and are overlain unconformably by Miocene marine sedimentary rocks. Carter (1970) determined a maximum thickness of about 6,600 ft (2,000 m) for these strata and divided the sequence into (1) a sandstone unit 600 ft (180 m) thick of Paleocene(?) age; (2) a mudstone unit 2,300 ft (700 m) thick of Paleocene age; and (3) a thinly interbedded sandstone, siltstone, and shale unit that contains some interbedded massive arkosic sandstone and a basal conglomeratic sandstone, 3,750 ft (1,150 m) thick and of Eocene age. The sandstones are 35-60 percent quartz, 15-25 percent potassium feldspar, 1-10 percent plagioclase feldspar, 5-15 percent chert; less than 5 percent volcanic, schistose, and shale rock fragments; minor amounts of mica, sphene, epidote, garnet, zircon, and chlorite; and locally large amounts of glauconite (Carter, 1970; Bennett, 1972). Conglomerate clasts are primarily chert, porphyritic volcanic rocks, granitic and metamorphic rocks, sandstone, siltstone, limestone, and shale (Carter, 1970). The sequence is apparently incomplete in adjacent areas and different ages, thicknesses, and informal names have been assigned to it by other workers. Carter (1970) determined northwestward-directed paleocurrents from flute casts and primary current lineations. Bennett (1972) inferred that most of the sequence was deposited in deep marine environments with access to the open ocean, although some of the basal conglomeratic sandstones may have been deposited in shallow marine environments.	I

TESLA AREA	•****.

The Tesla Formation, which is as much as 2,000 ft (600 m) thick, crops out along the northeastern flank of﻿NORTHEASTERN AREA

19

the Diablo Range near Tesla. In this area, it is of Paleocene to lower Eocene ("Capay” age, unconform-ably overlies Upper Cretaceous marine strata and is unconformably overlain by Miocene strata (Huey, 1948). The Tesla is a heterogeneous assemblage of ar-kosic, quartzose, and anauxitic sandstone, carbonaceous shale and claystone, and lignite seams. The anauxitic sandstones are characteristic of the formation and resemble beach sands in that they are fine to medium grained, well sorted, and crossbedded. These sandstones are 75 percent or more angular quartz, 19-22 percent orthoclase (often kaolinized), up to 3 percent each of oligoclase-andesine and microcline, and traces of chert and biotite (Huey, 1948). Heavy minerals are sparse but include andalusite, zircon, tourmaline, and lesser amounts of staurolite, garnet and several other minerals (Huey, 1948; Morris, 1962).

A Sierran source for the anauxitic sandstones was suggested by Huey (1948) partly on the basis of mineralogical similarities to the lone Formation. Allen (1941) postulated a contemporaneous Franciscan source in the Coast Ranges for interbedded micaceous sandstones that contain fresh biotite, albite, and glau-cophane. The lower part of the Tesla contains brackish-water megafossils, and the upper part shallow-marine megafossils (Huey, 1948). The character of the Tesla sediments and faunas and the absence of the Tesla in outcrops farther north and in subsurface to the east suggest that the early Tertiary basin in the San Joaquin Valley shoaled northward and that basins in the Sacramento and San Joaquin Valley areas were separated from Paleocene to early Eocene time by a structural or topographic high, presumably the Stock-ton arch.

ORESTIMBA AREA

A conformable sequence of lower Tertiary sedimentary rocks crops out for nearly 25 miles (40 km) along the western border of the San Joaquin Valley near Orestimba; it conformably or disconformably overlies Cretaceous marine strata and is unconformably over-lain by Miocene marine strata (Collins, 1949; Booth, 1950; Hacker, 1950). The sequence comprises the Tesla and Kreyenhagen Formations.

The Tesla Formation is carbonaceous siltstone and shale with interbedded fine-grained anauxitic quartzose sandstone (Booth, 1950) containing ripple markings and cross-strata, about 2,300 ft (700 m) thick, of Paleocene to "Domengine” age. Brackish-water megafaunas are present in the lower 1,000 ft (300 m) of the Tesla (Booth, 1950) and shallow-marine magafaunas are present at the top in a greensand of as much as 20 percent glauconite and 70 percent or more quartz (Stewart and others, 1944; Collins, 1949; Booth, 1950).

The Kreyenhagen Formation is a locally carbonaceous shale with some andesitic sandstone in the lower part, 750-1,100 ft (230-340 m) thick and of Narizian age (Collins, 1949). These sandstones also contain zoned plagioclase, hypersthene, augite, and basaltic hornblende, and montmorillonoid-coated volcanic fragments that impart a distinctive blue color (Booth, 1950).

LAGUNA SECA AREA

Lower Tertiary sedimentary rocks about 2,000 ft (600 m) thick crop out for about 11 miles (18 km) along the west flank of the San Joaquin Valley south of Los Banos in the Laguna Seca area. The sequence comprises the Laguna Seca Formation of Payne (1951), the Tesla(?) Formation and the Kreyenhagen Formation, disconformably overlying Upper Cretaceous marine strata and unconformably overlain by Miocene nonmarine strata.

The Laguna Seca Formation of Payne (1951) is shale, siltstone and fine-grained massive micaceous sandstone, about 1,200 ft (370 m) thick, of "Martinez” to "Capay(?)” age (Stewart and others, 1944; Payne, 1951; Briggs, 1953). Deposition in shallow marine environments is indicated by crossbedded and ripple-marked sandstones, abundant molluscan and coralline faunas, glauconite, numerous petrified logs and wood fragments, andPholas borings in sandstone (Briggs, 1953).

The Tesla(?) Formation is a glauconitic quartzose sandstone and soft anauxitic carbonaceous claystone, locally ripple-marked and crossbedded, 50-200 ft (15-60 m) thick and "Capay(?)” to "Domengine(?)” in age (Briggs, 1953). Heavy minerals are sparse and include andalusite, zircon, garnet, epidote, sphene, and tourmaline. Deposition in shallow marine environments and a Sierran source are indicated by the sedimentary structures and sandstone composition. The only fossils are leaf imprints and wood fragments.

The Narizian Kreyenhagen Formation, diatoma-ceous and radiolarian shale with some thin limestone lentils and volcanic ash layers, is about 700 ft (210 m) thick in this area. Glauconitic sandstone and siltstone containing Tesla(?)-like pebbles and cobbles are present near the base of the Kreyenhagen, suggesting that the contact with the Tesla(?) Formation is an unconformity (Briggs, 1953). Deposition of the lower part of the Kreyenhagen in relatively shallow marine environments is suggested by the presence of mollusk burrows and cross bedding; deposition of the upper part in quiet, somewhat deeper marine environments is suggested by the presence of thin and regular bedding (Briggs, 1953).

BOLADO PARK AREA

The lower Tertiary strata that crop out along the west﻿20

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

flank of the Diablo Range near Bolado Park have been mapped by Kerr and Schenck (1925), Wilson (1943), Taliaferro (1945), Washburn (1946), Dempster (1951), and Dibblee (1972b, 1973d) as consisting in ascending order of (1) the Indart Sandstone of Taliaferro (1945), (2) The Los Muertos Creek Formation of Wilson (1943), and (3) the Tres Pinos Sandstone of Kerr and Schenck (1925). The sequence was generally thought to be internally conformable, to overlie Upper Cretaceous marine strata, and to be unconformably overlain by Quaternary nonmarine sediments.

The stratigraphic order of the sequence has been reinterpreted by Kaar (1962) on the basis of foraminiferal studies, by Sullivan (1965) on the basis of nannoplank-ton studies, and by Kleinpell, Weaver, and Doerner (1967) on the basis of general biostratigraphic relations, to consist in ascending order of (1) the Bolado Park Formation of Sullivan (1965), (2) the Tres Pinos Sandstone of Kerr and Schenck (1925), (3) the Los Muertos Creek Formation of Wilson (1943), and (4) the Indart Sandstone of Taliaferro (1945). These writers consider the top and bottom of the sequence to be truncated by faults and the sequence to be internally conformable, even though the contact between the Los Muertos Creek Formation and the Indart Sandstone is thought to be faulted and the contact between the Bolado Park Formation and the Tres Pinos Sandstone is covered.

Dibblee (oral commun., April 1974) considers the Bolado Park and Los Muertos Creek Formations to be equivalent and exposed on the opposite limbs of a syncline. We have not resolved the differences in the stratigraphic interpretations of this area and are not certain which stratigraphic superposition of units is correct. Preliminary work has suggested that the area is more complex structurally than has been previously shown. The following description of the formations is based on all of the previous work, with the ages based primarily on the paleontologic studies.

The Bolado Park Formation consists of foraminiferal mudstone and shale about 400 ft (120 m) thick. It is thought to-be of Ynezian to Penutian age, deposited at bathyal depths in a basin having access to the open ocean, although the lower 40 feet (12 m) may have been deposited in somewhat restricted conditions (Sullivan,

1965).

The unfossiliferous Tres Pinos Sandstone consists of thickly bedded sandstone with thin shale interbeds. It is as much as 900 ft (270 m) thick and is thought to be of Penutian age. It is composed of quartz, lesser amounts of feldspar, and small amounts of zircon, biotite, garnet, glaucophane, and sphene (Wilson, 1943). Our preliminary work indicates deposition on a submarine fan by turbidity currents, grain flows, and fluidized sediment flows; paleocurrent measurements indicate sediment

transport toward the north and northeast, with a source area consisting of granitic and metamorphic rocks located to the southwest within the Salinian block. It may be equivalent to the Cantua Sandstone Member of the Lodo Formation in the Vallecitos area (Nilsen, Dibblee, and Simoni,1974).

The Los Muertos Creek Formation is 1,100-1,250 ft (340-380 m) thick and consists of (a) a basal fossilifer-ous conglomerate 10-15 ft (3-4.5 m) thick that contains pebbles of quartz, chert and limestone; (b) siltstone and fine-grained sandstone about 600 ft (180 m) thick that contains local beds of coarse-grained sandstone as much as 4 ft (1.2 m) thick compositionally similar to the Tres Pinos Sandstone; and (c) interbedded siltstone, mudstone, and siliceous shale about 600 ft (180 m) thick. The Los Muertos Creek Formation thought to be of Ulati-sian and Narizian age. Molluscan faunas indicate deposition of the basal conglomerate in shallow marine environments; foraminiferal faunas from shale in the middle part of the formation indicate deposition at bathyal to abyssal depths and foraminiferal faunas from siliceous shale in the upper part of the formation indicate deposition at intermediate depths.

The Indart Sandstone consists of unfossiliferous fine-grained sandstone about 900 ft (270 m) thick and is thought to be Narizian or younger.

VALLECITOS AREA

Lower Tertiary strata as much as 5,000 ft (1,500 m) thick crop out in the Vallecitos syncline and along the adjacent eastern flank of the central Diablo Range. The strata disconformably overlie Upper Cretaceous marine strata and are conformably overlain by Refugian marine strata. The sequence is internally conformable except for an unconformity at the base of the Yokut Sandstone of White (1940) and the Domengine Sandstone (Anderson and Pack, 1915; White, 1938, 1940; Payne, 1951; Schoellhamer and Kinney, 1953; Pacific Section, American Association of Petroleum Geologists, 1957b; Mallory, 1959; Enos, 1965; Dibblee and Nilsen,

1974). The sequence comprises four units:

(1)	the Lodo Formation, about 500 to 5,000 ft (150-

1,500	m) thick, is here subdivided into three members: (a) the Cerros Shale Member, 100-700 ft (30-210 m) thick of Ynezian and Bulitian(?) age; (b) the Cantua Sandstone Member, 0-4,500 ft (0-1,400 m) thick of late Bulitian and Penutian age; and (c) the Arroyo Hondo Shale Member, 500-1,100 ft (150-340 m) thick of Penutian and Ulatisian age (White, 1938, 1940; Mallory, 1959; Sullivan, 1965). The shale members are similar in age and lithology to the Lodo Formation of other parts of the southern Diablo and northern Temblor Ranges and are mostly glauconitic, foraminiferal mudstone and siltstone but contain minor amounts of interbedded﻿NORTHEASTERN AREA

21

fine-grained sandstone. Only where the Cantua Sandstone Member is present are the shale members separable.

The Cantua Sandstone Member in outcrop wedges out in shale 7-8 miles (11-13 km) north and south of the Vallecitos syncline and probably in subsurface about 15 miles (24 km) east of it (White, 1940; Regan, 1943; Pacific Section, American Association of Petroleum Geologists, 1958). The Cantua consists mostly of fine- to coarse-grained, massive, thickly bedded, arkosic sandstone beds as much as 25 ft (7.6 m) thick, separated by thin shale interbeds. Regan (1943) determined a composition of about 40 percent quartz, 40 percent potassium feldspar, 15 percent andesine, and 5 percent heavy minerals and rock fragments. Nilsen, Dibblee and Si-moni (1974) counted 21-51 percent quartz, 13-29 percent potassium feldspar, 12-33 percent plagioclase feldspar, 1-4 percent glauconite, and 0-6 percent lithic fragments, biotite, and heavy minerals, and calculated a mean quartz:feldspar ratio of 0.92:1 and a mean potassium:plagioclase feldspar ratio of 1.18:1. The heavy mineral assemblage is characterized by variable but often high percentages of green hornblende, epidote and titanite, small amounts of garnet, zircon, and tourmaline, and rare andalusite and pyroxene (Regan, 1943). The mineralogy suggests that it was derived principally from a source area underlain by felsic plutonic rocks. Moderate depths and open ocean conditions are indicated by foraminiferal faunas from both the Cantua and lower Arroyo Hondo Members (Wood-side, 1957; Mallory, 1959). The thickness of the Cantua Sandstone Member together with the presence of fossils in shales of the Lodo Formation only a short distance to the north and south indicate deposition at shallow to medium depths and suggest that the sandstone was deposited in an east-west-trending, relatively narrow, subsiding trough. Regan (1943) concluded that Cantua sands were transported eastward through the Vallecitos "channel” from granitic source rocks west of the San Andreas fault. Nilsen, Dibblee, and Simoni (1974) determined that sediments were transported northward and northwestward, suggesting that the source area was located to the south, in the granitic rocks of the Salinian block west of the San Andreas fault.

(2)	The Ulatisian Yokut Sandstone of White (1940) is 0-300 ft (0-90 m) of fine- to medium-grained massive sandstones that are silty, micaceous, and somewhat carbonaceous near the base, and clean and well sorted in the upper part (White, 1940; Mallory, 1959). It is characterized by high potassium to plagioclase feldspar ratios (as much as 30:1) and a sparse heavy mineral assemblage dominated by zircon, tourmaline, garnet, and andalusite (Regan, 1943). Both abundant mollusks and discocyclinid Foraminifera suggest deposition in

shallow marine environments (White, 1940). Regan (1943) suggested that the Yokut sands were derived from a western source.

(3)	The Ulatisian Domengine Sandstone, 0-800 ft (0-240 m) thick, consists mostly of silty glauconitic shale with minor amounts of interbedded fine-grained sandstone and a basal fine- to medium-grained fos-siliferous pebbly sandstone (White, 1940; Mallory, 1959). It overlaps the Yokut Sandstone north and south of the Vallecitos syncline area and is widespread in the northern San Joaquin Valley. Thin lignite seams and fossiliferous "reefs” that contain abundant molluscan and foraminiferal faunas suggest deposition in shallow marine and locally brackish-water environments (White, 1940). Common heavy minerals include zircon, tourmaline, titanite, garnet, and glaucophane; variable amounts of epidote, andalusite, and hornblende are also present (Regan, 1943). The abundance of glaucophane and red and green radiolarian chert pebbles suggests a Franciscan provenance probably located in the area of the present central Coast Ranges (White, 1940; Regan, 1943). The Domengine and Yokut cannot be separated throughout the area, and Dibblee and Nilsen (1974) mapped them as an undivided unit, both deposited in shallow marine conditions, locally with angular unconformity on older rocks.

(4)	The Kreyenhagen Shale, 1,000 to 2,000 ft (300-600 m) thick, of Narizian and Refugian age, consists of shale that is semisiliceous in the upper part and contains foraminiferal faunas indicative of deposition at medium or greater depths and free access to the open ocean (Mallory, 1959).

NORTHERN TEMBLOR RANGE, SOUTHERN DIABLO RANGE,

AND ADJACENT SAN JOAQUIN VALLEY — cJU<r

The thick lower Tertiary sequence in the southwestern San Joaquin Valley and adjacent Coast Ranges has been subdivided by Dibblee (1973c, e) into four parts. (1) The Lodo(?) Formation, 0-300 ft (0-90 m) thick and of Ynezian to early Penutian age, consists mostly of shale.

In the Temblor Range and Devils Den area, foraminiferal faunas from the lower part suggest deposition at bathyal depths in a basin having free access to the open ocean whereas those from the upper part suggest deposition at neritic depths (Mallory, 1970).

(2) The Avenal Sandstone (includes the Mabury Formation of Van Couvering and Allen (1943), middle Lodo Sandstone of Mallory (1959), and Acebedo Sandstone of Dickinson (1963), as well as the typical Avenal Sandstone), 0-600 ft (0-180 m) thick and of late Penutian to Ulatisian age, is a fine- to coarse-grained sandstone that contains discocyclinid Foraminifera, corals, burrowing annelids, and algal debris indicative of deposition at shoal depths. In the northern Temblor Range the﻿22

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Avenal also contains abundant shale chips, pebbles and cobbles of chert, quartzite, and metavolcanic rocks, and less common boulders of granitic rocks.

(3)	The Kreyenhagen Shale, 0-1,250 ft (0-380 m) thick is of Ulatisian to Refugian age and consists mostly of deep-marine hemipelagic shale. The Kreyenhagen is separated into the Gredal Shale Member of Ulatisian age (includes the upper Lodo Shale of Mallory, 1959) and the Welcome Shale Member of Narizian and Refugian age by the intervening Point of Rocks Sandstone, which wedges out into the Kreyenhagen Shale. Foraminiferal faunas from the Gredal Shale Member in the Temblor Range and at Devils Den (V. S. Mallory, written commun., April 1970 and December 1971) suggest a progressive deepening of the basin from neritic to bathyal depths.

(4)	The Point of Rocks Sandstone, of Ulatisian to early Narizian age, is 0-2,900 ft (0-880 m) thick in outcrops at Devils Den and in the northern Temblor Range, where it is truncated by an unconformity. It increases in thickness to more than 5,000 ft (1,500 m) in subsurface farther southeast, where it may contain Penutian or older strata in its lower part; it decreases in thickness northward and eastward, wedging out within the Kreyenhagen Shale along Reef Ridge and in subsurface 18-25 miles (29-40 km) east of the Devils Den and Temblor Range outcrops (Clarke, 1973). It is mostly a thickly bedded, medium- to coarse-grained, arkosic sandstone with subordinate shale. The sandstones are 35-50 percent quartz, 14-18 percent potassium feldspar, 10-18 percent plagioclase feldspar, 1-5 percent other minerals (principally biotite), and 8-10 percent lithic fragments that include chert, quartzite, shale, slate, argillite, phyllite, quartzofeldspathic metamorphic and plutonic rocks, and minor amounts of andesitic or basaltic volcanic rocks. Microcline and perthite feldspar are ubiquitous constituents; the plagioclase feldspar is unzoned oligoclase and sodic an-desine. Zircon, sphene, apatite, epidote, pink garnet, and green hornblende are the most common heavy minerals. The sandstones are generally intermediate between arenites and wackes (Clarke, 1973).

Foraminiferal faunas indicate that the Point of Rocks Sandstone was deposited largely at bathyal or greater depths in a basin having free access to the open ocean (Mallory, 1959, 1970). Paleocurrents in the northern Temblor Range indicate northwestward sediment transport, and those in the southern Diablo Range northeastward sediment transport (Clarke, 1973). Clarke (1973) concluded that the Point of Rocks sands were probably derived from two source areas within the Salinian block to the west: one situated south of the northern Temblor Range and the other west of the Devils Den and Avenal Ridge outcrop areas. Both source

areas are inferred to have been underlain by felsic plutonic and associated metamorphic basement rocks as well as older sedimentary rocks. Clarke (1973) inferred that the Point of Rocks was deposited as a large deep-sea fan.

The shallow-marine Avenal Sandstone of the Reef Ridge and probably of the Avenal Ridge area, is largely equivalent in age (Ulatisian) to the Gredal Shale Member and the lower part of the Point of Rocks Sandstone to the south (Stewart, 1946; Mallory, 1959; Dickinson, 1963; Sullivan, 1965). This relation indicates that shallow marine conditions prevailed in the southern Diablo Range concurrently with deep marine conditions to the south in the Devils Den area and northern Temblor Range.	_	. .	i i ,

&*/*r*f <rv

SAN EMIGDIO AND WESTERN TEHACHAPI MOUNTAINS AND ADJACENT SOUTHERN SAN JOAQUIN VALLEY

The Eocene sedimentary rocks that crop out extensively in the east-west-trending San Emigdio and western Tehachapi Mountains provide an exposed cross section of similar Eocene rocks that underlie the southern San Joaquin Valley to the north. The Eocene strata in the mountains comprise the Tejon Formation and the lower parts of the San Emigdio and Tecuya Formations. The sequence rests unconformably on granitic basement rocks in the eastern and central parts of the area and on mafic and ultramafic basement rocks in the western part of the area.

The Tejon Formation, which is as much as 4,000 ft (1,200 m) thick, has been subdivided by Marks (1941, 1943) into four members.

(1)	The Uvas Conglomerate Member, 0-400 ft (0-120 m) thick, ranges in age from "Capay” in the west to "Tejon” in the east. It consists of a basal cobble and boulder conglomerate made up of clasts derived from the underlying basement rocks, overlain by interbed-ded arkosic sandstone and pebble and cobble conglomerate composed primarily of clasts of quartzite, por-phyritic volcanic recks, granite, and gneiss. A locally abundant megafauna indicates deposition in shallow marine environments.

(2)	The Liveoak Shale Member is 0-2,000 ft (0-600 m) thick, of Ulatisian and Narizian age. It consists of shale with subordinate siltstone, fine-grained sandstone, and lenses of conglomerate. Locally abundant foraminiferal faunas indicate deposition at shallow depths in the east, bathyal depths in the central and western areas, and lower bathyal to abyssal depths in the westernmost areas.

(3)	The Metralla Sandstone Member, 0-2,000 ft (0-600 m) thick, is of "Tejon” age. It consists of massive, silty, fine-grained arkosic sandstone with some inter-bedded conglomerate and siltstone. Its abundant mol-﻿NORTHEASTERN AREA

23

luscan fauna indicates deposition at shallow depths in the east and at bathyal depths in the west. It fingers out westward into deep-marine shales of the Liveoak Shale Member.

(4)	The Narizian Reed Canyon Siltstone Member is 0-200 ft (0-60 m) thick, consisting mostly of siltstone but with some interbedded sandstone and shale that is locally very carbonaceous. Molluscan and foraminiferal faunas indicate deposition in shallow marine environments (Harris, P. B., 1950; Hammond, 1958; Mallory, 1959; Dibblee, 1961; Nilsen, 1972, 1973a, b, c; Nilsen and others, 1973).

Sandstones of the Tejon Formation are arkosic, generally about 50 percent quartz and 50 percent feldspar, with minor amounts of lithic fragments (chert, volcanic rocks, quartzite, granitic rocks, and shale) and biotite, chlorite, and muscovite. Nilsen (1973c) inferred (1) that the Tejon Formation was deposited during an eastward transgression across the present outcrop area during "Capay” to "Tejon” time and a subsequent westward regression during "Tejon” time; (2) that sediments were transported primarily toward the west; and (3) that a west-facing submarine slope in the western part of the area separated a shallow-marine shelf area in the east from a deep-marine basin in the west in which hemipelagic shales and turbidite sandstones were deposited.

In the east, the Tejon Formation grades upward into the Tecuya Formation, primarily nonmarine conglomerate apparently derived from source areas to the east and southeast and composed of clasts of quartzite, por-phyritic volcanic rocks, granite, gneiss, and marble (Nilsen and others, 1973). Nilsen (1972, 1973c) concluded that the lowermost part of the Tecuya Formation is late Eocene and that it was deposited as coastal plain fanglomerates. These overlie and in part interfinger westward with shallow-marine sedimentary rocks of the Tejon Formation.

In the west, the Tejon Formation is overlain conformably by the San Emigdio Formation of Narizian and Refugian age (DeLise, 1967). The lower (Narizian) part consists of a massive shallow-marine sandstone that contains pebbly conglomerate and abundant medium-to large-scale cross-strata, overlain by a shale deposited in deeper marine waters. Subsurface and outcrop data suggest that the sandstone was derived from a southern source area (Tipton, 1971; Tipton and others, 1973; Nilsen and others, 1973).

Middle and late Eocene subsurface equivalents of these formations can be traced northward for at least 75 miles (120 km) beneath the southern San Joaquin Valley. In the east, the lower part of the nonmarine Walker Formation, which ranges in age from Eocene to early Miocene, interfingers westward with the late Eocene

shallow-marine Famosa sand 7-12 miles (11-19 km) west of exposed Sierran basement (Pacific Section, American Association Petroleum Geologists, 1957a; Clarke, 1973). This marine-nonmarine transition probably corresponds to the contact between the Tejon and Tecuya Formations in the Tehachapi Mountains; it delineates the eastern shoreline of the San Joaquin basin area during the late Eocene.

The Famosa sand, which is present in subsurface 7-15 miles (11-24 km) west of this shoreline, is 200-600 ft (60- 180 m) thick and consist of fine- to coarse-grained, massive sandstone and interbedded siltstone and shale. It correlates with the upper part of the Tejon Formation to the south, as well as the Kreyenhagen Formation and Point of Rocks Sandstone to the west (Beck, 1952; Pacific Section, American Association Petroleum Geologists, 1957a; Hackel, 1966). The Famosa generally rests on an interbedded sandstone, siltstone, and shale unit 50-250 ft (15-75 m) thick that rests in turn on crystalline basement rocks; this lower unit was probably deposited in a nonmarine environment.

The Famosa sand interfingers westward in subsurface with the Kreyenhagen Formation, which is 250-650 ft (75-200 m) thick here and consists mostly of dark organic shale with some thin interbedded fine-grained sandstone. The Kreyenhagen is lithologically similar and generally equivalent in age to the Liveoak Shale Member of the Tejon Formation and the Kreyenhagen Formation of the Temblor Range. Foraminiferal faunas indicate a late Ulatisian and Narizian age, deposition at bathyal to abyssal depths, and possibly an eastward shallowing of the basin (Mallory, 1959; Clarke, 1973). This westward bathymetric and lithofacies transition from shelf to deep basin environments appears to define a west-facing paleoslope that extended northward from the western San Emigdio Mountains to a position 8-15 miles (13-24 km) southwest of Bakersfield and thence northeastward for about 60 miles (100 km) to a position 5-15 miles (8-24 km) east of the Kettleman Hills.

SOUTHERN TEHACHAPI MOUNTAINS ^

Lower Tertiary strata of the nonmarine Witnet Formation crop out in the southern Tehachapi Mountains and eastward along the Garlock fault (Buwalda, 1954; Dibblee, 1967; Dibblee and Louke, 1970). The formation is as much as 4,000 ft (1,200 m) thick, resting uncon-formably on granitic basement rocks and overlain un-conformably by Miocene volcanic and nonmarine sedimentary rocks. Although no fossils have been found in the Witnet Formation, Dibblee (1967) correlated it with the lower Tertiary Goler Formation in the El Paso Mountains to the west. The Witnet generally comprises a lower cobble conglomerate and pebbly arkosic sand-﻿24

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

stone that is overlain by arkosic sandstone with minor siltstone. The conglomerate clasts include granitic rocks, aplite, porphyritic volcanic rocks, metaporphyry, quartzite, and quartz. Dibblee (1967) concluded that the Witnet Formation was deposited by alluvial processes in a northeast-trending lowland area situated between highlands in the present Mojave Desert and Sierra Nevada regions.

EL PASO MOUNTAINS	*

Lower Tertiary strata of the nonmarine Goler Formation crop out along the north flank of the El Paso Mountains, which are located north of the Garlock fault and east of the Sierra Nevada (Dibblee, 1952, 1967). The formation is as much as 6,500 ft (2,000 m) thick, resting unconformably on igneous and metamorphic basement and overlain unconformably by Pliocene nonmarine sedimentary rocks. Fossil plant remains and leaves considered to be of Eocene age have been recovered from a thin coal seam at the base of the formation (F. W. Knowlton, in Fairbanks, 1896; Axelrod, 1949). However, vertebrate remains recovered from localities about 1,500 ft (460 m) stratigraphically above the Eocene plant locality are considered to be of Paleocene age (McKenna, 1955, 1960). Dibblee (1952) divided the Goler Formation informally into two members: a conglomerate and breccia unit 0-1,500 ft (0-460 m) thick apparently derived from source rocks underlying the El Paso Mountains, and an overlying arkosic sandstone and red mudstone unit as much as 6,000 ft (1,800 m) thick with local lenses of conglomerate, apparently derived (Christiansen, 1961) from source areas beyond the El Paso Mountains. Conglomerate clasts include granitic rocks, chert, quartzite, limestone, and porphyritic volcanic rocks. Dibblee (1952, 1967) inferred that the Goler Formation was deposited by alluvial processes in a northeast-trending lowland area situated between highlands in the present Mojave Desert and Sierra Nevada regions.

SOUTHEASTERN AREA

Lower Tertiary marine sedimentary rocks crop out only in two relatively small and widely separated parts of the southeastern area, which is located south of the Garlock fault and east of the San Andreas fault and includes parts of the Mojave Desert, Transverse Ranges, and Salton Trough provinces (figs. 1 and 2). The lower Tertiary marine strata in both areas are unconformably overlain by Oligocene or Miocene nonmarine and volcanic strata.

CAJON PASS AREA

Lower Tertiary strata that crop out in and adjacent to Cajon Pass were originally designated the Martinez Formation by Noble (1954) and later redefined as the

San Francisquito Formation by Dibblee (1967). These strata rest unconformably on granitic and gneissic basement rocks and are unconformably overlain by Miocene strata. The San Francisquito Formation is considered Paleocene and Eocene(?) on the basis of rare marine megafauna recovered from the basal part of the sequence. It consists of a lower pebble to boulder conglomerate 550 ft (170 m) thick composed of clasts of the underlying basement rocks and interbedded with thin to thick-bedded lenticular sandstone, and an upper interbedded sandstone and shale 270 ft (80 m) thick (Sage, 1973). The conglomerate near the top of the lower conglomeratic unit contains mostly clasts of quartz monzo-nite, biotite gneiss, and aplite, with lesser amounts of quartzite, quartz, and sandstone and very small amounts of volcanic rocks; the overlying sandstone is arkosic and contains much larger amounts of potassium feldspar than plagioclase feldspar (Sage, 1973). Sage (1973) determined south-southwest-directed paleocur-rents in the San Francisquito Formation and inferred that it was deposited as a submarine fan; he also suggested that it was derived from a source area underlain by felsic to intermediate plutonic and gneissic rocks.

OROCOPIA MOUNTAINS


The Maniobra Formation of Crowell and Susuki (1959), 4,800 ft (1,460 m) thick, crops out in a structural depression in the Orocopia Mountains. The Maniobra is considered to be of "Capay” and "Domengine” age on the basis of marine magafauna; it rests unconformably on granitic and gneissic basement rocks, and is unconformably overlain by Miocene(?) nonmarine sedimentary rocks. Crowell and Susuki (1959) informally divided it into a lower breccia and conglomerate 2,000 ft (600 m) thick and an upper thinly bedded siltstone 3,000 ft (900 m) thick that contains some interbedded arkosic sandstone beds as much as 30 ft (9 m) thick. Both units contain exotic clasts as large as 30 ft (9 m) in diameter. The sandstones are 43-80 percent quartz, 15-48 percent potassium feldspar, 1-14 percent perthite, and 1-5 percent plagioclase feldspar and lithic fragments, including quartzite, granite, gneiss, and metasiltstone. Crowell and Susuki (1959) concluded that the Maniobra Formation was deposited in a shallow marine embay-ment that probably extended eastward from the present outcrops, may have deepened offshore toward the west or south, and was adjacent to a steep, rugged coastline.

SOUTHWESTERN AREA

A great variety of lower Tertiary strata crop out in the southwestern area, which is bounded on the north and east by the Sur-Nacimiento, Rinconada, Big Pine, and San Andreas faults (fig. 1, 2). Marine strata crop out in the Transverse Ranges, western Peninsular Ranges and offshore islands; nonmarine strata crop out in the﻿SOUTHWESTERN AREA

25

eastern Transverse Ranges and Peninsular Ranges. The marine and nonmarine facies distinguished in the Peninsular Ranges can be traced southward into Baja California.

Distinctive grayish-red porphyritic rhyolite tuff clasts, known as the "Poway Conglomerate clast assemblage” or "Poway-type” clasts (Woodford and others, 1968) are present in Eocene conglomerates in the Lake Elsinore, Lake Henshaw, western Peninsular Ranges, Santa Ana Mountains, San Joaquin Hills, Santa Monica Mountains, Simi Hills, and Piru Creek areas, as well as on the Channel Islands and San Nicolas Island (Yeats, 1968; Cole, 1973; Yerkes and others, 1965; Minch, 1971). They are variously considered to have been derived from unroofing of the Peninsular Ranges batholith (Bellemin and Merriam, 1958), from Permian and Triassic rocks of the Mojave Desert (Delisle and others, 1965), from an unspecified distant eastern source (Peterson, 1970, 1971), and from volcanic rocks in northern Sonora, Mexico (Merriam, 1968, 1972). The clasts are very hard and extremely resistant to abrasion, and are inferred by Abbott and Peterson (1974) to indicate high energy, long distance fluvial transport.

Nonmarine strata of late Eocene, Oligocene, and early Miocene age conformably or unconformably over-lie the lower Tertiary marine strata in most parts of the southwestern area (Bohannon, 1974). These nonmarine strata are generally coarse-grained clastic rocks that were deposited in a variety of fluvial environments. Lower Tertiary marine sequences are conformably overlain by the nonmarine Sespe Formation of late Eocene, Oligocene and, early Miocene age in the Ortega Hill, Santa Ynez Mountains, Topatopa Mountains, central Santa Monica Mountains, Santa Ana Mountains, and San Joaquin Hills areas, and are unconformably overlain by the Sespe Formation in the Piru Creek, Las Llajas Canyon, Simi Hills, and Santa Rosa Island areas (McCracken, 1969, 1972). However, the conformable or unconformable nature of the basal contact of the Sespe has not been agreed upon in each area by all workers, and its nature may vary locally within the different areas. In the Elizabeth Lake Canyon area, the nonmarine and volcanic Vasquez Formation of Oligocene and early Miocene(?) age overlies lower Tertiary strata (Dibblee, 1967). In the western Peninsular Ranges, the last phase of lower Tertiary sedimentation is marked by deposition of nonmarine conglomerates of the Poway Group.

ORTEGA HILL, PINE MOUNTAIN, SANTA YNEZ MOUNTAINS, AND TOPATOPA MOUNTAINS AREAS

A thick, mostly Eocene sequence of lower Tertiary strata is present in these areas and fills an east-west

trending basin generally known as the Santa Ynez basin. The basin can be informally divided into four areas for discussion purposes: (1) the Ortega Hill area, located south of the Big Pine fault, southwest of the Pine Mountain fault, and north of the Hildreth-Munson Creek-Tule Creek faults; (2) the Pine Mountain area, located south of the Big Pine fault and northeast of the Pine Mountain fault; (3) the Topatopa Mountains area, located south of the Tule Creek and Pine Mountain faults and east of Ojai; and (4) the Santa Ynez Mountains area, located south of the Hildreth-Munson Creek-Tule Creek faults and west of Ojai, and subdivided into northern and southern areas by the Santa Ynez fault (fig. 3). The sequence rests disconformably on Upper Cretaceous marine strata in most areas but on granitic basement rocks in the Pine Mountain area and on Franciscan rocks in the westernmost outcrops north of the Santa Ynez fault.

The sequence can conveniently be divided into (1) Ynezian(?) to Ulatisian strata, comprising the Juncal Formation and lithologically similar units of correlative age, and (2) Ulatisian and Narizian strata, comprising the Matilija Sandstone, Cozy Dell Shale, Coldwater Sandstone, and lithologically similar units of generally correlative age (Dickinson, 1969).

The Juncal Formation in its type area in the northern Santa Ynez Mountains area consists of (1) a lower unit of shale 1,000 ft (300 m) thick, (2) a middle unit of sandstone 1,000 ft (300 m) thick and (3) an upper unit of shale 1,500 ft (460 m) thick (Page and others, 1951; Dibblee, 1966a). The depositional basin in this area shoaled toward the north and east where shallow marine facies are present and deepened toward the south and west, where deeper marine facies are present. In its type area, the Juncal conformably overlies the Sierra Blanca Limestone, which is of Penutian age and 0-270 ft (0-80 m) thick, consisting of carbonates deposited in algal bank, shoreline, talus slope, and other shallow marine environments (Walker, 1950; Johnson, 1968; Schroeter, 1972a, b, 1973).

In the Pine Mountain area to the northeast, the Juncal consists of fossiliferous, lenticular units of conglomerate, arkosic sandstone, siltstone and mudstone that are about 12,000 ft (3,700 m) thick (Schlee, 1952; Ved-der and others, 1973; Givens, 1974). It rests unconformably on granitic rocks along the eastern margin of the area. These deposits are inferred to have been derived from source areas north, northeast, east, and southeast of the basin (Jestes, 1963). It was deposited in continental, transitional, and generally shallow marine environments (Givens, 1974). In the Ortega Hill area to the west, the Juncal consists mostly of mudstone and silt-stone (Jestes, 1963; Badger, 1957).

South of the Santa Ynez fault in the central Santa Ynez Mountains, the three lithologic divisions of the﻿26

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

OCEAN

PACIFIC

Figure 3.—Index map of the western Transverse Ranges showing the distribution of outcrops of lower Tertiary sedimentary rocks (modified from Jennings and Strand,

1969, and Jennings, 1959).﻿SOUTHWESTERN AREA

27

Juncal distinguished in the type area are present; however, the middle sandstone is much thicker and is called the Camino Cielo Sandstone Member (Page and others, 1951). Stauffer (1965, 1967) concluded that most of the Juncal Formation in this area was deposited by turbidity currents, and that the Camino Cielo was deposited by grain-flow processes. Paleocurrent measurements from the lower Juncal indicate sediment transport to the southwest; those from the upper Juncal indicate transport to the west, south, and southeast.

Farther east, in the western Topatopa Mountains, the Juncal Formation consists of the Camino Cielo Sandstone Member, 1,500 ft (460 m) thick, overlain by a mudstone unit 5,000 ft (1,500 m) thick that contains some interbedded sandstone (Bailey, in Redwine and others, 1952). The Juncal is not present in the eastern Topatopa Mountains (Eschner, 1969). The sandstones of the Juncal are arkoses, with the potassium feldspar to plagioclase feldspar ratios varying from 1:4 to 4:1; other constituents are lithic fragments (9-26 percent), which include granitic, volcanic, metamorphic, and chert fragments, and minor amounts of biotite and heavy minerals (Stauffer, 1965).

In the western Santa Ynez Mountains, the Anita Shale of Kelly (1943), 300-1,000 ft (90-300 m) thick and of Ynezian to Ulatisian age, underlies the Matilija Sandstone and is laterally equivalent to the Juncal Formation (Kelley, 1943; Dibblee, 1950; Kleinpell and Weaver, 1963; Hornaday and Phillips, 1972; Gibson, 1973c). The Anita has been divided by Gibson (1973c) into a lower silstone member, a middle mudstone member, and an upper siltstone member; in its lower strata, it contains thin sandstone beds with scattered lenses of algal limestone (Weaver and Molander, 1964; Gilson, 1972,1973b, c). Weaver (1962) concluded that it was deposited in an offshore basin that deepened southward progressively to bathyal depths. Paleocurrent measurements indicate that sediment transport was southward (Stauffer, 1965) and south westward (Gibson, 1973c). According to Sage (1973), the Anita Shale was deposited on an offshore ocean floor characterized by very slow rates of sedimentation; the source area lay to the east (Gibson, 1973c).

The Ulatisian and younger parts of the Eocene sequence have type areas south of the Santa Ynez fault in the eastern Santa Ynez Mountains and Topatopa Mountains areas (Vedder, 1972). Although parts of the sequence have been traced northward and westward, correlation over the whole area is difficult, probably because depositional environments represented by tongues and lenses of lithologically similar strata migrated laterally through time, producing complex facies relationships (Dickinson, 1969).

The type Matilija Sandstone is 2,750 ft (840 m) thick,

of Ulatisian or Narizian age. The lower part of the formation consists of thinly bedded, fine-grained sandstone (Bailey, in Redwine and others, 1952) with foraminiferal faunas indicative of deposition at bathyal depths (Blaisdell, 1955). The lower part of the Matilija Sandstone was deposited by turbidity currents that flowed northwestward, northeastward, and northward (Jestes, 1963). The upper part of the Matilija Sandstone in the type area is thickly bedded, medium- to coarsegrained sandstone (Bailey, in Redwine and others, 1952) that contains molluscan and foraminiferal faunas indicating deposition in shallow marine environments (Blaisdell, 1955). Very shallow marine nearshore deposition is indicated by sedimentary features in the upper Matilija, and paleocurrent patterns indicate sediment transport toward the southeast (Jestes, 1963). The Matilija is thought to thin eastward in the eastern Topatopa Mountains area, where it may finger out into shale (Eschner, 1969); however, a thick sequence of fossiliferous sandstone and shale is present there that may possibly be laterally equivalent to the Matilija. This sequence is thought to have been deposited in shallow marine environments and is inferred to have been derived from source areas to the north and east.

In the central Santa Ynez Mountains, the Matilija is massive sandstone with some intercalated mudstone about 2,000 ft (600 m) thick (Page and others, 1951; Dibblee, 1966a). Stauffer (1965, 1967) concluded that the lower part of the Matilija here was deposited principally by grain-flow processes, with sediment transport toward the south and east; for the upper part, he inferred shallow marine deposition, with sediment transport toward the south and west. The Matilija thins in the western Santa Ynez Mountains near San Marcos Pass, and has been correlated with different units by different workers in the westernmost areas (Kelley, 1943; Dibblee, 1950). For the correlative unit determined by Stauffer (1965, 1967) and Gibson (1973a, c) in the western Santa Ynez Mountains, Stauffer (1967) inferred that it had been deposited by grain-flow processes, and determined sediment transport toward the west and south. In the northern Santa Ynez Mountains area north of the Santa Ynez fault, the Matilija is about 1,300 ft (400 m) thick; here also the lower part is thought to be a deep marine grain-flow deposit and the upper part a shallow marine traction current deposit (Stauffer, 1965; Link, 1971, 1972, 1974).

In the Ortega Hill and Pine Mountain areas, the Matilija apparently consists of several sandstone and shale units; in general, coarse-grained, shallow-marine deposits are present toward the east and fine-grained, deeper marine deposits toward the west (Schlee, 1952; Badger, 1957; Kiessling, 1958; Carman, 1964; Dickinson, 1969; Vedder and others, 1973). The Matilija in the﻿28

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Pine Mountain area i s as much as 1,600 ft (490 m) thick and is inferred to haT e been deposited in a nearshore, inner-sublittoral, marine environment (Givens, 1974); paleocurrents indicate sediment transport toward the north and west, with source areas probably to the east and possibly to the north, south and southeast (Jestes, 1963). In the Ortega Hill area, the Matilija is inferred to have been deposited by turbidity currents and submarine sliding; paleocurrents indicate sediment transport toward the northwest (Jestes, 1963).

In the northern Santa Ynez Mountains, the composition of the Matilija Sandstone averages 40 percent quartz, 35 percent feldspar (about equal amounts of potassium and plagioclase feldspar), and smaller amounts of lithic fragments, which include granitic, metamorphic, volcanic, and sedimentary types, mica, chlorite, and chert; heavy minerals include epidote, sphene, magnetite, apatite, zircon, tourmaline, garnet, and monazite (Link, 1972). Conglomerate clasts from local pebble beds consist of silicic volcanic rocks, chert, mafic igneous rocks, graywacke, limestone, granitic rocks, and quartz arenite (Link, 1972).

The Narizian Cozy Dell Shale is about 3,250 ft (1,000 m) thick in its type area, where it is silty shale and mudstone with some thin beds of fine-grained sandstone and limestone concretions (Kerr and Schenck, 1928; Bailey, in Redwine and others, 1952). It has been mapped throughout almost the entire region, although its thickness varies considerably: 465 ft (140 m) thick in the eastern Topatopa Mountains area, 1,700 ft (520 m) thick in the central Santa Ynez Mountains (Page and others, 1951; Dibblee, 1966a), about 700 ft (210 m) thick in the western Santa Ynez Mountains (Dibblee, 1950), as much as 4,000 ft (1,200 m) thick in the northwestern Santa Ynez Mountains area (Dibblee, 1966a; Blaisdell, 1955), and more than 4,000 ft (1,200 m) thick in the Ortega Hill area, where it includes thick sequences of sandstone (Jestes, 1963; Badger, 1957; Dickinson,

1969). In the Pine Mountain area it has been mapped as a southeastward-lensing tongue of mudstone that includes much sandstone and some limestone; it ranges in thickness from 0 to 700 feet (0-210 m) and is thought to have been deposited at outer-sublittoral or bathyal depths (Vedder and others, 1973; Givens, 1974). Stauffer (1965, 1967) determined that sediment transport in the Cozy Dell was toward the south and west, and locally toward the north. Weaver (1962), Weaver and Weaver (1962), and Molander (1956) concluded that deposition took place at bathyal depths.

The Narizian Coldwater Sandstone is about 2,500 ft (760 m) thick in its type area in the Topatopa Mountains area, where it is a thick-bedded fossiliferous sandstone interbedded with mudstone, shale and pebble conglomerate (Kerr and Schenck, 1928; Bailey, in Redwine and

others, 1952). The Coldwater is lithologically similar at the eastern end of the Topatopa Mountains area, but is only 1,280 ft (390 m) thick (Eschner, 1969). In these areas, the lower part of the Coldwater is thought to be a turbidite, and the upper part a shallow-marine deposit (Natland and Kuenen, 1951). In the Pine Mountain and Ortega Hill areas, the Coldwater is about 500 ft (150 m) thick and consists of sandstone that is locally conglomeratic and interbedded with siltstone and mudstone; in these areas, it rests with local unconformity on the Cozy Dell Shale and was deposited in very nearshore marine and marginal marine, locally deltaic, environments (Jestes, 1963; Vedder and others, 1973; Givens, 1974).

In the western Santa Ynez Mountains, the Coldwater Sandstone grades laterally westward into the Sacate Formation of Kelley (1943), which is about 1,000 ft (300 m) thick, mostly sandstone in the lower part and mudstone in the upper part (Kelley, 1943; Dibblee, 1950; Hornaday, 1965; Hornaday and Phillips, 1972). The Sacate is thought to have been deposited at bathyal depths (Wilson, 1954; Hornaday, 1961; Kleinpell and Weaver, 1963); deposition is thought to have been by grain-flow and turbidity current processes as well as by hemipelagic sedimentation on a submarine fan, with sediment transport dominantly toward the west (O’Brien, 1972).

The Gaviota Formation of Effinger (1936), 700-1,750 ft (210-530 m) thick and of Narizian and Refugian age, overlies the Coldwater and Sacate Formations in the western Santa Ynez Mountains (Kelley, 1943; Dibblee, 1950). The lower member is a mudstone of Narizian age which was deposited at bathyal depths (Wilson, 1954; Kleinpell and Weaver, 1963); this member thins eastward and grades laterally into shallow marine sandstone (O’Brien, 1972).

Sandstones of the Coldwater, Sacate, and Gaviota Formations in the western Santa Ynez Mountains are arkoses or lithic arkoses, 40-50 percent quartz, 20-30 percent potassium feldspar, 10-20 percent plagioclase feldspar, and 5-30 percent lithic fragments, mostly igneous but including some metamorphic and sedimentary fragments (O’Brien, 1972).

The overall mineralogy and chemistry of the arkosic sandstones and shales of the Eocene and Oligocene strata in the Santa Ynez Mountains area are thought to indicate a source area of plutonic igneous and metamorphic rocks with minor amounts of volcanic rocks; these data, combined with general paleogeo-graphic and paleocurrent data, suggest that the primary source area was located to the east in the Mojave Desert region (Van de Kamp and Leake, 1974).

Stauffer (1965, 1967) suggested that the east-westtrending Santa Ynez basin filled with sediment during﻿SOUTHWESTERN AREA

29

two successive cycles of sedimentation, the first concluding with the shallow marine sandstones of the upper Matilija and the second with the shallow marine sandstones of the Coldwater and nonmarine deposits of the Sespe. He considered the primary source area to be to the north except for the Cozy Dell Formation, which may have had a southerly source, and the Coldwater and Sespe Formations, which may have had sources more to the east.

Within the general area of the early Tertiary Santa Ynez basin, the limits of the basin and several subbasins have been recognized. The basin was apparently separated from the Sierra Madre basin to the north by an east-northeast-trending high generally known as the San Rafael high, which was underlain by Franciscan rocks. The high was not a major source of sediment for the deposits of the Santa Ynez basin prior to middle Eocene time, because only the localized algal bank deposits in the northern Santa Ynez Mountains contain Franciscan detritus before this time. However, Franciscan detritus is more abundant locally in younger strata, suggesting that it may have become a more important source of sediments in middle and late Eocene and Oligocene time (Gibson, 1973c).

To the west, in the Point Conception area, the Anita Formation and younger strata thin against a sill underlain by Franciscan rocks that forms the western boundary of the basin (Gibson, 1973c). The shelf break that separated relatively deep marine deposits to the south from shallow marine deposits to the north trended generally parallel to the modern Santa Ynez fault (Stauffer, 1965; Gibson, 1973c). A high in the San Marcos Pass area may have separated the basin into two subbasins to the west and east; prominent facies and thickness changes take place in this area. Eastward, the basin merges into the southeastern end of the Sierra Madre basin (Chipping, 1972a); farther eastward and southeastward, other basins or subbasins were present in the Simi Hills and Elizabeth Lake Canyon areas. The southern edge of the Santa Ynez basin is not well defined; the basin may have continued offshore into an ocean floor setting.

PIRU CREEK AREA

Upper Paleocene to upper Eocene strata 17,000 ft (5,200 m) thick rest unconformably on granitic basement rocks east and west of lower Piru Creek. Kriz (1947) divided the sequence into (1) conglomerate 2,900 ft (880 m) thick with minor amounts of shale and sandstone; (2) silty shale 5,000 ft (1,500 m) thick; ($) finegrained conglomerate 2,000 ft (600 m) thick, with some sandstone near the base; (4) shale 4,500 ft (1,400 m) thick interbedded with sandstone; (5) thickly bedded, locally pebbly feldspathic marine sandstone 650-2,400

ft (180-730 m) thick interbedded with some shale; and (6) massive, cross-stratified nonmarine sandstone 0-2,300 ft (0-700 m) thick interbedded with varicolored shale, siltstone, and some pebbly conglomerate. Kriz (1947) concluded that the entire sequence was deposited in shallow marine, possibly deltaic environments during a marine transgression followed by a regression. For the lower 2,300 ft (700 m) of the sequence, however, Sage (1973) determined southwest-flowing paleocur-rents; he inferred that this part of the sequence was deposited on a submarine fan and was derived from a nearby source area to the northeast underlain by felsic to intermediate volcanic and plutonic rocks and gneissic rocks.

LAS LLAJAS CANYON, SIMI HILLS AND SANTA SUSANNA MOUNTAINS AREA

Lower Tertiary strata crop out in Las Llajas Canyon and in the southwestern Santa Susanna Mountains to the north and the Simi Hills to the south. The sequence rests unconformably on Upper Cretaceous marine strata and consists of four parts.

(1)	Marine and nonmarine strata of "Martinez” age 280-1,430 ft (85-440 m) thick, consist of (a) a lower unfossiliferous conglomerate containing sandstone lenses inferred to have been deposited in an alluvial fan-braided river complex, (b) a middle unit of red beds consisting of conglomerate, sandstone, shale, and pisolitic claystone, inferred to have been deposited in meandering river and lagoonal environments, and (c) an upper fossiliferous sandstone that is lenticularly bedded, contains peaty shale interbeds, and is inferred to have been deposited' in lagoonal, alluvial, and shallow-marine environments (Sage, 1973).

(2)	Fossiliferous sandstone interbedded with shale, 415-2,360 ft (125-720 m) thick of Ynezian to Bulitian age, is inferred to have been deposited in transgressive shallow-marine environments (Sage, 1973).

For both of these Paleocene units, Sage (1973) concluded that sediments were transported southwestward and were derived from a source area of granitic, gneissic, quartzitic, and felsic to intermediate volcanic rocks that was located to the northeast.

(3)	Shale and siltstone is 300-2,110 ft (90-646 m) thick, of "Meganos(?)” to "Capay(?)” age. These strata are mostly of shallow-marine origin, contain a basal conglomerate and sandstone and disconformably over-lie the older part of the sequence.

(4)	The top unit is composed mostly of sandstone, 1,400-2,500 ft (430-760 m) thick of "Domengine(?)” age. This unit disconformably overlies the shale of unit 3 and consists of a lower conglomerate overlain by fossiliferous sandstone, siltstone, and shale inferred to have been deposited in shallow marine environments﻿30

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

(Cushman and McMasters, 1936; Levorsen, 1947; Conrad, 1949; Bishop, 1950; Fantozzi, 1955; Martin, 1958).

SANTA MONICA MOUNTAINS

Marine and nonmarine strata of early Tertiary age crop out in various parts of the Santa Monica Mountains, but are difficult to correlate because of abrupt facies changes and complex structure. Paleocene strata crop out discontinuously in fault blocks in four main areas.

(1) In the easternmost part of the range is un-fossiliferous, nonmarine feldspathic sandstone and conglomerate about 300 ft (90 m) thick (Yerkes and others, 1965). (2) In the Topanga Canyon area to the east, fossiliferous conglomerate, sandstone, and shale is as much as 2,000 ft (600 m) thick (Campbell and others, 1970; Yerkes and others, 1971). Sage (1973) concluded that this sequence consists of alluvial fan deposits that grade upward into shallow marine and then into deeper marine deposits. (3) In the central part of the range in the Carbon Canyon area, conglomerate, sandstone, and shale is possibly as much as 2,000 to 8,500 ft (600-2,600 m) thick (Pelline, 1952; Carter, 1958; Champeny, 1961). However, this sequence may include some strata younger or older than Paleocene (R. H. Campbell, oral commun., October 1973). Sage (1973) interpreted the sequence as shallow submarine fan deposits. (4) In the western part of the range in the Solstice Canyon area, conglomerate, sandstone, and shale are as much as 1,650 ft (500 m) thick. The sequence contains interbeds of peaty shale and pisolitic claystone near the base at some localities. Sage (1973) inferred meandering river and lagoonal deposition in the lower part and shoreline and shallow marine deposition in the upper part. Sage (1973) concluded that these strata were derived from an area of granitic, gneissic, and felsic to intermediate volcanic rocks to the northeast and east, and transported southwestward into a subsiding and deepening marine basin.

The Eocene Llajas(?) Formation of Schenck (1931), about 1,200 ft (370 m) thick and of "Domengine” age, overlies the Paleocene strata with possible disconfor-mity. It consists of interbedded locally fossiliferous fine-grained sandstone and siltstone of shallow-marine origin, and includes some thin discontinuous beds of very coarse-grained sandstone and cobble conglomerate (Campbell and others, 1970; Yerkes and others, 1971).

ELSMERE CANYON AND GOLD CREEK AREAS

In Elsmere Canyon south of Newhall, strata of probable "Capay” to "Tejon” age about 1,000 ft (300 m) thick are faulted against granitic basement rocks (Oakeshott, 1958). Winterer (1954) divided the Elsmere Canyon sequence into a lower unit of massively bedded arkosic sandstone that contains pebbles of quartz and granitic

rock, a middle unit of silty shale interbedded with sandy limestone and conglomerate with clasts of slate and granitic rock, and an upper unit of very thickly bedded sandstone with interbeds of silty shale, large siltstone clasts, and pebbles of granitic rock. Because graded bedding is common in these strata, Winterer and Durham (1962) concluded that they were probably tur-bidites, noting, however, that the abundant molluscan fauna present suggested that the depth of water was not great.

Strata about 1,500 ft (460 m) thick of probable "Martinez” age crop out near Gold Creek. These deposits are mostly thickly bedded coarse-grained sandstone interbedded with some thin shales. Lenses of pebble conglomerate containing porphyritic volcanic, gneiss, quartzite, anorthosite!?), and limestone clasts are locally present. The sequence is thought to have been deposited at littoral depths along a rugged coastline (Oakeshott, 1958).

ELIZABETH LAKE CANYON AND VALYERMO AREAS

The Paleocene and Eocene(?) San Francisquito Formation is about 6,900 ft (2,100 m) thick in the Elizabeth Lake Canyon area and 4,000 ft (1,200 m) in the Val-yermo area (Dibblee, 1967). In both areas it unconform-ably overlies and is in fault contact with gneissic and granitic basement rocks; it is conformably overlain by Oligocene nonmarine strata in the Elizabeth Lake Canyon area and unconformably overlain by Miocene strata near Valyermo. The San Francisquito Formation consists of interbedded marine breccia, conglomerate, sandstone, siltstone, and shale that in both areas contain a "Martinez” molluscan megafauna in the lower part. Various subdivisions and interpretations of the origin of the formation have been made by Clements (1937), Pfaffman (1941), Herbert Harris (1950), Smith (1951), Johnson (1952), Miller (1952), Holwerda (1952), Szatai (1961), Setudehnia (1964), Sams (1964), Stanley (1966), Konigsberg (1967), and Sage (1973). The formation in both areas was interpreted by Sage (1973) to represent submarine fan and basin floor sediments deposited in an unrestricted, southwest-trending basin that progressively deepened during the course of sedimentation. He inferred a provenance composed of felsic to intermediate plutonic, gneissic, and porphyritic felsic volcanic rocks that lay nearby to the northeast.

CHANNEL ISLANDS

The marine lower Tertiary sequences on Santa Cruz and San Miguel Islands rest on Upper Cretaceous marine strata and are overlain by Oligocene marine strata. The sequence on Santa Cruz Island has been described by Rand (1931, 1933) and Doerner (1968, 1969), as consisting of three parts. (1) the Pozo Formation of Doerner (1969), is an Ynezian(?) to Bulitian﻿SOUTHWESTERN AREA

31

sandstone and siltstone 225 ft (70 m) thick containing fossiliferous calcareous lenses. The lower part of the formation is inferred to be inner shelf deposits that were transported southward (Merschat, 1968, 1971; Sage, 1973), and the upper part is inferred to be central shelf to upper bathyal deposits (Doerner, 1968). (2) The Canada Formation of Doerner (1969), 1,420 ft (430 m) thick, of Penutian to Narizian age, consists of shale and siltstone with minor amounts of fine-grained sandstone. The Canada Formation unconformably overlies the Pozo Formation and was deposited at central shelf to upper bathyal depths (Doerner, 1968) by southwest-ward-flowing currents (Merschat, 1971). (3) The Jolla Vieja Formation of Doerner (1969), is a sandstone and conglomerate of Narizian age as much as 880 ft (270 m) thick, containing minor amounts of fine-grained sandstone and inferred by Doerner (1968) to have been deposited at abyssal depths by southwestward-flowing currents.

The San Miguel Island sequence is composed of two members (Weaver, 1969). (1) Undifferentiated Pozo-Canada Formations, shale, sandstone and conglomerate are 2,250 ft (685 m) thick and of Ynezian to Ulatisian age. The lower part is thought to have been deposited on the lower part of a deep-sea fan by north-northwest- and south-southeast-flowing turbidity currents and grain flows (Sage, 1973): (2) The South Point Formation of Weaver and Doerner (1969) is 2,920 ft (890 m) thick and of Ulatisian to Narizian age. It consists of sandstone and conglomerate inferred to have been deposited by northeastward-flowing turbidity currents and grain flows, and siltstone and mudstone inferred to have been deposited by both traction currents and the vertical settling of pelagic detritus. The South Point Formation is thought to have been deposited on the upper part of a deep-sea fan (Parsley, 1972). Outer shelf to upper bathyal conditions with free access to the open ocean are indicated by foraminiferal faunas in both formations (Weaver and Doerner, 1969); the source area was located to the northeast and east and consisted of granitic and metamorphic rocks (Parsley, 1972; Weaver and Doerner, 1969).

A conformable sequence of lower Tertiary strata on Santa Rosa Island according to Weaver and Doerner (1969) starts with (1) the Canada Formation, shale and conglomerate of probable Ynezian to Ulatisian age and present only in subsurface. (2) The South Point Formation, 700 ft (210 m) thick in outcrop and 3,450 ft (1,050 m) thick in subsurface, is of Ulatisian and Narizian age and consists of fine- to coarse-grained sandstone rhythmically interbedded with siltstone and mudstone. It is inferred to have been deposited at bathyal depths as a deep-sea fan in an unrestricted basin by mass flows that moved northwestward; the source area is thought to have consisted of quartz-monzonitic to granodioritic

plutonic rocks or their derivative sediments (Erickson, 1972). (3) The Cozy Dell Formation is mudstone and shale of Narizian age and 410 ft (130 m) thick, deposited at bathyal depths in an unrestricted basin. On top is (4) the nonmarine Sespe Formation.

SANTA ANA MOUNTAINS AND SAN JOAQUIN HILLS

Lower Tertiary marine and nonmarine strata rest unconformably on both Upper Cretaceous sedimentary rocks and granitic basement rocks in the San Joaquin Hills and northern Santa Ana Mountains, and extend southeastward along the Elsinore fault toward Lake Elsinore (Woodring and Popenoe, 1945; Schoellhamer and others, 1954; Vedder and others, 1957; Engel, 1959; Gray, 1961; Durham and Yerkes, 1964; Yerkes and others, 1965; Vedder, 1970b).

The Paleocene Silverado Formation, 1,150-1,875 ft (350-570 m) thick, has a lower unit consisting of a basal nonmarine conglomerate overlain by a coarse-grained pebbly arkosic sandstone that contains interbedded siltstone, carbonaceous shale, clayey grit, red pisolitic sandy claystone, and lignite. Sage (1973) inferred deposition of the basal conglomerate in a braided, meandering river system, and deposition of the overlying sediments in fluvial and lagoonal environments and as residual deposits on a stable area of low relief that had been subjected to prolonged chemical weathering. The upper unit consists of fine- to medium-grained fossiliferous sandstone thought to have been deposited in brackish to shallow-marine environments during a transgression of the sea (Yerkes and others, 1965). Paleocurrents indicating sediment transport toward the south-southwest were determined by Sage (1973), who inferred that the source area was to the northeast and consisted of granitic and felsic to intermediate volcanic rocks.

The Santiago Formation, 300-2,700 ft (90-820 m) thick, overlies the Silverado Formation with apparent conformity, although a hiatus representing early Eocene time separates the two. It consists of: (1) a basal shallow-marine conglomerate and sandstone that contains clasts of porphyritic volcanic, sedimentary, and granitic rocks, quartzite, quartz, chert, aplite, and conglomerate, with calcareous algae and other marine fossils in its upper part; (2) a shallow-marine sandstone; and (3) a nonmarine regressive pebbly sandstone. Mol-luscan and foraminiferal faunas indicate "Domengine” and Ulatisian ages, respectively, for the Santiago Formation (Woodring and Popenoe, 1945; Gray, 1961; Yerkes and others, 1965).

SAN NICOLAS ISLAND

Eocene marine conglomerate, pebbly mudstone, sandstone, siltstone, and mudstone 3,445 ft (1,050 m) thick crop out on San Nicolas Island (Vedder and Nor-﻿32

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

ris, 1963). These strata are of Ulatisian and Narizian age and are tentatively correlated with the South Point Formation of San Miguel and Santa Rosa Islands on the basis of bathyal foraminiferal faunas and rare mollusks (Weaver, 1969). The sandstones are arkosic, containing 40-60 percent quartz, 48 percent feldspar (primarily oligoclase), and 8-20 percent metavolcanic lithic fragments (Vedder and Norris, 1963). Paleocurrent measurements by Cole (1970,1973) indicate sediment transport toward the south-southwest; he inferred that deposition took place on part of a large submarine delta-fan complex principally by grain-flow processes but also by subaqueous mudslides, turbidity currents, and high-energy traction currents.

WESTERN PENINSULAR RANGES

Nearly flat-lying shallow-marine and nonmarine Eocene strata as much as 1,600 ft (490 m) thick crop out along the western flank of the Peninsular Ranges in coastal areas north of San Diego. These strata uncon-formably overlie Upper Cretaceous marine strata and are unconformably overlain by upper Tertiary strata (Peterson, 1970, 1971; Moore and Kennedy, 1970; Peterson and Nordstrom, 1970; Kennedy and Moore, 1971; Gibson and Steineck, 1972a). Kennedy (1971) and Kennedy and Moore (1971) divided the sequence in the San Diego area into the La Jolla and Poway Groups, assigning ages to various formations on the basis of coccolith studies by Bukry and Kennedy (1969), mollus-can studies by Hanna (1926) and Moore (1968), and vertebrate studies by Golz (1971) and Golz and Kennedy

(1971).

The La Jolla Group consists of (1) the Mount Soledad Formation, marine conglomerate and sandstone of early(?) and middle Eocene age 230 ft (70 m) thick; (2) the Delmar Formation, marine sandstone and shale of middle Eocene age, 100-200 ft (30-60 m) thick, a probable lagoonal deposit; (3) the Torrey Sandstone, medium-to coarse-grained sandstone of "Domengine” age, 200 ft (60 m) thick, a probable shallow-marine deposit; (4) the Ardath Shale, richly fossiliferous silty shale of "Domengine” age, 230 ft (70 m) thick and considered by Gibson and Steineck (1972a) to have been deposited at depths greater than 1,500 ft (460 m); (5) the Scripps Formation, sandstone with subordinate amounts of conglomerate and siltstone of middle and late Eocene age, 220 ft (65 m) thick; and (6) the Friars Formation, nonmarine sandstone of middle and late Eocene age, 115 ft (35 m) thick.

The Poway Group consists of (1) the Stadium Conglomerate, primarily nonmarine massive cobble and boulder conglomerate of middle(?) and late Eocene age, 165 ft (50 m) thick and containing abundant Poway-type clasts; (2) the Mission Valley Formation, fine-grained sandstone with conglomerate in the upper

part, of late Eocene ("Tejon”) age and 190 ft (58 m) thick, thought to have been deposited in shallow marine and nonmarine environments (Kern, 1974); and (3) an unnamed nonmarine formation of late Eocene age, 33 ft (10 m) thick.

The Eocene sequence according to Kennedy and Moore (1971) records an early(?) to late Eocene transgression, with the Mount Soledad, Delmar, Torrey, and Ardath Formations representing successive basal conglomerate, lagoonal, barrier-beach, and offshore-shelf facies, respectively, followed by a late Eocene regression, with the Scripps, Friars, and Stadium Formations representing nearshore shelf and nonmarine facies. The cycle ended with renewed transgression represented by the Mission Valley Formation and finally regression represented by the uppermost unnamed nonmarine conglomerate formation.

LAKE ELSINORE, LAKE HENSHAW, AND JACUMBA VALLEY AREAS

Lower Tertiary nonmarine gravels that are locally auriferous crop out in the interior parts of the Peninsular Ranges at several scattered localities. The northernmost gravels crop out near Santa Rosa Ranch in the northeastern Peninsular Ranges about 10 miles (16 km) south of Lake Elsinore, and have been informally called the Santa Rosa gravels (Minch, 1970); they unconformably overlie granitic and metamorphic basement rocks and are overlain by Quaternary volcanic rocks. A second group of gravels crop out adjacent to the Ballenas Valley in the central Peninsular Ranges south of Lake Henshaw, and have been informally called the Ballenas gravels (Minch, 1970, 1971); they unconformably over-lie granitic basement rocks and are overlain by Quaternary alluvium. A third group of gravels crop out near the Jacumba Valley in the southeastern Peninsular Ranges near the Baja California border, and have been informally called the Jacumba gravels by Minch (1970) and Minch and Abbott (1973); they unconformably overlie pre-Eocene conglomeratic sandstone and are overlain unconformably by Miocene volcanic and nonmarine sedimentary rocks. None of the gravels has been accurately dated, but they are considered to be of middle or possibly late Eocene age on the basis of regional stratigraphic relations.

Each of the gravels is thought to have been deposited by major Eocene rivers (Santa Rosa, Ballenas, and Jacumba rivers) that flowed southwestward and emptied into the shallow sea located to the west along the present western edge of the Peninsular Ranges (Minch, 1971, 1972). The Eocene Jacumba river is inferred to have been a southward-flowing tributary to the larger La Pumerosa-Las Paluma river of Eocene age that was located in northern Baja California.

Congomerate clasts in the gravels of the Lake Elsi-﻿EARLY TERTIARY HISTORY OF THE SAN ANDREAS FAULT

33

nore and Lake Henshaw areas consist of quartzite, Poway-type rhyolite and dacite porphyries, epidotized metavolcanic rocks, and epiclastic metasedimentary rocks; however, in the gravels of the Jacumba Valley area, the clasts consist of quartzite, epidotized metavolcanic and metasedimentary rocks, and granitic rocks, without Poway-type rhyolite and dacite porphyries (Minch, 1970, 1972). Because only a partial suite of the Poway-type clast assemblage is present in the Jacumba gravels, Minch (1970) inferred that these gravels were deposited close to the boundary between Poway-type clast assemblages in Eocene rocks to the north, and quartzite-chert-argillite clast assemblages to the south.

NORTHERN BAJA CALIFORNIA

The general stratigraphic distribution of lower Tertiary sedimentary rocks in the Peninsular Ranges continues southward into northern Baja California. Three additional nonmarine gravels thought to have been deposited by southwestward-flowing early Tertiary river systems have been recognized by Minch (1970, 1971) in the Peninsular Ranges of northern Baja. The southernmost ones, the Campo Nacional and El Rodeo Rivers, contain clasts of gray to black quartzites, cherts, argillites, gneisses, and chlorite schists, but no Poway-type clasts. The northernmost river gravels are located about 10 miles (16 km) south of the California border and contain a partial suite of the Poway-type clast assemblage; these gravels were deposited by the La Pumorosa-Las Palmas River, of which the Jacumba River is thought to have been a tributary.

Middle Eocene sedimentary strata of shallow-marine character extend discontinuously southward from San Diego along the northwestern coast of Baja California (Allison, 1966; Minch, 1967; Flynn, 1970a, b). The strata rest unconformably on metavolcanic basement rocks or Upper Cretaceous marine sedimentary rocks and consist of (1) the Delicias Formation of Flynn (1970a), mudstone and siltstone overlain by fine-to medium-grained sandstones about 300 ft (90 m) thick, of "Domengine” age, thought to have been deposited in restricted marginal marine (brackish?) environments; and (2) the Buenos Aires Formation of Flynn (1970a), conglomerate overlain by sandstone, about 500 ft (150 m) thick and considered of "Domengine” age. It rests with angular unconformity on the Delicias Formation and is thought to have been deposited in shallow marine environments. Conglomerate clasts within the Buenos Aires consist of quartzite, porphyry, volcanic breccia, dacite, and granitic rocks.

EARLY TERTIARY HISTORY OF THE SAN ANDREAS FAULT

Movements along the San Andreas fault have

strongly influenced the tectonic and paleogeographic evolution of early Tertiary California and the pattern, style, and loci of sedimentation. Previous paleogeographic reconstructions by Reed (1933) and Reed and Hollister (1936) have been largely invalidated by convincing evidence for far more offset along the San Andreas and related faults in the Coast Ranges than was formerly believed. We suggested earlier that the San Andreas fault began to move in a right-lateral sense during the Late Cretaceous. What is known of its subsequent history is briefly summarized below.

Hill and Dibblee (1953) observed numerous right-lateral offsets of Cretaceous to Quaternary geologic features along the San Andreas fault and noted that progressively older rocks were apparently offset by progressively greater distances. They concluded that the San Andreas fault had moved steadily during the past 100 million years. Other stratigraphic, sedimen-tologic, and paleontologic studies have provided additional evidence of continuous offset. However, Dickinson and Grantz (1968) concluded that while convincing evidence existed for relatively continuous movement from early Miocene to the present, the evidence for pre-Oligocene offset was only suggestive.

An additional problem is the apparent disparity between the total offsets in northern and southern California. Evidence from the north suggests offset of more than 325 miles (520 km), while evidence from the south suggests that a total of no more than about 200 miles (320 km) of offset has accumulated along the combined San Gabriel and San Andreas faults (Crowell, 1962, 1973a).

More recent studies in'central and northern California have demonstrated that lower Miocene rocks about 22 and 23.5 m.y. old are offset between 185 and 200 miles (300-320 km) (Bazeley, 1961; Turner, 1968,1969; Turner and others, 1970; Huffman, 1972a, b; Huffman and others, 1973; Matthews, 1972,1973a, b). A preliminary study of Oligocene faunal and paleogeographic elements suggests that Oligocene rocks have been offset about the same distance, 190-200 miles (305-320 km) (Addicott, 1968). Detailed studies of the Eocene Butano Sandstone of the Santa Cruz Mountains and the Point of Rocks Sandstone of the northern Temblor Range indicate that they are congeneric and have been offset by about 190 miles (305 km) since mid-Narizian time, about 44 m.y. ago (Clarke and Nilsen, 1972, 1973; Clarke, 1973). Nilsen, Dibblee and Simoni (1974) have suggested that the Paleocene and Eocene German Rancho Formation of the Gualala area is congeneric with and offset about 190-200 miles (305-320 km) along the San Andreas fault from the Lodo Formation and its Cantua Sandstone Member in the Vallecitos area. In addition, work in progress by T. H. Nilsen and M. H.﻿34

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Link suggests that Eocene and Oligocene strata of the northern Gabilan Range and northern Santa Lucia Range are offset 190-200 miles (305-320 km) from equivalent strata in the San Emigdio Mountains. A variety of evidence suggests that Upper Cretaceous sedimentary rocks near Gualala have been separated from their source area by about 350 miles (560 km), and that mid-Mesozoic basement rocks are offset between 325 and 450 miles (520-720 km) (Wentworth, 1966, 1968; Ross, 1970; Ross and others, 1973).

These data thus suggest a history of intermittent rather than continuous movement on the San Andreas fault: (1) right-lateral strike-slip faulting with 135 to 260 miles (220-420 km) of offset in central and northern California during the Cretaceous and (or) early Paleocene; (2) inactivity from at least late Paleocene to early Miocene, and (3) renewed right-slip movement with about 190 miles (305 km) of offset along the present San Andreas fault since the early Miocene (fig. 4). Kistler, Peterman, Ross, and Gottfried (1973) have suggested a similar history on the basis of geochemical studies of basement rocks within the Salinian block.

In southern California, rocks of Precambrian to about middle Miocene age are displaced right-laterally an equal distance, about 200 miles (320 km), along the present San Andreas fault (Crowell, 1962, 1973a; Minch, 1971; Merriam, 1972). The Late Cretaceous and Paleocene episode of right-lateral slip evident in central and northern California is not yet recognized in southern California, where the displacements are apparently entirely post-middle Miocene in age. The presence of a "proto-San Andreas” fault, which bypassed the present San Andreas fault in southern California, and along which about 200 miles (320 km) of offset accumulated by late Oligocene time, was suggested by Suppe (1970) to explain the apparent disparity in offsets between northern and southern California. He proposed that the Newport-Inglewood fault west of the present San Andreas fault might represent this ancestral fault trace. Others believe that it may be located still farther west, or perhaps even east of the present San Andreas fault. Gastil, Phillips, and Rodriquez-Torres (1972) considered it to be near the present Gulf of California, Gastil and Jensky (1973) beneath the Trans-Mexican volcanic belt, and Minch and James (1974) proposed that a major fault along the east coast of central Baja California is the proto-San Andreas fault.

The interpretation of magnetic anomalies on the ocean floor to the west and the reconstruction of the history of plate movements in the Pacific also suggests that the California continental margin may have undergone two major episodes of right-lateral strike-slip faulting. Studies of sea-floor spreading data in the eastern Pacific region suggest that the present San Andreas fault system is a transform fault along which the Pacific

10	20	30	40	50	60	70

AGE IN MILLIONS OF YEARS

Figure 4.—Inferred history of offset along the San Andreas fault in central California. Data points include: (1) Dickinson and others (1972); (2) Huffman (1972 a, b); (3) Turner and others (1970); (4) Turner and others (1970) and Huffman (1970); (5) Addicott (1968); (6) Clarke and Nilsen (1972,1973); (7) Nilsen and others, 1974; (8) Ross and others (1973). Locations of Bodega Head (BH), Point Arena (PA), and Shelter Cove (SC) (about 30 miles (48 km) south of Cape Mendocino) shown on figures 1 and 2. Age estimates of time boundaries from Berggren (1972).

and North American plates are moving past one another in a right-lateral sense (Wilson, 1965a, 1965b; Vine, 1966; Morgan, 1968; McKenzie and Morgan,

1969)	. Atwater (1970) and Atwater and Molnar (1973) concluded that the present San Andreas system is no more than 30 m.y. old; however, Atwater’s (1970) reconstruction of earlier plate motions suggests that right-lateral faulting took place along the California continental margin during the period from about 80 to 60 m.y. ago (fig. 5).

Her model suggests that the Kula plate, which has now been completely subducted beneath the Aleutian Islands and mainland Alaska (Grow and Atwater,

1970)	, was sliding past the North American plate at this time. The history of the California continental margin as deduced from her model consists of (1) Mesozoic subduction, during which Franciscan rocks were underthrust beneath the Great Valley sequence, (2) right-lateral offset along a transform fault, perhaps the "proto-San Andreas fault” of Suppe (1970), during Late Cretaceous and early Tertiary; (3) subduction, without right-lateral displacement, during the period from about Paleocene to early Miocene time, and (4) right-lateral offset along a transform fault, the present San Andreas system, from early Miocene to the present.

We believe that a proto-San Andreas fault along which 135 miles (220 km) or more of offset occurred prior to the Eocene is consistent with geologic evidence﻿EARLY TERTIARY HISTORY OF THE SAN ANDREAS FAULT

35

20 m.y.

EXPLANATION


Line of spreading; arrows show relative directions of motion

i y»y-H-

Line of subduction; arrows on underthrusting plate

Transform fault; arrows show relotive directions of motion

Motion of plates relative to North America

PACIFIC PLATE

Figure 5.__Mesozoic and Cenozoic plate relations in the western

Pacific Ocean (modified from Atwater, 1970, fig. 18). North American plate is held fixed, and large arrows show motion relative to it. Captions give time in millions of years before present. Pacific-North American motion assumed constant at 6 cm/yr in a horizontal direction for last 20 m.y., 4 cm/yr taken up by near-coast faults and 2 cm/yr by inland faults. WH = Whitehorse; S = Seattle; SF = San Francisco; LA = Los Angeles; MZ = Mazatlan.

from central and northern California, and provides the most satisfactory means of reconciling the differing amounts of total offset in northern and southern California. Moreover, the Late Cretaceous and Paleocene period of right-lateral slip indicated by onshore geologic evidence in central and northern California corresponds well in type, location and timing of displacement to Atwater’s model involving Kula plate motion, and supports the contention that the San Andreas is part of a complex transform fault system (Hill, 1971; Dickinson and others, 1972; Hill, 1974).

The location of a proto-San Andreas fault is problematical. If it was a transform fault forming the boundary between the Kula and North America plates, its orientation probably differed from that of the present San Andreas system, as the directions of movement of the Kula and Pacific plates with respect to the North American plate are unlikely to have been identical. Atwater (1970) shows the directions of movement to be slightly different (fig. 5). In addition, sedimentation and deformation in Eocene and later time have been exten-

sive in this region, undoubtedly obscuring the presence of an older fault and older offsets.

It seems probable that an ancestral San Andreas fault zone was located somewhere to the west of the present trace of the fault in central California. Unusual and remarkably similar sequences of Jurassic gabbros (Ross, 1970) overlain by Eocene to early Miocene sedimentary rocks are present east of the fault near Eagle Rest Peak in the San Emigdio Range and west of the fault near San Juan Bautista. Should these sequences prove to be correlative, as suggested by Huffman (1972a), Clarke (1973, p. 231-232) and Clarke and Nilsen (1973, p. 362), it would indicate that the Gabilan and San Emigdio basement terranes originally constituted a single block which was not offset until after early Miocene time. This would limit displacement along the present trace of the fault in central California to post-early Miocene time and a maximum distance of about 200 miles (320 km), thus indicating that the proposed proto-San Andreas fault in this region did not coincide with the present San Andreas fault.

Subsequent study may establish that proto-San Andreas fault displacement is represented in part by Late Cretaceous and early Tertiary offset along the Reliz-Rinconada fault of Dibblee (1972a), as suggested by Kistler and others (1973); this fault parallels the east flank of the Santa Lucia Range, eventually coinciding with the Nacimiento fault southward to the Big Pine fault (figs. 1 and 2). However, no evidence for pre-Miocene right-lateral slip along this fault has been presented (Dibblee, 1972a), and the proto-San Andreas fault may be one of several other buried faults in the area between the Gabilan and Santa Lucia Ranges. In the San Francisco Bay region, it may be partly represented by the Pilarcitos fault, which separates Franciscan and granitic basement rocks and was probably an active trace of the San Andreas system before the Pliocene (Dibblee, 1966b, p. 383). To the south, it probably bypasses present-day southern California. It may extend beneath the Transverse Ranges, where it cannot be recognized because of subsequent deformation and burial, and thence southward into the continental borderland of southern and Baja California.

In summary, we think it probable that two episodes of right-lateral strike-slip faulting have occurred in the California continental margin since the emplacement of Mesozoic basement rocks. During latest Cretaceous and Paleocene time, right-lateral slip of 135 to 260 miles (220-420 km) occurred along a proto-San Andreas fault which probably paralleled, but did not coincide with the present San Andreas fault in central and northern California; this ancestral fault extended southward into the southern California borderland. Displacement along the proto-San Andreas fault proba-﻿36

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

bly ceased during Paleocene or earliest Eocene time, possibly with a tectonic change from right-lateral faulting to subduction along the continental margin. During the remainder of Eocene time, the Salinian block west of the proto-San Andreas fault jutted out perhaps 150 miles (240 km) or more from the continental margin as a long peninsula or island chain, forming a continental borderland with deep marine basins to the east and west (fig. 5). Subduction may have continued west of this borderland until right-lateral displacement recommenced along the present San Andreas fault some time after the early Miocene (Atwater, 1970).

EARLY TERTIARY PALEOGEOGRAPHY INTRODUCTION

Our paleogeographic synthesis of early Tertiary California differs from earlier syntheses by Reed (1933) and Reed and Hollister (1936) in that we have incorporated the following concepts: (1) right-lateral displacements that total about 190-200 miles (305-320 km) along the San Andreas fault during the past 20 million years, offsetting lower Tertiary strata that were originally contiguous; (2) significant displacements along other lateral faults, including the Reliz-Rinconanda fault (Dibblee, 1972a), the Garlock fault (Smith, 1962), the Big Pine and other faults in the Transverse Ranges (Hill and Dibblee, 1953), the San Gabriel fault (Crowell, 1962), and offshore faults in the southern California borderland area (Yeats, 1968; Yeats and others, 1974; Howell and others, 1974); (3) right-lateral displacements that totalled 135-260 miles (220-420 km) along a proto-San Andreas fault before or during Paleocene time, resulting in the emplacement of a long borderland underlain by continental crust to the west of the continental margin (fig. 6); and (4) many thick sequences of sandstone and conglomerate, previously considered to be of shallow marine origin, appear on the basis of modern sedimentologic and paleontologic criteria to be submarine fan deposits that accumulated at bathyal or greater depths.

Our reconstruction of the paleogeography is drawn largely from the previously cited published reports and unpublished theses, and we are indebted to these authors. Some units and areas have been thoroughly studied, whereas others have been examined only in reconnaissance. We encourage future studies to test and refine our synthesis, especially those aimed at a better understanding of the sedimentary processes and environments, sediment dispersal patterns, location of source areas, and those directed toward unraveling the complicated post-Eocene tectonic history of western California.

The paleogeography of California changed considerably during early Tertiary time. In the early Paleocene,

the inferred proto-San Andreas fault was probably active; during at least late Paleocene to late Eocene time, movement along it had ceased. Within the borderland region, basins developed at different times and underwent different histories of development. Some basins persisted throughout the early Tertiary, whereas others lasted for only relatively short periods of time. Sedimentation on deep-sea fans was probably rapid, and many fans were relatively short lived. Source areas also changed abruptly, indicating that major tectonic uplift occurred contemporaneously with sedimentation in adjoining basins. All of these features are characteristic of a transform plate boundary, and one of our purposes in this paper is to demonstrate the types and patterns of tectonism and sedimentation characteristic of plate boundaries marked by transform faults. These tectonic and sedimentary patterns can also be studied in the later history of the San Andreas fault region and in some of the modern basins and uplifted areas along the fault.

Despite the rapid rate of tectonic change during the early Tertiary along the transform boundary, we have compiled a generalized paleogeographic map of early Tertiary California that groups Paleocene and Eocene elements together (fig. 7). The map, which incorporates palinspastic restorations of lateral movements along the San Andreas and other post-Eocene faults, is thus a composite of all or most of the major paleogeographic elements present in early Tertiary California. It may not be fully correct in all the details, but we feel that it presents a reasonably accurate assembly of the paleogeographic elements based on the many published and unpublished studies summarized earlier. From the descriptions of these paleogeographic elements that follow, the reader will be able to place each element in its proper time framework within the early Tertiary.

SOURCE AREAS

The major source areas for the lower Tertiary sediments were underlain by (1) granitic rocks, (2) various metamorphic rocks that included granitic gneisses, schists, quartzites, and metavolcanic rocks, and (3) fel-sic to intermediate volcanic rocks. In some areas, erosion of older sedimentary rocks, including sandstones, conglomerates, shales, mudstones, siltstones, and cherts provided sediment. Some of the volcanic and metamorphic detritus was derived from erosion of Upper Cretaceous sedimentary rocks; in fact, resistant and well-rounded pebbles and cobbles of chert, quartzite, and volcanic rocks may have been derived from several earlier cycles of erosion and sedimentation, and thus represent recycled clastic detritus.

The source areas were located both westward in the Salinian block and eastward in the Sierra Nevada,﻿EARLY TERTIARY PALEOGEOGRAPHY

37

EXPLANATION

FR

Franciscan rocks GVS

Great Valley sequence SN

Sierra Nevada GV

Great Valley SB

Salinian block P-SAF

Proto-San Andreas fault

—V-----▼	*	■

Subduction zone

Teeth on upper plate; queried where not known to have been active or possibly

incorrectly located

\ 'N "s'n'V'V'N Western edge of continental crust locally expressed as a continental slope

Upland source area	Ocean floor

Directions of sediment transport Areas of thick sedimentation

Direction of right—lateral slip along proto —San Andreas fault

Figure 6.—Diagrammatic sketch showing the early Tertiary tectonic development of central California, formation of the continental borderland, and influence of the proto-San Andreas fault.

Great Basin, eastern Transverse Ranges, Mojave Desert, Peninsular Ranges, and Salton Trough provinces, as well as the Sonoran Desert region of northern Mexico (fig. 1). The source rocks in the western and eastern source areas were generally similar; as a result, almost all of the lower Tertiary sandstones in California are arkosic in composition and variations are relatively minor. Where paleogeographic, paleocurrent, and stratigraphic data are ambiguous, it may be impossible to distinguish those sandstones derived from eastern source areas from those derived from western source areas. The distinction may be equally difficult for con-

glomeratic strata, because the almost ubiquitous appearance of granitic, volcanic, and quartzitic clasts in so many lower Tertiary conglomerates may prevent the distinction of eastern from western source areas. Similarly, the mineralogy of various shale, mudstone, and claystone units may not permit distinction of source areas based on our present knowledge of what the source areas were like.

In some lower Tertiary deposits of central California, source areas located to the east have been inferred on the basis of the mineralogy of quartz-rich, anauxitic sandstones and the presence of andalusite and stauro-﻿38

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

0

b

0

GARLOCK fault PRESENT TRACE)

N

PACIFIC

OCEAN

50

I

100 MILES

50	100 KILOMETRES

Figure 7.—Generalized paleogeographic map of early Tertiary California, based on reversal of 190 miles (305 km) of post-Eocene right-lateral offset along the present San Andreas fault. The prominent paleogeographic features of both Paleocene and Eocene age are shown on the map; paleogeographic changes between the early Paleocene, when the proto-San Andreas fault may have been active, and the end of the Eocene are not shown. The present locations of several cities and the Garlock fault are included for orientation purposes. Abbreviations: SAC-Sacramento; SF-San Francisco; BAK-Bakersfield; MON-Monterey; LA-Los Angeles; SD-San Diego.﻿EARLY TERTIARY PALEOGEOGRAPHY

39

lite in the heavy mineral assemblages. These inferences may prove to be valid, but not enough detailed work has been completed yet in central California to clearly demonstrate it. In southern California, the presence of Poway-type clasts has been used to demonstrate an eastern source area for many lower Tertiary deposits.

Franciscan rocks constituted an additional minor source that locally supplied detritus at various times in the northern Coast Ranges (Middle Mountain and Rice Valley areas and possibly within the "coastal belt” part of the Franciscan assemblage), in the central Coast Ranges (Mount Diablo, Orestimba, Tesla, Vallecitos, and San Jose areas), and in the western Transverse Ranges (western Santa Ynez Mountains north of the Santa Ynez fault). In these areas, Franciscan sources have been clearly demonstrated; in other areas, Franciscan sources have been suggested on the basis of minor amounts of glaucophane in heavy mineral assemblages and cherts of Franciscan affinity in conglomerate clast assemblages.

In summary, a great deal of additional mineralogic and petrographic work will be required before we can easily distinguish sediments derived from the Salinian block, the Sierra Nevada and other eastern source areas, and the Franciscan. Detailed data are needed on the composition of conglomerate clasts, feldspars and lithic fragments in the arkosic sandstones, clay minerals, and heavy mineral suites.

EASTERN NONMARINE DEPOSITS

The easternmost lower Tertiary sedimentary rocks throughout California generally consist of nonmarine facies, indicating the presence of a continental upland area to the east. The coarseness, volume, and widespread distribution of conglomerate, sandstone, and local breccia derived from this terrane suggest that it had considerable relief and occupied a large area. Sediment transport was principally toward the west and southwest; eastern source areas have been determined or inferred for fluvial deposits in the northern Sacramento Valley (Butte Gravel Member of the Sutter Formation), northern Sierra Nevada (prevolcanic gravels and nonmarine parts of the lone Formation near and south of Oroville), southern Sierra Nevada and eastern San Joaquin Valley (Walker Formation), San Emigdio and western Tehachapi Mountains (Tecuya Formation), eastern Santa Monica Mountains, Santa Ana Mountains and San Joaquin Hills (Silverado and Santiago Formations), central Peninsular Ranges (Santa Rosa, Ballenas, and Jacumba River gravels of Minch, 1970), western flank of the Peninsular Ranges (regressive Stadium Conglomerate), and northern Baja California (La Pumorosa-Las Palmas, Campo Nacional, and El Rodeo River gravels of Minch, 1970).

The lower Tertiary fluvial deposits in most areas rest unconformably on Upper Cretaceous marine strata or

Mesozoic granitic and metamorphic basement rocks. The erosional surface has variable relief, ranging from high in some areas where it is topographically very irregular and the thickness of the overlying fluvial deposits changes abruptly, to low in other areas where fluvial deposits of uniform thickness are widespread. In the northern Sierra Nevada, Peninsular Ranges, and northern Baja California, fluvial gravels crop out in long sinuous patterns that represent the channels of major westward-flowing rivers cut into the underlying basement rocks.

The eastern continental upland to the east that was the principal source of sediments varied in relief, morphology, and composition both areally and through time. Tropical climates and deep lateritic weathering are suggested during early and middle Eocene time by the presence of quartzose, anauxitic sandstone lacking in feldspar and the scarcity of clasts of granitic rock in the lone Formation and prevolcanic gravels of the northern Sierra Nevada, Mount Diablo and adjacent Great Valley area, Santa Monica Mountains, Santa Ana Mountains, and western and central Peninsular Ranges. Pisolitic claystones associated with these deposits in these areas are probably residual accumulations on the deeply weathered surfaces. The conglomerate clasts in these strata are primarily types resistant to chemical weathering: in northern areas they are primarily quartz, chert, quartzite, and low-grade metamorphic rock; in the Peninsular Ranges, quartzite, metavolcanic and metasedimentary rock, and Poway-type rhyolite and dacite clasts; and in northern Baja California, quartzite, chert, argillite, and gneiss.

In contrast, the younger nonmarine deposits of late Eocene and Oligocene age that flank the continental upland consist of arkosic and lithic sandstones that do not contain anauxite, and conglomerates with abundant clasts of granitic rock as large as boulder size. These deposits probably represent broad alluvial fan complexes that fringed coastlines, rather than individual river channel deposits. They indicate that relief was probably higher, erosion more rapid, and physical weathering more dominant than chemical weathering, resulting in little, if any, development of laterites.

The Goler and Witnet Formations of the southern Tehachapi and El Paso Mountains are probably alluvial fans deposited in intramontane basins located within the eastern continental upland area. Dibblee (1967) suggested that these units were deposited in a long, continuous, linear lowland that separated upland areas to the north and south. The coarseness, thickness, and nature of the deposits suggests deposition in a fault-bounded basin in which sedimentation occurred contemporaneously with tectonic uplift. Detritus was derived primarily from the south edge of the basin, located along the northern edge of the Mojave Desert region. The orientation of the linear lowland parallel to the﻿40

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

present trend of the Garlock fault suggests that a zone of structural weakness and possible precursor to the modern Garlock fault may have been present in the area in the early Tertiary. These data suggest that the Garlock fault zone may have been a possible transform fault boundary even earlier than suggested by Davis and Burchfiel (1973), and that movement along it may have been initiated during the early Tertiary. The deposits of other early Tertiary intramontane basins which may have been present within the eastern source areas have not been preserved.

Most of the lower Tertiary fluvial deposits are inferred or known to be primarily Eocene rather than Paleocene. Paleocene nonmarine strata have been reported only from the Las Llajas-Simi Hills-Santa Susanna Mountains, Santa Monica Mountains, Santa Ana Mountains-San Joaquin Hills, La Panza Range, and possibly the Tehachapi and El Paso Mountains areas. The lack of recognized Paleocene nonmarine strata may reflect the general paucity of fossil remains in the early Tertiary nonmarine strata or erosion of Paleocene deposits prior to deposition of the extensive Eocene strata of western California. However, it probably also reflects profound paleogeographic changes in the eastern source region and surrounding areas in Paleocene and Eocene time. Paleocene marine strata to the west are generally fine grained, except for those conglomerate and sandstone units derived from western source areas. Thus, Paleocene time was probably characterized primarily by low relief and little deposition adjacent to or within the eastern source areas; active tectonism and sedimentation was taking place primarily to the west in the continental borderland area. Major uplift of the eastern source areas during Eocene and Oligocene time resulted in westward transport and deposition of large volumes of coarse-grained nonmarine sediment.

SHALLOW MARINE SHELF DEPOSITS

Nonmarin'e strata in the east grade laterally westward into shallow-marine sedimentary strata that appear to have been mostly deposited along a narrow northwest-southeast trending continental shelf west of the continental landmass. The shelf averaged 10-50 miles (16-80 km) in width, and shelf deposits range from about 500 to 4,000 ft (150-1,200 m) in thickness. The continental shelf east of the proto-San Andreas fault appears to have been relatively straight, continuous, and unbroken by faulting throughout most of its extent (north of the Tehachapi Mountains and south of the Santa Monica Mountains), in sharp contrast to the disrupted borderland area west of the proto-San Andreas fault (fig. 7). These shallow marine shelf deposits are preserved along the western flank of the northern and central Sierra Nevada ("Dry Creek” and lone For-

mations), in klippen that rest on Franciscan rocks in the Clear Lake, Rice Valley, Middle Mountain, and Round Valley areas of the northern Coast Ranges, in subsurface beneath the Sacramento Valley and in the Mount Diablo area (Martinez, Meganos, Capay, and Domen-gine Formations), in subsurface beneath the western San Joaquin Valley and in adjacent outcrops of the Coast Ranges (Laguna Seca, Tesla, Yokut, Avenal, and Domengine Formations), in subsurface beneath the eastern San Joaquin Valley (Famosa sand), in the western Tehachapi and San Emigdio Mountains (shallow marine facies of the Tejon Formation), in the Pine Mountain and Piru Creek areas, in some of the strata in the Gold Creek, Las Llajas Canyon, Simi Hills, Santa Susanna Mountains, and Santa Monica Mountains areas, in the Santa Ana Mountains and San Joaquin Hills areas (marine strata of the Silverado and Santiago Formations), in the coastal region west of the Peninsular Ranges and southward into Baja California (La Jolla and Poway Groups), and in the Orocopia Mountains (Maniobra Formation).

In the San Joaquin Valley area the shelf was probably 15 to 40 miles (24-64 km) wide, based on the present distribution of shallow and deep marine strata. In the northern San Joaquin Valley, the shelf had a westward extension formed by the Stockton arch, an east-west trending structural high bounded on the north by the Stockton fault (figs. 2,7). During much of Paleocene and Eocene time, this high may have formed an emergent or shallow marine barrier which extended at least as far west as the Tesla area and divided the Great Valley into separate San Joaquin and Sacramento basins (Hackel,

1966). This arch may have resulted from buckling of the pre-Eocene continental margin due to compression associated with emplacement of the borderland by lateral movements along the proto-San Andreas fault.

North of the Stockton arch in the Sacramento Valley, the Martinez, Meganos, Capay, and Domengine Formations are largely shallow-marine deposits thought to represent shelf sedimentation. Remnants of similar deposits are also found in klippen to the west in the Clear Lake, Rice Valley, Middle Mountain and Round Valley areas. The width and geometry of the shelf in this region is not known because the boundary between shallow and deep-marine facies is not preserved in the northern Coast Ranges. However, the present distribution of shallow-marine strata from the Sierran foothills westward to the southwestern margin of the valley indicates that the shelf was at least 50 miles (80 km) wide in this region. Franciscan detritus is found in the shallow marine Eocene rocks in klippen at Rice Valley and Round Valley, indicating that the Franciscan rocks were exposed at least locally during the Paleogene in the northern Coast Ranges west of the Sacramento Valley.﻿EARLY TERTIARY PALEOGEOGRAPHY

41

In the coastal region south of Los Angeles, the Eocene continental shelf apparently extended southward for more than 100 miles (160 km) into western Baja California (fig. 7). The shelf in this area was probably 10-40 miles (16-64 km) wide, but could have been wider to the south. The shelf extended northward in middle Eocene time, including deposits of the Las Llajas Canyon, Simi Hills, Santa Susanna Mountains, and Santa Monica Mountains areas. No evidence exists from these deposits for derivation of sediments from western source areas underlain by Franciscan-type rocks.

In the Sacramento Valley area, the continental shelf was cut by the Capay and Markley gorges, which appear to have been submarine canyons through which shelf sediments were transported southward and westward into deeper environments. No such gorges or canyons have been recognized as cutting the shelves in the San Joaquin Valley area or the coastal area south of Los Angeles. However, one has been suggested to have been present in the southern area, through which sediments were transported westward to Poway fan (fig. 7; Yeats and others, 1974).

Marine transgressions across the eastern shelf are indicated in many areas by sedimentary sequences consisting of basal conglomerates overlain by fossilifer-ous sandstones, siltstones, and shales. Eastward transgressions are indicated in the San Emigdio and western Tehachapi Mountains area from early to late Eocene, in the Piru Creek area from late Paleocene to late Eocene, in the Santa Ana Mountains and SanJoaquin Hills area from middle to late Eocene and in the coastal area west of the Peninsular Ranges from early to late Eocene. Detailed studies in the subsurface of the eastern Great Valley area and in the Las Llajas Canyon, Simi Hills and Santa Monica Mountains areas may reveal that broadly transgressive conditions also existed in those areas from late Paleocene to Late Eocene time.

The erosional surface over which marine transgressions occurred was one of great relief in many places. As much as 1,000 ft (300 m) of relief is indicated at the base of the lone Formation. In the San Emigdio and Orocopia Mountains areas, the Tejon and Maniobra Formations contain very coarse, thick boulder beds which were apparently deposited along steep, irregular shorelines. In contrast, the shelf region extending from the Santa Ana Mountains and San Joaquin Hills areas south along the western edge of the Peninsular Ranges to San Diego was probably characterized by a stable shelf having relatively little relief (Yerkes and others, 1965; Peterson and Nordstrom, 1970).

A widespread late Eocene to Oligocene regression in which nonmarine deposition prograded westward across the shelf occurred in the western Tehachapi and San Emigdio Mountains and adjacent San Joaquin Valley, in the Transverse Ranges and in the Santa Ana

Mountains, and along the western edge of the Peninsular Ranges areas. Regressive conditions also characterized parts of the eastern San Joaquin and northern and eastern Sacramento basins (Hackel, 1966). Uplift of the eastern continental landmass at the close of Eocene time was evidently regional in extent, and in some areas was accompanied by extensive deformation.

Shallow marine sedimentary strata are also present along the western margin of the San Joaquin Valley, principally in the Diablo Range (Laguna Seca and Tesla Formations, and Yokut, Avenal, and Domengine Sandstones). These strata range in age from Paleocene to Eocene in the northern Diablo Range, but elsewhere they are mostly middle Eocene. These deposits were derived in part from source areas located within the Diablo Range and also from the borderland area to the west. In the northern Diablo Range, the Tesla Formation contains mineralogic evidence for derivation from both eastern and western sources; albite and glau-cophane indicate derivation from Franciscan rocks of the northern Diablo Range (Allen, 1941; Morris, 1962). Significant amounts of glaucophane, commonly accompanied by granules and pebbles of radiolarian chert, are also present in the Domengine Sandstone throughout the Diablo Range; glaucophane also is found in trace amounts in other units (White, 1940; Regan, 1943; Morris, 1962). Regan (1943) concluded on the basis of both mineralogic and lithofacies evidence that the Yokut Sandstone of the Vallecitos area had a granitic source to the west. Serpentine is locally abundant in the Avenal Sandstone of the southern Diablo Range (Acebedo Sandstone of Herrera, 1951); this mineral is abundant in nearby bedrock outcrops, and its presence in sediments thought to have been deposited in near-shore environments suggests a local derivation from within the southern Diablo Range.

The long history of brackish water and shallow marine deposition, and evidence of mixed eastern and western source areas in the northern Diablo Range, suggest that shelf sedimentation during the early Tertiary extended completely across the Great Valley in the vicinity of the Stockton arch and northern Diablo Range. Shallow-marine strata farther south in the Diablo Range were probably deposited flanking emergent areas located both within the present Diablo Range area and in the borderland area west of the proto-San Andreas fault. The sources of these deposits were probably mostly the older sedimentary rocks and granitic basement rocks of the Salinian block; however, Franciscan rocks, which underlay the ocean basin area east of the proto-San Andreas fault, were a distinctive secondary source. Tectonic instability during the Eocene is indicated locally in this region by unconformities at the base of the Avenal and Domengine Sandstones. The Stockton arch, central and western San Joaquin Valley,﻿42

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

and much of the Sacramento Valley region finally subsided in late Eocene time, as indicated by widespread deposition of shales of the Kreyenhagen Formation in a deeper marine environment.

CONTINENTAL SLOPE AND OCEAN FLOOR DEPOSITS

INTRODUCTION

A prominent west-facing submarine slope (the continental slope) formed the western edge of the shelf, and the floor of the Pacific Ocean extended westward from the base of this slope (fig. 7). In northern California, a deep-sea trench and subduction zone may have been located west of the continental shelf and slope. In central California north of the San Emigdio Mountains, a continental borderland was located west of the continental shelf and slope and a strip of ocean floor. In southern California between the San Emigdio Mountains and Los Angeles, the proto-San Andreas fault probably transected the continental margin, producing an area characterized by irregular borderland geography. Locally within this area, a west-facing continental slope and ocean floor was located west of a narrow shelf area; in other parts of this area, upland parts of the borderland were contiguous with the Mojave Desert upland area, without an intervening continental shelf and slope and ocean floor. South of Los Angeles, the continental slope and ocean floor were located west of the shelf with no evidence for the presence of a borderland. A deep-sea trench or subduction zone may have been located west of the borderland area of central and southern California, although conclusive evidence has not been produced; it may possibly have extended further south, offshore from the area in which the Poway fan was deposited (fig. 7).

The continental slope and ocean floor strata comprise (1) a widespread thin blanket of fine-grained hemi-pelagic sediments (a mixture of terrigenous detritus and pelagic plankton tests), and (2) thick, areally restricted coarse-grained deep-sea fan deposits, derived from both the borderland to the west and the continental shelf to the east. The deep-sea fan and hemipelagic deposits are commonly coeval and interfinger laterally with one another.

HEMIPELAGIC DEPOSITS

The hemipelagic deposits consist of mudstones, shales, and siltstones with some thinly interbedded turbidite sandstones, deposited at middle bathyal to abyssal depths. The deposits are widespread but generally thin because of the slow rate of sedimentation. They are commonly indistinguishable from the fine-grained interchannel and distal deposits of deep-sea fans with which they interfinger. No contourites (deposits of bot-

tom currents2) have been recognized in these rocks, but some may be present. Deposition by turbid-layer transport (slowly moving low-density turbidity currents that transport fine-grained sediments to deep water) may have been important, as this process has been observed in the modern continental borderland of southern California and is responsible for the deposition of similar deposits (Moore, 1969, p. 83). The planktonic foraminiferal faunas in these hemipelagic deposits, including those of the region of central California that was bounded on the west by the borderland, indicate free access to the open ocean.

The hemipelagic continental slope and ocean floor deposits are present in subsurface throughout much of the western Great Valley and in outcrops in the Coast Ranges, San Emigdio Mountains, western Santa Ynez Mountains, Channel Islands, San Nicolas Island, and possibly along the western flank of the Peninsular Ranges. The transitions from shelf to slope to ocean floor deposition are apparent in the Tejon Formation of the western San Emigdio Mountains (fig. 2), where shallow-marine sandstones of the late Eocene Metralla Sandstone Member grade laterally westward into bathyal and abyssal hemipelagic shales and mudstones of the Liveoak Shale Member (Nilsen, 1973c). The westernmost hemipelagic shales overlie mafic and ultramafic basement rocks which may represent Mesozoic oceanic crust. The continental slope and ocean floor facies represented by the Liveoak Shale Member in the San Emigdio Mountains can be traced northwestward as the Kreyenhagen Formation for almost 200 miles (320 km) in well sections and outcrops along the west side of the San Joaquin Valley. Toward the north the Kreyenhagen becomes siliceous, suggesting deposition in very deep silica-rich waters. Older, Ynezian to Penutian slope and ocean basin deposits may be represented in cental California by hemipelagic shales and mudstones in the Lodo Formation which crops out in the northern Temblor and eastern Diablo Ranges.

In the Sacramento Valley area, the Nortonville Shale Member of the Kreyenhagen Formation consists mostly of hemipelagic deposits, although these were deposited at neritic depths and probably represent shelf muds. Fine-grained continental slope and deep ocean basin deposits have not been recognized in the Sacramento Valley area except for probably the Sidney Shale Member of the Kreyenhagen Formation. In the northern Coast Ranges, parts of the "coastal belt” Franciscan rocks, which probably represent trench-fill deposits, may represent slope and deep ocean hemipelagic deposits. West of the Stockton arch-northern Diablo Range area, hemipelagic sediments deposited at conti-

2Bottom currents are traction currents that flow because of the potential energy in a water mass, and not because of sediment load (Piper, 1970).﻿EARLY TERTIARY PALEOGEOGRAPHY

43

nental slope depths are represented by unnamed siliceous shale of Ynezian age in the San Leandro Hills area; mudstone of Paleocene and early(?) Eocene age southwest and southeast of San Jose; the upper Ulatisian and Narizian Nortonville Shale Member of the Kreyenhagen Formation; the late Narizian Sidney Shale Member of the Kreyenhagen Formation; and mudstone of the Bolado Park Formation and siliceous shales and mudstones of the Los Muertos Creek Formation of the Bolado Park area (fig. 2). These shales are locally phosphatic (Dickert, 1966).

Lower Tertiary hemipelagic shales and mudstones are not abundant in southern California south of the Santa Ynez basin; however, our paleogeographic model suggests that they should have been deposited in the area of the present southern California borderland west of the Peninsular Ranges and west of Baja California (figs. 2, 7). Examples of such deposits may include the Pozo, Canada, and Cozy Dell Formations in the Channel Islands, and the Ardath Shale, which is evidently an offshore shale facies of the shallow marine deposits in the San Diego area.

DEEP-SEA FANS DEPOSITED EAST OF THE BORDERLAND AND DERIVED FROM EASTERN SOURCE AREAS

Deep-sea fans were deposited on the ocean floor west of the continental slope. In central California, these deposits were derived from both western sources in the borderland and Sierran sources to the east. Only those fans derived from eastern source areas and deposited east of the borderland are described in this section. Four fan deposits of this type have been identified, two to the north and two to the south of the borderland (fig. 7): (1) thick sandstones in the lower Tertiary "coastal belt” Franciscan rocks, which were probably deposited as deep-sea fans in a trench; (2) the Markley Sandstone Member and other strata of the northern Diablo Range, southwestern Sacramento Valley, and San Jose areas;

(3)	the San Francisquito, Juncal, Matilija, and Sacate Formations of the Santa Ynez Mountains and adjacent areas; and (4) the Poway fan of Yeats (1968) and Yeats, Cole, Merschat, and Parsley (1974), inferred to have been deposited west of the Peninsular Ranges and to comprise deposits now located in the Channel Islands, Santa Monica Mountains, San Nicolas Island, and adjacent areas. The "coastal belt” Franciscan rocks will be discussed in a later section under "trench(?)” deposits.

These fans were probably deposited at the base of the continental slope to form continental-rise prisms and may have been fed by large submarine canyons that funneled sediments westward and southward from the shelf areas into deeper water. Because they were deposited on the open ocean rather than in an enclosed borderland basin, these fans were probably larger and

more nearly symmetrical than those in the borderland.

Several deep-sea fans that were derived from Sierran sources may have been deposited on the ocean floor in central California in the general vicinity of the northern Diablo Range. Sediments were probably transported westward and southwestward through the Capay (Princeton) and Markley gorges, which probably represent early Tertiary submarine canyons (fig. 7). Thick sequences of sandstones that probably represent submarine canyon and fan deposition are present in the Capay gorge area, Markley gorge and adjacent Mount Diablo and southwestern Sacramento Valley areas, and in the San Jose area.

Redwine (1972; oral commun., February 1974) has shown the presence of submarine canyon-fill deposits of "Capay” age within Capay gorge and has inferred the presence of a deep-sea fan deposit at the mouth of the gorge. Sands of the Markley Sandstone Member of the Kreyenhagen Formation were probably transported westward through the Markley gorge and deposited as a deep-sea fan in the Mount Diablo and southwestern Sacramento Valley area; the Markley is present north of the Stockton arch and thickens abruptly west of the Midland fault, suggesting that fan growth was controlled by these features. The full extent of this fan to the west is not presently known, although it may possibly include parts of the thick sandstone sequences of the San Jose area described by Esser (1958), Mack (1959), Beaulieu (1970), McLaughlin (1973), and Carter (1970); however, these deposits most likely represent separate fans deposited at different times.

The paleogeography and pattern of sedimentation represented by the thick lower Tertiary sections in the San Jose area cannot be easily reconstructed on the basis of available mineralogic, sedimentologic, and paleontologic data. These sequences may have been deposited as small, separate fans derived from either the Salinian block to the west or from the northern Diablo Range-Stockton arch area to the east. On the other hand, they may have been deposited as a single elongate fan in a relatively narrow northwest-trending basin with a northwestward axial slope located between the borderland area to the southwest and a possible emergent area to the northeast in the northern Diablo Range. This type of reconstruction would be reasonably consistent with the paleogeographic framework proposed by Wentworth (1966, 1968) for deposition of the German Rancho Formation of the Gualala area to the northwest across the San Andreas fault. However, the deposits of the San Jose area have variable ages, mineralogies, and paleocurrent directions, including some oriented toward the south; simple correlations of this sequence with those of the Gualala area are not convincing, and require a great deal of additional study﻿44

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

of the lower Tertiary sequences in the San Jose area. At least some of these deposits, particularly those described by Beaulieu (1970) and Tieh (1973), suggest deep-sea fan deposition derived from eastern source areas.

The Santa Ynez basin and adjacent areas could reasonably be part of the western borderland area, inasmuch as tectonic movements in the southern part of the borderland influenced deposition in the basin (fig. 7). However, because the sediments were derived primarily from eastern source areas, were deposited as fans that extended westward and southwestward onto the open ocean floor, and were effectively deposited south of the true borderland area, we shall discuss the paleogeography of the deep-sea fans deposited in the Santa Ynez basin and adjacent areas in this section.

Reconstruction of the early Tertiary paleogeography of the Santa Ynez basin and adjacent areas to the east and southeast is complicated by abundant post-Eocene lateral faulting and compressive folding that must be palinspastically restored to determine the original paleogeography. In order to delineate the middle Eocene paleogeography of southern California, Howell (1974) restored about 30 miles (48 km) of right-lateral displacement along the San Gabriel fault, 50 miles (80 km) of left-lateral displacement along the Garlock fault, 9 miles (14.5 km) of left-lateral displacement along the Big Pine and Santa Ynez faults, 56 miles (90 km) of left-lateral displacement along the Malibu Coast fault (an east-west-trending fault located along the southern edge of the Santa Monica Mountains and extending westward toward the Channel Islands), 88 miles (140 km) of right-lateral displacement along the east Santa Cruz Basin fault of Howell, Stuart, Platt, and Hill (1974) (a northwest-trending fault located in the central part of the southern California borderland), and 10 miles (16 km) of north-south crustal extension to unfold the Transverse Range.

Restorations along these and other faults yield a late Paleocene paleogeography consisting of a relatively straight northwest-trending shoreline and narrow shelf, southwest of which submarine fans represented by thick Paleocene strata in the Piru Creek area and the San Francisquito Formation of the Elizabeth Lake Canyon, Valyermo, and Cajon Pass areas were deposited (Sage, 1973). Because these fan deposits rest mostly on granitic crust, they may have been deposited on the outer part of the continental shelf and continental slope, or on strongly downwarped parts of the outer shelf. Sage (1973, fig. 100) indicates that the late Paleocene shoreline extended northwestward into the La Panza Range area, and that the deep marine hemipelagic deposits of the Anita Shale of the Santa Ynez basin were deposited far offshore and southwest of the limits of the deep-sea fan deposits.

The restorations along the faults indicate that the Eocene Santa Ynez basin was irregularly shaped, extending northward into the Sierra Madre basin and eastward into the Piru Creek area. Within the basin, the Juncal, Matilija, and Sacate Formations have been interpreted as submarine fan deposits derived from source areas located primarily to the north and east (Stauffer, 1965; Weaver, 1969; Link, 1971, 1972; O’Brien, 1972; Van De Camp and others, 1974; Howell, 1974). The Eocene basin was bounded on the southeast, east, northeast, and northwest by upland areas; the deep-sea fans were derived from these upland areas and coalesced within the basin to form thick, irregularly-shaped fan deposits that extended far out onto the ocean floor to the southwest. During the middle Eocene, the Santa Ynez basin was bounded on the southeast by the northward extension of the continental shelf and slope that was present in the coastal area west of the Peninsular Ranges, Santa Ana Mountains, and San Joaquin Hills areas; the middle Eocene sequences of the Las Llajas Canyon, Simi Hills, Santa Susanna Mountains, and Santa Monica Mountains areas were deposited on this part of the continental shelf (D. G. Howell, written commun., May 1974).

Thus, the paleogeography of the Santa Ynez basin area changed considerably during the early Tertiary. Tectonic activity in the borderland area northwest of the basin was probably the chief cause of these paleogeographic changes. The history of these paleogeographic changes in this complex area is not completely understood yet, particularly for the early Paleocene and early Eocene intervals.

The Poway deep-sea fan and submarine cone of the southern California borderland is the fourth deposit to be considered in the category of deep-sea fans derived from eastern source areas and deposited east of or beyond the limits of the borderland. The Poway fan was reconstructed by Yeats, Cole, Merschat, and Parsley (1974) from scattered Eocene deposits that contain the distinctive Poway-type clast assemblage; the fan is thought to have radiated westward from a point source located near Lake Elsinore and to have been derived in part from an eastern source area underlain by Poway-type rocks and probably located in northern Sonora, Mexico (Minch, 1971; Merriam, 1972). However, Howell, Stuart, Platt and Hill (1974) consider the point source to be located further south in the San Diego area. Conglomerate and sandstone in the Santa Monica and Santa Ana Mountains areas are thought to represent the upper part of the Poway fan, whereas grain-flow and turbidite deposits of San Nicolas, Santa Rosa, Santa Cruz, and San Miguel Islands are thought to represent the middle and lower parts of the fan (Yeats, 1968,1973; Yeats and others, 1970; Yeats and others, 1974; Merschat, 1968, 1971; Parsley, 1972; Cole, 1973). The﻿EARLY TERTIARY PALEOGEOGRAPHY

45

Poway fan was probably deposited on the ocean floor as a large, unrestricted open-ocean fan, and it was probably completely separated from the fans deposited in the Santa Ynez basin to the north.

Yeats, Cole, Merschat, and Parsley (1974) concluded that the Eocene Poway fan had been fragmented and distributed by later Miocene rifting within the modern southern California borderland area. Howell, Stuart, Platt, and Hill (1974), on the other hand, concluded that the Poway fan had been fragmented and distributed by right-lateral strike-slip faulting along the East Santa Cruz Basin fault system within the modern southern California borderland area. Both, however, accept the presence of the Poway fan in the area during middle and late Eocene time.

CONTINENTAL BORDERLAND DEPOSITS

We infer that the thick, coarse-grained, and areally restricted sequences of sandstone and conglomerate in the borderland represent deep-sea fan deposits. Thinner sequences of shale and mudstone associated with these deposits are inferred to represent deep-sea hemipelagic sediments laid down when and where fan growth was not active. Shallow marine and nonmarine deposits of lower Tertiary age are rare in the borderland. Paleocur-rent analyses, stratigraphic studies, and mineralogic data indicate that the deep-sea fans were derived from sources within the borderland rather than from eastern sources in the Sierra or Mojave areas.

Large deep-marine borderland basins are suggested by extensive fan deposits in the Gualala area (Gualala basin of Wentworth, 1968), the Santa Cruz Mountains (La Honda basin of Cummings and others, 1962), the southern Santa Lucia, La Panza and Sierra Madre Ranges (Sierra Madre basin of Chipping, 1970a, 1972a), and the western Transverse Ranges (Santa Ynez basin of Stauffer, 1965, 1967). Because the Santa Ynez basin may have been located at the south end of the early Tertiary borderland area and the sediments deposited within it derived primarily from source areas located east of the borderland area, we have discussed it in an earlier section.

Smaller borderland basins are suggested by localized outcrops of sandstone and conglomerate that resemble deep-sea fan deposits in the Point Reyes area, Point San Pedro area, Point Lobos area, and in the northern Santa Lucia Range. Some of these may not have been separate, individual basins but connected to or at the fringe of the larger basins. Thus, the Point Reyes deposits may possibly have been laid down along the southern edge of the Gualala basin, although relations between these sequences would be very difficult to prove; the Point San Pedro deposits may be related to those of the larger La Honda basin (as suggested by Chipping, 1972b) and the lower Tertiary sequences in the Pattiway Ridge, Mount

Pinos, and Pine Mountain areas were probably deposited in the eastern Sierra Madre and Santa Ynez basins, where they merge eastward and their sediments grade laterally into shallow-marine deposits. The relation of the Carmelo Formation at Point Lobos to the La Honda or northern Santa Lucia Range basins is uncertain. The lower Tertiary deposits of the Adelaida area, probably of shallow marine origin, may have been deposited in the Sierra Madre basin and subsequently offset right-laterally from it along the Rinconada fault, as suggested by Schwade, Carlson, and O’Flynn (1958) and Dibblee (1972a).

The borderland paleogeography was characterized primarily by deep restricted basins separated by upland source areas. Outcrops are not sufficient, particularly in the northern end of the borderland area which is now largely under the sea, to establish conclusively whether the upland areas were separate, detached islands or partly or wholly interconnected to form a long, irregularly shaped peninsula. It is doubtful that upland areas underlain by granitic rock existed north of the Gualala basin, inasmuch as seismic data reveal the absence of granitic crust north of Point Arena (Silver and others,

1971). Planktonic foraminiferal faunas from the borderland deposits indicate access to the open ocean, suggesting that the basins were not enclosed by land areas. Paleocurrent and lithofacies data indicate that source areas were located southwest of the Gualala basin (Wentworth, 1966); southeast of the Point San Pedro deposits (Chipping, 1972b); south and possibly northwest of the La Honda basin (Nilsen and Simoni, 1973); east of the Point Lobos deposits (Nili-Esfahani, 1965); possibly southeast of the northern Santa Lucia Mountains deposits (Link, 1975); north, east, and south of the Sierra Madre basin sequence (Chipping, 1972a); north and northeast of the Pattiway Ridge deposits (Sage, 1973); and north and east of the Santa Ynez basin sequence (Stauffer, 1967).

A palinspastic reconstruction of central California made by unslipping the San Andreas fault 190 miles (305 km) to allow for post-early Miocene right-lateral displacement juxtaposes the following lower Tertiary sequences; (1) the German Rancho Formation of the Gualala area with the Cantua Sandstone Member of the Lodo Formation of the Vallecitos area and possibly the Tres Pinos Sandstone of the Bolado Park area; (2) the Locatelli Formation, Butano Sandstone, and Twobar Shale Member of the San Lorenzo Formation of the Santa Cruz Mountains area with the Lodo Formation, Point of Rocks Sandstone, and Wagonwheel Shale Member of the Kreyenhagen Formation of the northern Temblor Range; and (3) shales and siltstones of the San Juan Bautista area with the Liveoak Shale Member of the Tejon Formation and the San Emigdio Formation of the western San Emigdio Mountains. In addition, it is﻿46

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

probable that the shoreline represented by the eastward interfingering of the marine Tejon and San Emigdio Formations with the nonmarine Tecuya Formation in the western Tehachapi and San Emigdio Mountains extended southwestward across the San Andreas fault and is represented in the northern Santa Lucia Range by eastward interfingering of the Reliz Canyon and Church Creek Formations with the partly nonmarine Berry Formation. We believe that these sequences were contiguous at the time of deposition and were subsequently offset about 190 miles (305 km) by right-lateral slip along the San Andreas fault.

Kirkpatrick (1958), Crowell (1962), and Dickinson, Cowan, and Schweickert (1972) have concluded that in southern California the Maniobra Formation of the Orocopia Mountains has been offset along the San Andreas and San Gabriel fault as much as 190 miles (310 km) from lower and middle Eocene sandstones in the Mount Pinos-Pine Mountain areas. Paleocene strata in the Pattiway Ridge area also appear to have been offset from similar strata in the Cajon Pass area; however, the amount of displacement is less (about 140 miles, 225 km), suggesting that either the fault had another active strand in this region during its history or that the Cajon Pass sequence may itself lie within a sliver of the San Andreas fault.

In the Gualala basin, the deep-sea fan of the German Rancho Formation apparently extended beyond the borderland onto the ocean floor to the east across the present trace of the San Andreas fault. Similarly, the fan of the Butano Sandstone in the La Honda basin extended eastward across the fault as the Point of Rocks Sandstone. The ocean floor east of the borderland thus received deep-sea fan sediments from both the borderland to the west and the continental landmass to the east. Submarine fan deposits may have also spilled out of the borderland onto the ocean floor to the west and, if present, into an offshore trench.

Deep marine hemipelagic shales accumulated in areas that did not receive deep-sea fan sediments and on the fans when coarse-grained clastic sediments were not being deposited. These sediments make up the Locatelli and San Lorenzo Formations in the La Honda basin, Eocene shale in the San Juan Bautista area, Eocene shale in subsurface southeast of Point Reyes, some of the thick shale sequences in the Sierra Madre basin, and shales of the Juncal, Anita, Cozy Dell, and Gaviota Formations in the Santa Ynez basin. These shale units are locally siliceous and phosphatic (Dick-ert, 1966).

The basins in the central part of the borderland area are unusual in that both submarine fan deposits, shallow marine, and nonmarine strata of approximately the same age are preserved. In the northern Santa Lucia Range basin, the lower part of the Eocene and Oligocene

sequence consists of a shallow marine, transgressive basal sandstone (Junipero Sandstone) overlain by a shale (Lucia Shale) deposited in quiet, offshore waters (Dickinson, 1965). The upper part of the sequence (The Rocks Sandstone and Church Creek Formation) contains sandstones indicative of offshore deposition. The Rocks Sandstone appears to represent submarine fan deposition (Link, 1975), and the Church Creek Formation was deposited at outer shelf or slope depths (Brabb and others, 1971). The upper part of the sequence, which is probably regressive, may grade laterally eastward into the nonmarine Berry Formation, considered of 01igocene(?) age (Durham, 1974), but the lower part may possibly be late Eocene.

Paleocene strata near the northern edge of the Sierra Madre basin have been interpreted by Chipping (1972a) and Sage (1973) as shallow marine and nonmarine deposits. The strata near Adelaida may represent similar facies, although nonmarine deposits have not been described.

Thus, the central part of the borderland area, which adjoined the upland continental landmass area to the east, apparently did not subside to form very deep basins in which thick deep-sea fan sequences were deposited. To the north, in the La Honda basin, and to the south, in the main part of the Sierra Madre and in the Santa Ynez basins, thick deep-sea fan deposits accumulated.

DEEP-SEA TRENCH DEPOSITS

A number of writers have recently inferred the presence of a deep-sea trench west of California in the early Tertiary, and several have identified the trench deposits. Atwater’s (1970) model for late Mesozoic and Cenozoic plate interactions along the west coast of North America suggests the presence along the boundary between the North American and Farallon plates of a deep-sea trench and subduction zone during the early Tertiary (fig. 5). On the basis of lower Tertiary strata found in what was interpreted as the upper plate of a "fossil” underthrust or subduction zone, Berkland

(1972)	suggested that an early Tertiary deep-sea trench and subduction zone was present in northern California. On the basis of chaotically structured beds in lower Tertiary strata northwest of San Jose, and other data, Travers (1972) inferred the presence of an early Tertiary deep-sea trench west of central California. Raymond and Christensen (1971), Chipping (1971), O’Day and Kramer (1972), Berkland (1972), O’Day (1974), and Kleist (1974) have suggested or inferred that the "coastal belt” Franciscan rocks were deposited largely as fill in a deep-sea trench in which active subduction was no longer occurring.

Unfortunately, with the single exception of the "coastal belt” Franciscan rocks, little concrete evidence exists for the presence of the early Tertiary trench and﻿SEDIMENTOLOGY OF THE BORDERLAND DEEP-SEA FANS

47

subduction zone. If deposited, trench fill would have accumulated west of the early Tertiary borderland area of central California and west of the continental shelf, slope and ocean floor of the Poway fan area of southern California (fig. 7). Because these areas presently lie offshore and relatively little information is available about possible lower Tertiary deposits in these areas, we can only speculate that possibly a trench and subduction zone existed west of central and southern California to fit the constraints of Atwater’s (1970) model; however, its existence remains unproven. The slump features and chaotic bedding in lower Tertiary strata of the San Jose area may represent slumping within one of the basins formed adjacent to the proto-San Andreas fault rather than penecontemporaneous deformation within a trench, as suggested by Travers (1972).

The "coastal belt” Franciscan rocks and "fossil” subduction zone of Berkland (1972) provide good evidence for the existence of a trench in northern California. Berkland (1972) suggests that active subduction in the trench continued until at least the middle Paleocene; after subduction had ceased, the trench was filled with sediments. "Coastal belt” sandstones and conglomerates are relatively unmetamorphosed and generally lack the presence of volcanic rocks, serpentine, chert, melange structure, and exotic blocks of high pressure-low temperature metamorphic rocks. The thick sandstone, shale, and conglomerate sequences were deposited by turbidity currents, grain flows, debris flows, slumping, and sliding; deep-sea fans may have grown outward down the axis of the trench. The source areas for these sediments are not known, but presumably they lay to the east or north.

SEDIMENTOLOGY OF THE BORDERLAND DEEP-SEA FANS

The borderland deep-sea fan deposits consist mostly of thick irregularly bedded conglomerate, thickly bedded ungraded or poorly graded sandstone, more thinly bedded graded sandstone, and thin-bedded to massive hemipelagic mudstone, shale, and siltstone. These different strata grade laterally and vertically into one another and form the various facies of deep-sea fan deposits. The most common facies is the thickly bedded, ungraded to poorly graded sandstone, identified by various workers as proximal turbidites, fluxoturbi-dites, grain flow deposits, and submarine slide or slump deposits.

Recent studies of the physiography, morphology, growth patterns, and sedimentology of modern deep-sea fans along the continental margin of western North America and particularly in the modern southern California borderland area have provided useful models for comparison with the early Tertiary borderland fans.

The modern fans and their surrounding areas generally comprise: (1) a submarine canyon which acts as a conduit for the transport of sediment from shallow to deep marine areas; (2) an upper fan area cut by a large incised valley that extends from the submarine canyon out onto the fan surface, where it is flanked by levees; (3) a middle fan area characterized by a depositional bulge or suprafan that results from major sedimentation where the leveed upper fan valley divides downfan into meandering major channels; (4) a lower fan area where the middle fan channels divide further into many smaller, shallower braided distributary channels; and

(5)	a fan fringe area, where fine-grained sands and silts grade laterally outward into hemipelagic sediments of the ocean floor (Normark and Piper, 1969, 1972; Nor-mark, 1970; Nelson and others, 1970; Haner, 1971; Nelson and Kulm, 1973; Nelson and Nilsen, 1974).

The resulting modern fan deposits comprise two distinct facies, coarser grained and more thickly bedded channel deposits and finer grained and more thinly bedded interchannel deposits. Because the major sedimentation in the middle fan area is accompanied by the lateral migration of channels, the two facies overlap one another and the resulting deposits are laterally discontinuous. Furthermore, because turbidity currents, grain flows, and other transporting mechanisms rapidly lose velocity in the lower submarine canyon and upper fan area, the coarsest detritus is deposited in the submarine canyon and upper fan channel. Progressively finer grained sediments are transported to more distal parts of the fan, where fine sand and silt is deposited as laterally continuous thin turbidite beds. Thus, the proximal (upper and middle fan) deposits are generally coarser grained that the distal (lower fan) and fan fringe deposits.

These studies of modern submarine fans also show that, in general, irregularly bedded conglomerates form in submarine canyons and upper fan channels; thickly bedded, poorly graded sandstones form in submarine canyons, upper fan, and upper suprafan channels; thinly bedded graded sandstones form in interchannel areas, the lower suprafan, lower fan channels, and fan fringe areas; and hemipelagic shales form on and beyond the fan fringe and on any part of the fan or canyon where coarse-grained terrigenous detritus is not being deposited. We believe that these general relationships also apply to the lower Tertiary deposits of this study.

Of the coarse-grained sediments, the upper fan and middle fan channel deposits are most commonly preserved in the rock record, largely because more proximal submarine canyon deposits were of limited extent and are commonly removed by subsequent uplift and erosion of the basin margin. The early Tertiary borderland fans apparently had large, thick suprafans, where﻿48

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

subaqueous sediment gravity flows, including grain flows, fluidized sediment flows, and turbidity currents deposited proximal turbidites in numerous large channels (Middleton and Hampton, 1973; Nelson and Kulm, 1973; Nelson and Nilsen, 1974). Thinly bedded, finer grained interchannel and levee deposits resulted from overbank spilling of large sediment gravity flows. The basin slopes were probably relatively steep and submarine canyons poorly developed. The fans are small in size compared to many modern fans, and source areas in some cases were located on more than one side of the basin; as a result, the more distal, thin-bedded flysch-like deposits are generally poorly developed. As reconstructed, the Butano-Point of Rocks and German Rancho-Cantua fans overflowed the borderland basins onto the ocean floor to the east, where both the Point of Rocks and Cantua interfingered eastward with fine-grained hemipelagic sediments of the San Joaquin basin area.

Many characteristic features of modern deep-sea fan deposits are present in the reconstructed early Tertiary Butano-Point of Rocks fan, including (1) a fan-shaped wedge of sediment that thins distally; (2) a radiating system of fan channels, indicated by the distribution of coarse-grained conglomerate and by paleoccurent patterns; (3) coarse-grained conglomerates in proximal depositional sites, thought to be upper fan channels; (4) common channeling of sandstones in the upper and middle fan areas; (5) abrupt vertical and lateral facies changes representing the shifting of channel, levee and interchannel deposits; (6) downfan fining and thinning of channel deposits; (7) Bouma ae sequences in strata thought to be proximal channel deposits, Bouma ae to abode sequences in strata thought to be suprafan channel deposits, and Bouma abode to ode sequences in strata thought to be distal channel deposits; (8) Bouma ode and de sequences in strata thought to be levee and interchannel deposits; and (9) bioturbation of finegrained sediments (Nilsen, 1970, 1971; Nilsen and Simoni, 1973; Clarke, 1973; Nelson and Nilsen, 1974).

The sedimentary structures and other features which characterize the lower Tertiary deep-sea fan deposits of the California continental margin are summarized in table 2. Similar deposits from other regions have been described by Walker (1970), Mutti and Ricci-Lucci (1972), Stanley and Unrug (1972), and Walker and Mutti (1973).

The sandstones of the early Tertiary fan deposits are typically ungraded or have very poorly defined grading, delayed grading, or "coarse-tail” grading; some beds show a reverse grading at the base. The coarse-grained sandstones and conglomerates have beds as much as 75 ft (23 ill) or more in thickness. The soles of many beds have load casts and large flute and groove casts; however, smooth, flat soles may be even more common.

Diffuse parallel lamination, dish structures, swirled lamination, and elutriation columns indicative of the upward escape of fluid are common. Large mudstone and siltstone rip-up clasts that may be deformed are found evenly distributed through beds or concentrated along particular horizons, as are calcareous concretions. The uppermost parts of the beds, if graded, characteristically contain convolute laminae and contorted stratification. Thin mudstone and shale interbeds commonly separate the thick sandstones; however, these interbeds or partings are commonly laterally discontinuous. Amalgamation of sandstones due to the nondeposition of or removal of fine-grained interbeds is common and results in composite sequences of sandstone beds as much as 150 ft (45 m) thick.

Conglomerate clasts may be oriented or irregularly dispersed in a sandstone matrix. Pebbly mudstone is very rare. Channeling and downcutting into underlying strata is common, both at the base of sandstone beds and within beds. Sequences of thick sandstones grade laterally into more thinly bedded sandstones and downcur-rent into more thinly bedded turbidite sandstones with more completely developed Bouma sequences. Rotational slumps and contorted strata are present in both thickly bedded and thinly bedded sandstones inferred to be channel and interchannel deposits. Sand injection structures, such as dikes, sills, and diapirs are locally abundant. Invertebrate megafossils are rare, but Foraminifera are common in interbedded shales.

These deposits are mostly very proximal turbidites as defined by Walker (1967, 1970); however, they are interbedded seemingly at random with more thinly bedded, finer grained flyschlike sandstones which are very distal turbidites by the same definition. The thinly bedded sandstones apparently represent interchannel deposits, and are characterized by graded bedding, flute, groove and load casts, primary current lineation, convolute lamination, flame structures, current ripple markings, small-scale cross-strata, and generally incomplete Bouma sequences.

TECTONIC FRAMEWORK OF BORDERLAND SEDIMENTATION

We believe that the deep, restricted early Tertiary basins of central California probably resulted from right-lateral slip along a proto-San Andreas fault. The formation of these basins is closely linked spatially and temporally to the postulated emplacement of the continental borderland by right-slip transform faulting along the proto-San Andreas fault. The basins appear to be similar to those suggested by Crowell (1972, 1973b, 1974) to result from slicing and fragmentation of continental crust along transform boundaries between major crustal plates. Such tectonism results in local crustal extension, the pulling apart or rifting of the continental﻿TECTONIC FRAMEWORK OF BORDERLAND SEDIMENTATION

49

crust to form basins at the same time that compression, folding, and uplift forms adjacent highland source areas.

The basins formed by crustal stretching or extension are small rhombochasms or pull-apart basins; they may be grabens or half-grabens bounded by normal faults which trend at high angles to the major transform fault zone, or may be elongate depressed blocks within the complex, bifurcating transform zone (fig. 8). The basins are typically bounded by upland areas on two sides, often three or four sides. Sediments may be transported into the basins from adjacent uplifted blocks or longitudinally from source areas farther away, on either side of the major transform fault. The Ridge basin, parts of the Ventura basin and the Santa Barbara Channel have been suggested as possible examples of late Cenozoic basins formed as rhombochasms or pull-aparts related to movement on the present San Andreas fault. Other modern features such as San Francisco Bay, Monterey Bay, and at least some of the borderland basins of southern California have probably also been formed as a result of right-lateral slip.

We conclude that similar processes disrupted the early Tertiary continental borderland formed by the Salinian block, and that thick, areally restricted borderland deep-sea fan deposits filled deep rhombic holes or pull-apart basins formed by right-lateral slip along the proto-San Andreas fault. As the Salinian block was transported northwestward during Late Cretaceous and early Tertiary time, it broke into separate fragments that formed island sources areas separated by deep marine basins. Most of the basins were probably fault-bounded, although some may have originated partly as simple downwarps of the crust due to extension. Because the island source areas were rapidly uplifted, the detritus supplied to the depositional basins was coarse-grained, fresh, and unweathered. In many areas, gravels and coarse-grained sands were apparently transported directly from source areas to deep marine depositional sites. Most of the pull-apart basins of the borderland were probably deep and bounded by relatively steep slopes. As a result of the volume, coarseness, and high rate of sediment supply, thick, coarse-grained upper and middle fan facies dominated the submarine fans deposited in these basins.

The major basins in the early Tertiary continental borderland area, the Gualala, La Honda, Sierra Madre, and Santa Ynez basins, contain thick, deep marine sedimentary sections. In contrast, many of the late Tertiary rhombochasmic basins along the present San Andreas fault system are largely filled with shallow marine and nonmarine sediments. An exception to this general pattern in the early Tertiary continental borderland may have been the northern Santa Lucia Range basin, which appears to have been filled substantially

by shallow marine and even nonmarine deposits; however, the original extent of this basin and its deposits cannot be ascertained from the existing outcrops. Two of the deepest basins with very thick sediment fills were the Gualala and La Honda basins, located in the part of the borderland that jutted out more than 150 miles (240 km) northwestward from the continental margin (figs. 7, 8).

The geometry and boundaries of the Gualala basin cannot be fully determined because it is truncated on the east by the San Andreas fault, covered on the west by the Pacific Ocean, and its strata are beveled by a post-middle Eocene unconformity. The oldest strata in the basin, which are Late Cretaceous in age, rest on a pillowed spilite that resembles volcanic rocks in the Franciscan Formation and has oceanic affinities (Wentworth, 1966). It is possible that rifting and extension of the continental crust near the margin of the continent during the Late Cretaceous may have resulted in oceanic crust being exposed in the central part of the basin; by this process, the Gualala basin or possibly some of the other borderland basins may be floored by oceanic crust, even though it is part of the Salinian block. Alternatively, the presumably Franciscan spilite may have been offset right-laterally from Franciscan basement rocks near the inferred Sierran-Franciscan contact located northwest of the western San Andreas fault, as suggested by Wentworth (1968).

The original boundaries of the La flonda basin are also poorly known. The southern margin may have been formed by the Monterey fault, an old fault that trends approximately east-west within Monterey Canyon, is probably upthrown on the south side, and may have been active in the early Tertiary (Martin and Emery, 1967; Greene, 1970). A second potential boundary is the Santa Cruz fault of Ross and Brabb (1973), which trends northeast-southwest near the south end of the Santa Cruz Mountains; it is a dip-slip fault of moderate displacement along which granitic basement rocks are upthrown on the south. A bounding landmass northwest of the reconstructed La Honda basin is suggested by the presence of some southeastward-directed pale-ocurrents and fine conglomerates in the northwest-ernmost outcrops of the Butano Sandstone, and by northeastward-directed paleocurrents and thick, coarse-grained upper and middle fan facies in the northwesternmost outcrops of the Point of Rocks Sandstone. The relation between the La Honda basin and the Paleocene basin represented by deposits in the Point San Pedro area is not known. The La Honda basin was probably bounded by uplands on the northwest and south, and possibly on the southwest. The lower Tertiary sedimentary strata within it indicate that initial shallow marine deposition was followed by rapid deepening of the basin and deposition of deeper marine﻿50

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

CS

GR

PR

PSP

POR

BU

C

TR

SM

SRH

SIERRA

NEVADA

EXPLANATION

Cantua Sandstone Member of Lodo Formation,

Vallecitos area

German Rancho Formation of Wentworth, 1968,

Gualala area

Conglomerate, sandstone and shale of Point Reyes area

Conglomerate, sandstone and shale of Point San Pedro area

Point of Rocks Sandstone of the northern Temblor Range and southwestern San Joaquin Valley area Butano Sandstone of the Santa Cruz Mountains area

Carmelo Formation of Bowen, 1965a, of the Point Lobos area

The Rocks Sandstone of Thorup, 1941, of the northern Santa Lucia Range area Sierra Madre basin San Rafael high

APPROXIMATE SCALE

100 KILOMETRES﻿TECTONIC FRAMEWORK OF BORDERLAND SEDIMENTATION

51

shale; this was followed in turn by deposition of a large volume of coarse-grained sediment derived principally from a felsic plutonic area to the south. In latest Eocene time, only deep marine shale was deposited in the basin, indicating that uplift of the source area had ceased or that coarse-grained sediments were prevented from reaching the basin.

The Sierra Madre and Santa Ynez basins may have been partly bounded by east-west-trending normal faults. A variety of paleocurrent and lithofacies data indicates that these basins were separated in the west by a wedge-shaped emergent area known as the San Rafael high, which had an east-west-trending southern edge and a northwest-trending northern edge (fig. 7). This high may have been fault-bounded, as the two basins appear to have deepened abruptly to the north and south. Recurrent uplift of the high is indicated in part by the abundant coarse-grained sediments derived from it. Eastward, the Sierra Madre and Santa Ynez basins appear to merge into a common basin.

In summary, we suggest that (1) the early Tertiary sedimentary basins located west of the San Andreas fault were formed tectonically by crustal stretching associated with emplacement of the early Tertiary continental borderland along a proto-San Andreas fault during the Late Cretaceous and early Tertiary; (2) the basin margins were tectonically active and formed by normal faulting and downwarping; (3) the basin floors were also tectonically active, undergoing uplift and subsidence; (4) the larger basins were very deep and were filled primarily by deep-sea fan deposits and hemipelagic shale; (5) some basins received deep-sea fan deposits continuously from Late Cretaceous to late Eocene time, whereas others received fan deposits for much shorter periods; and (6) the basins were limited in extent and most were bounded by upland areas on at least two sides. South of the Santa Ynez basin, the continental margin was characterized by a continental shelf, slope, and possible deep-sea fans to the west deposited on the open, unrestricted continental rise area.

Although the major conclusions of this paper substantiate the major conclusions about the plate tectonic

Figure 8.—Generalized map showing tectonic activity within the early Tertiary continental borderland of western California, based on restoration of 190 miles (305 km) of post-Eocene right-lateral offset along the present San Andreas fault. Upland areas are indicated by +, continental shelf by closely spaced horizontal lines, continental slope by hachure lines, and low-lying basins and ocean floor by widely spaced horizontal lines. Deep-sea fans are shown by dotted pattern, edges of deep-sea fans by short dashed lines, and paleocurrent directions by single-headed arrows. Directions of rifting apart of borderland blocks indicated by solid, double-headed arrows.

history of the western North American continental margin developed by Atwater (1970) and Atwater and Molnar (1973), some of the early Tertiary paleogeo-graphic data do not completely fit into her model. As a result, we can only speculate about the overall tectonic history and development of the California continental margin during the early Tertiary. Atwater indicates that a triple junction developed in the Late Cretaceous and early Tertiary where the spreading ridge that separated the Kula and Farallon plates interacted with the North American plate (fig. 5). According to her model, this triple junction migrated northwestward during the Late Cretaceous and early Tertiary along the transform fault that separated the Kula and North American plates, in response to the relative motion between these two plates and to the spreading systems to the west and south. North of the triple junction, the transform boundary (proto-San Andreas fault) was progressively shortened, while south of the triple junction the subduc-tion zone that formed the boundary between the North American and Farallon plates was progressively lengthened. As a consequence of this geometric relationship of plates, the emplacement of the continental borderland by right-slip movements along the proto-San Andreas fault was succeeded by subduction along the continental margin.

We suggest that in central California subduction probably took place in the early Tertiary west of the continental borderland at the boundary between oceanic and continental crust, rather than at the site of the transform boundary as shown by Atwater (1970) (figs. 5, 7). Only after the triple junction migrated to a position north of the northwestern end of the continental borderland making up the Salinian block, perhaps about 60 million years ago, did subduction begin to occur along the site of the transform boundary. However, the data to support this inference are not presently available, because the evidence presumably lies buried in offshore areas, west of the Salinian block and possibly in the western part of the modern southern California borderland. The "coastal belt” Franciscan rocks of early Tertiary age provide evidence for the existence of a trench in northern California. However, preliminary work suggests that this trench was not actively undergoing subduction during most of the early Tertiary; the "coastal belt” strata have been interpreted as trench-fill deposits in an inactive trench. Possibly the active trench postulated herein for the early Tertiary lay west of the inactive trench represented by the "coastal belt” Franciscan strata.

The data needed to support Atwater’s model of a northward-lengthening subduction zone in the early﻿52

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

Tertiary along the contact between the Farallon and North American plates are not available from the onshore record of the lower Tertiary strata. The only concrete evidence for a trench exists in the record of the "coastal belt” Franciscan rocks, where preliminary data indicate evidence for subduction continuing only up to the middle Paleocene (Berkland, 1972). If Atwater’s model is correct, the subduction zone should have been initiated at successively later times toward the north.

It may be possible that the subduction of the Farallon plate in the early Tertiary was very slow or that it proceeded in such a manner that evidence for active subduction in the "coastal belt” Franciscan strata of northern California is not clearly recognizable. The extensive volcanic activity throughout California that began in Oligocene time is probably related to subduction of the Farallon plate; the rate of subduction may have increased along the postulated offshore trench and subduction zone to the west during the Oligocene. Much additional study of early Tertiary sedimentary rocks in the "coastal belt” Franciscan, San Francisco Bay region, and offshore areas will be required to satisfactorily resolve some of the large-scale problems of the early Tertiary tectonic history of California.

SUMMARY AND CONCLUSIONS

Recent geologic studies suggest that 135-260 miles (220-420 km) of right-lateral offset occurred along a proto-San Andreas fault in central and northern California during Late Cretaceous and early Paleocene time (fig. 4). Mid-Mesozoic granitic basement rocks in the Salinian block have been offset northwestward between 325 and 450 miles (520-720 km) from the southern end of the Sierra Nevada (Hill and Dibblee, 1953; Curtis and others, 1958). Displacements along the present San Andreas fault appear to be limited to about 190 miles (305 km), an offset which has been demonstrated for rocks of late Paleocene, Eocene, Oligocene, and Miocene (about 22 and 23.5 m.y. old) age. These displacements indicate that right-lateral slip did not occur between early Paleocene and early Miocene time and that the offset observed on the present San Andreas fault results entirely from post-early Miocene movements (Turner, 1968, 1969; Turner and others, 1970; Huffman, 1972a, b; Huffman and others, 1973; Clarke and Nilsen, 1972, 1973; Nilsen and Clarke, 1972; Clarke, 1973; Dickinson and others, 1972; Matthews, 1973a, b; Nilsen, Dibblee, and Simoni, 1974). The remaining offset of 135-260 miles (220-420 km) was taken up by the proto-San Andreas fault (Suppe, 1970). This conclusion is supported by a tentative reconstruction of plate motions in the eastern Pacific which suggest that interaction of the North American and Kula plates resulted in right-lateral transform faulting of the California continental margin from about 80 to 60 m.y. ago (Atwater, 1970).

The trace of this old fault in central and northern California is probably almost parallel to but west of the present San Andreas fault; it probably bypassed the present onshore southern California area and is located in the present continental borderland west of southern California and northern Baja California. Part of it may be preserved onshore in southern Baja California (Minch and James, 1974).

Displacement of the Salinian block from the southern Sierra Nevada along the proto-San Andreas fault formed an elongate continental borderland which extended perhaps 200 miles (320 km) northwestward from the Mesozoic continental margin (fig. 7). This borderland probably consisted of granitic island uplands separated by deep marine basins, although the uplands may have been interconnected to form a long irregular peninsula. Preservation of the early Tertiary basins in the borderland areas, determination of fault offsets, and recognition that the Salinian block formed a borderland in the early Tertiary argue against emplacement of the Salinian block wholly during the Neogene (Johnson and Normark, 1974). The borderland may have been bounded on the west by an active subduction zone and trench (Atwater, 1970), which possibly extended northwestward through the present northern Coast Ranges of California where it could be represented by the "coastal belt” Franciscan rocks (Berkland, 1972).

The sedimentary record indicates that the borderland was tectonically active; sedimentation was rapid and both basins and source areas were mobile. Uplift and vigorous erosion of granitic and metamorphic terranes is also suggested by the arkosic composition, freshness, angularity, and coarseness of sands derived from this region, and by the presence of pebble to boulder-size clasts of plutonic and gneissic rock. Very well rounded pebbles and cobbles of quartz, quartzite, chert, and por- , phyritic volcanic rock are common, indicating that older sedimentary rocks, including conglomerates, were also present in many borderland source areas.

Some basins subsided to bathyal-abyssal depths. Paleocurrent directions in basin deposits are varied, and in some cases, suggest that basins received sediments from two or more sides. Most of these deposits were clearly derived from source areas within the borderland. Shallow-marine deposits are rare, possibly due to subsequent deformation and erosion of basin margins. However, their absence also suggests that shallow-marine shelves were not well developed, so that sediments were transported from source areas directly to deep-marine environments.

Clastic sediments from borderland sources were deposited mostly as submarine fans, some of which apparently spilled eastward out of the borderland onto the floor of the San Joaquin basin. Some deposits represent several fans which coalesced to form a single, large﻿SUMMARY AND CONCLUSIONS

53

composite fan. The major early Tertiary deep-sea fans of the borderland were: (1) an early Paleocene to middle Eocene fan comprising the present German Rancho Formation of Wentworth (1968) in the Gualala area, the Cantua Sandstone Member of the Lodo Formation in the Vallecitos area and possibly the Tres Pinos Sandstone of Kerr and Schenck (1925) in the Bolado Park area; (2) an early to late Eocene fan comprising the Butano Sandstone in the Santa Cruz Mountains and the Point of Rocks Sandstone in the southern Diablo and northern Temblor Ranges; (3) a middle and late Eocene fan represented by The Rocks Sandstone of Thorup (1941) in the northern Santa Lucia Range; and (4) Late Cretaceous, Paleocene, and Eocene fans represented by deep-marine sandstone and conglomerate in the La Panza, southern Santa Lucia, and Sierra Madre Ranges. Other large deep-sea fans are represented by similar deposits located to the south in the Santa Ynez Mountains and adjacent areas (Stauffer, 1965, 1967; Link, 1971, 1972; O’Brien, 1972; Sage, 1973; Howell, 1974; Van de Camp and others, 1974). Smaller submarine fans may have developed within the borderland in the Point Reyes, Point San Pedro, and Point Lobos areas.

The deep-sea fan deposits are mostly thickly bedded, medium- to coarse-grained sandstone, but pebble to boulder conglomerates are prominent in several areas. They were probably funneled into the basin through submarine canyons; however, the sedimentary record of such basin margin deposition has been largely obliterated by post-Eocene uplift and erosion. Upper and middle fan facies dominate the fan deposits which are preserved, undoubtedly reflecting the coarseness and great volume of sediments, high rate of influx, and perhaps factors such as multiple sources of supply and physical restrictions on lateral growth of the fans. Upper fan facies comprise thickly bedded coarse-grained sandstones and conglomerates (interpreted as channel deposits) which are vertically and laterally juxtaposed with thinly interbedded sandstone, siltstone, and shale (interpreted as levee and interchannel deposits). Middle fan facies consist mostly of thickly bedded, medium- to coarse-grained sandstone which forms laterally discontinuous beds, reflecting the migration of major channels through time. These coarse-grained deposits bear evidence of deposition by various subaqueous gravity flow processes, including turbidity currents, fluidized sediment flows, and grain flows (Middleton and Hampton, 1973). Pebbly mudstones are generally rare in the borderland deposits.

Distal fan facies comprise thinly interbedded sandstones, siltstones, and shales, and more rarely, channel sandstones. This facies appears to have been poorly developed in borderland fans. Most very fine terrigenous sediments probably were transported in suspension

beyond the borderland where they were deposited on the adjacent ocean floors with clay and pelagic detritus to form hemipelagic shale, siltstone, and mudstone. The Kreyenhagen Formation in the San Joaquin Valley and Brabb’s (1964) Twobar Shale Member of the San Lorenzo Formation in the Santa Cruz Mountains represent such deposits. These fine-grained sediments also accumulated on deep-sea fans when and where coarsegrained clastic sedimentation was not occurring. Siliceous and phosphatic shales characterize the Kreyenhagen Formation and several other deep marine shale deposits (Dickert, 1966).

Large, deep-sea fans constructed westward from sources in the Sierra Nevada and Peninsular Ranges include (1) the Markley fan, of late Eocene age, represented by deep-marine sandstones in the Markley Sandstone Member of the Kreyenhagen Formation north of Mount Diablo, and (2) the Poway fan (Y eats and others, 1974), of Eocene to Oligoecene age, which has been reconstructed from shallow to deep marine conglomerate and sandstone presently exposed in the Santa Monica and Santa Ana Mountains, and on San Nicolas, Santa Rosa, Santa Cruz, and San Miguel Islands. The Poway fan deposits are thought to represent a delta which graded offshore westward into a large, unrestricted deep-sea fan of the open ocean, perhaps the only fan of this type preserved in the early Tertiary rock record of the California continental margin. Smaller fans from several different source areas are probably represented by various lower Tertiary deposits in the San Jose area. Other fans may have been constructed at the bases of "gorges” thought to represent submarine canyons, such as the Paleocene and early Eocene Meganos and Capay (Princeton) gorges of the Sacramento Valley.

East of the borderland, lower and middle Eocene shallow-marine sedimentary rocks derived from the Sierra Nevada and Peninsular Ranges contain quartz-ose, anauxitic, feldspar-deficient sandstone, residual pisolitic claystone, and conglomerate composed principally of resistant clast types (e.g., quartz, quartzite, chert, metavolcanic, and metasedimentary rocks). These deposits suggest a history of prolonged chemical weathering and a relatively quiet tectonic history. Upper Eocene and Oligocene deposits, in contrast, are composed largely arkosic and lithic sandstone, and conglomerates containing cobble to boulder-size clasts of granitic rock, suggesting increasing tectonic activity attended by uplift and rapid erosion. Along the east flank of the Diablo Range and in the northern Coast Ranges, middle Eocene and older shallow-marine and brackish-water sandstones contain glaucophane, serpentine, radiolarian chert pebbles, and other indicators of derivation from within the Franciscan assemblage, indicating that portions of the Diablo Range and north-﻿54

TERTIARY SEDIMENTATION AND TECTONICS, CONTINENTAL BORDERLAND OF CALIFORNIA

ern Coast Ranges were emergent during Paleocene and Eocene time.

The complete record of early Tertiary sedimentation and tectonics in California is characteristic of the complexities developed along transform fault boundaries that involve continental margins. The history of events and variety of processes that acted in the shelf, slope, ocean floor, trench, and borderland areas yielded a remarkably varied and rapidly changing paleogeography; related events and processes have continued to the present, yielding the complex geography of modern California along the modern San Andreas transform fault.

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Allen, J. E., 1946, Geology of the San Juan Bautista quadrangle, California: California Div. Mines Bull. 133, p. 9-75.

Allen, V. T., 1929, The lone Formation of California: California Univ. Pubs. Dept. Geol. Sci. Bull., v. 18, no. 14, p. 347-448.

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Anderson, Robert, and Pack, R. W., 1915, Geology and oil resources of the west border of the San Joaquin Valley north of Coalinga, California: U.S. Geol. Survey Bull. 603, 220 p.

Atwater, Tanya, 1970, Implications of plate tectonics for the Cenozoic tectonic evolution of western North America: Geol. Soc. America Bull., v. 81, no. 11, p. 3513-3536.

Atwater, Tanya, and Molnar, Peter, 1973, Relative motion of the Pacific and North American plates deduced from sea-floor spreading in the Atlantic, Indian, and South Pacific Oceans, in Kovach, R. L., and Nur, Amos, eds., Proc. Conf. Tectonic Problems of the San Andreas fault system: Stanford Univ. Pubs. Geol. Sci., v. 13, p. 136-148.

Axelrod, D. I., 1949, Eocene and Oligocene formations in the western Great Basin [abs.]: Geol. Soc. America Bull., v. 60, no. 12, p. 1935-1936.

Badger, R. L., 1957, Geology of the western Lion Canyon quadrangle, Ventura County, California: California Univ., Los Angeles, M. A. thesis, 84 p.

Bailey, E. H., ed., 1966, Geology of northern California: Calif. Div.

Mines and Geology Bull. 190, 508 p.

Bailey, E. H., and Blake, M. C., Jr., 1969, Late Mesozoic tectonic development of western California: Geotectonics, no. 3, p. 148-154, 225-230.

Bailey, E. H., Blake, M. C., Jr., and Jones, D. L., 1970, On-land Mesozoic oceanic crust in California Coast Ranges: U.S. Geol. Survey Prof. Paper 700-C, p. C70-C81.

Bailey, E. H., and Everhart, D. L., 1964, Geology and quicksilver

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------1970b, Eocene stratigraphy of northwestern Baja California, in

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