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A Contribution to the
Structural History of the

Vidal-Parker Region,
California and Arizona

By w. J. CARR

 

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1430

Prepared in cooperation with the
US. Nuclear Regulatory Commission

A report concerning stratigraphy, structure, and geophysics of a region within
the eastern Mojave Desert and Mojave-Sonoran structural-physiographic belt,
wherein tectonic activity has occurred at a very low rate since

late Miocene time. Important structural activity of Tertiary age

culminated and concluded in a

major regional episode of detachment faulting

 

 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1991

US. DEPARTMENT OF THE INTERIOR

MANUEL LUJAN, JR., Secretary

U.S. GEOLOGICAL SURVEY

Dallas L. Peck, Director

Any use of trade, product, or firm names in this publication is for
descriptive purposes only and does not imply endorsement by the
U.S. Government

Library of Congress Cataloging in Publication Data

Carr, Wilfred James, 1926—

A contribution to the structural history of the Vidal-Parker region. California and Arizona.
(US. Geological Survey professional paper ; 1430)
Bibliography: p.
Supt. of docs, no.: I 19.16zl430
l. Geology—Califomia—Vidal Region. 2. Geology—Arizona—Parker Region.
3. Geology, Structural. I. US. Nuclear Regulatory Commission. 11. Series.
QE90.VS3C37 1990 557.94’9 85—600261

 

For sale by the Books and Open-File Reports Section, US Geological Survey,
Federal Center, Box 25425, Denver, CO 80225

CONTENTS

 

Page
Abstract ........................................... 1 Stratigraphic history—Continued
Introduction ....................................... 2 Tertiary volcanic and sedimentary rocks—Continued
Purpose of investigation .......................... 2 Sedimentary rocks—Continued
Methods of study ................................ 2 Bouse Formation .........................
Acknowledgments ............................... 3 Correlation with surrounding areas ..........
Physiography and the Mojave-Sonoran Belt ............. 4 Tertiary and Quaternary deposits ..................
Stratigraphic history ................................ 4 Colorado River deposits ..........................
Metamorphic, intrusive, and sedimentary rocks ...... 4 Alluvial deposits ................................
Mesozoic, Paleozoic, and older(?) rocks ........... 4 Age of the alluvial units ..........................
Rocks at the east foot of the Riverside Mountains 4 Structure and tectonics of the Vidal-Parker area and surround-
Rocks of probable late Paleozoic age ......... 5 ing region ........................................
Possible structural significance of changes in General setting ..................................
character in the upper Paleozoic rocks ...... 6 Geophysics .....................................
Lower plate gneisses ...................... 6 Seismology ..................................
Mesozoic(?) rocks .................. , ....... 8 Magnetics ...................................
Granite gneiss ............................ 8 Gravity .....................................
Metamorphic rocks intruded by dikes and sills 9 Level line, by D. D. Dickey .......................
Granite and gneissic granite ................ 9 Structures in pre-Tertiary rocks ....................
Tertiary volcanic and sedimentary rocks ............ 9 Tertiary structures ..............................
Volcanic rocks ............................... 12 Stratigraphic-structural record .................
Andesite lavas ........................... 12 Middle Miocene unconformity ..................
Rhyodacite lavas ......................... 12 Whipple Mountains detachment fault ...........
Basaltic rocks ............................ 12 Regional implications ......................
Trachytic rocks in the Buckskin Mountains . . . 13 Origin of Whipple Mountains detachment fault
Peach Springs Tuff of Young and Brennan (1974) 13 and regional extension ...................
Sedimentary rocks ........................... 15 Early end of faulting .........................
Breccias ................................. 15 Pliocene-Pleistocene tectonics ...............
Conglomerate, sandstone, siltstone, and limestone 15 Summary of structural history .................
Fanglomerate of Osborne Wash ............. 16 References cited ....................................
ILLUSTRATIONS

PLATE 1.

[Plates are in pocket]

Geologic and structural unit map of the Vidal-Parker region, California-Arizona.

2. Generalized regional geologic and structural unit map and Bouguer gravity map of part of southeastern California

and western Arizona .

3. Generalized regional geologic and structural unit map and residual aeromagnetic map of part of southeastern Califor-

nia and western Arizona.

4. Tectonic map of Vidal-Parker region, California and Arizona.
5. Generalized topography of part of southeastern California and western Arizona.

FIGURE 1.

Index map of the eastern Mojave Desert ..............................................................
Map of the basins and ranges of Arizona, Utah, Nevada, and southeastern California ........................
Map showing postulated areal distribution of Permian rocks at localities in western Arizona, southern Nevada, and

southeastern California ..........................................................................
Composite diagrammatic columnar sections of Tertiary rocks in the Vidal-Parker region ......................
Distribution of the Peach Springs Tuff of Young and Brennan ...........................................
Relation of Tertiary and Quaternary deposits between the Whipple Mountains and Colorado River in the vicinity of

Parker, Ariz.

Page

17
18
19
19
19
19

21
21
22
22
23
24
25
26
28
29
29

31
33
35
35

37
37

Page

11
14

20

IV CONTENTS
Page
FIGURE 7. Seismic stations in the eastern Mojave Desert, 1974—77 ................................................. 22
8. Map and profile along part of the Colorado River aqueduct showing elevation differences between surveys in 1931 and
1975 ......................................................................................... 26
9. Section through the eastern Whipple Mountains showing configuration of the Whipple Mountains detachment fault 28
10. Structure contour sketch map of the Whipple Mountains detachment fault ................................ , 32
TABLES
Page
TABLE 1. Potassium-argon dates on granitic rocks in Vidal- Parker region ........................................... 9
2. Age of Tertiary volcanic rocks' in Vidal-Parker region ................................................... 10
3. Petrographic comparison of the phenocrysts of Peach Springs 'hiff of the Vidal- Parker region with those of the type
area in northwestern Arizona ............................................ V ........................ 15
4. Comparison of ash beds in sand of the Bouse Formation and in fanglomerate of Osborne Wash ............... 17
5. Faults and photo lineaments in old alluvium of the Vidal-Parker region .................................... 36

A CONTRIBUTION TO THE STRUCTURAL HISTORY OF THE
VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

By w. J. CARR

ABSTRACT

Geologic investigations in the area of the lower Colorado River
Valley have provided some new information that permits an integra-
tion of part of the geologic history for western Arizona and
southeastern California. The studies, aimed principally at evaluating
the recency of faulting in the eastern Mojave Desert, were done in
support of geologic evaluation of the region for proposed nuclear power
generating facilities.

Several maps are presented, including 12125.000-scale geologic map,
and regional compilations of geology, gravity, and aeromagnetics at
1:500,000.

Physiography, geology, and geophysics combine to delineate a
northwest-trending zone about 100 km wide, here named the Moj ave-
Sonoran Belt. This structural-physiographic feature can be viewed as
a southeastward extension of the Walker Lane Belt of western Nevada

Rocks of Precambrian, Permian, Cretaceous, Miocene, Pliocene. and
Quaternary age have been identified in the Vidal-Parker region. All
the pre-Tertiary rocks have undergone varying degrees of metamor-
phism. Although some rocks in the Riverside Mountains are probably
Precambrian. some evidence suggests that most of the rocks previous-
ly mapped in the Vidal-Parker region as Precambrian may be Paleozoic
or Mesozoic in age. A sequence of late Paleozoic rocks, mostly of Per-
mian age, has been recognized in several areas in the region. This se-
quence is characterized by a uniform, fine-grained quartzite that
probably correlates, not with the Coconino Sandstone, but with the
Esplanade Sandstone of the Supai Group, or with the Queantoweap
Sandstone of McNair (1951). Differences in the Paleozoic section be-
tween the Riverside and nearby Big Maria Mountains, and elsewhere,
suggest that major strike-slip faulting may have occurred between
those two areas.

One of the most widespread metamorphic rock units is a thick, fairly
uniform, partly mylonitic gneiss. This strongly banded or foliated rock
unit occurs above late Paleozoic rocks in several areas, and it is believed
to be Mesozoic in age. Potassium-argon and fission-track dates record
a minimum age of early Tertiary, however. On the other hand. rocks
of this unit differ in character from other Mesozoic(?) rocks in the
region.

Granite grading abruptly into granite gneiss is abundant in the
region. These rocks have been dated as Late Cretaceous by potassium-
argon techniques.

Tertiary rocks of the Vidal-Parker area are both Miocene and
Pliocene. but nearly all the volcanic rocks are Miocene. The Tertiary
stratigraphy is highly complex, units are discontinuous, and changes
are abrupt. Many pronounced unconformities occur. Breccias and
megabreccias are a prominent feature of the lithology. Two major lava
sequences, consisting of predominantly rhyodacite and andesite flows
and breccias, intertongue in the western Whipple Mountains. These
rocks range in age from about 22 to 18 my (million years).

Basaltic volcanism began about 15 my. ago and continued
sporadically for about 10 my. Many of the younger mafic lavas are

 

trachybasalts or basaltic andesites. A small center in the Buckskin
Mountains erupted trachytes and trachyandesites with peralkaline
affinities.

Peach Springs Tuff of Young and Brennan (1974), an important ash-
flow tuff stratigraphic marker, has been found at several localities
in the Vidal-Parker region. A map of the known localities of the tuff
shows a predominant northeast-southwest distribution, with a possible
source southwest of Kingman, Ariz.

Sedimentary material, ranging from megabreccia to lacustrine
limestone, dominates the Tertiary section in most areas. Megabrec-
cias consist of metamorphic and locally identifiable late Paleozoic
rocks. In some areas a prominent unconformity separates volcanic
rocks and breccias consisting of granitic and metamorphic rocks from
overlying thin-bedded sandstone. siltstone, and limestone.

A unit of detrital material called the fanglomerate of Osborne Wash,
overlies with sharp unconformity the highly disturbed older Tertiary
volcanic and sedimentary rocks. 0n the basis of dates on intercalated
lavas, this unit ranges in age from about 13 to 5 my.

The Bouse Formation, a late Miocene and Pliocene estuarine deposit,
found at scattered locations below about 330 m, grades upward
and laterally into what are interpreted as beach and eolian deposits.
The Bouse is generally overlain by deposits laid down by the Colo-
rado River, but in one area fluvial gravels are present beneath the
Bouse.

Alluvium in the Vidal-Parker region consists of old, highly dis-
sected gravels, of intermediate-age fan deposits displaying varying
degrees of soil and desert varnish formation. and of younger alluvium
related to present drainage. Ages of these units are imprecise, but
the oldest is probably Pliocene and Pleistocene; one of the more
prominent deposits of intermediate age is apparently about 80,000
years old.

The Vidal-Parker region is a somewhat anomalous part of the Basin
and Range physiographic province. It lies within a structural-
physiographic belt perceived to be a part of a major continental linea-
ment that extends from Texas to Oregon. In this area the lineament
is here named the Moj ave-Sonoran Belt. The northeast edge is marked
by a rather abrupt termination of northerly trending basins and ranges;
the southwest edge is less distinct but is defined partly by an en
echelon series of northwest-trending faults, commonly expressed
topographically. and having important components of strike-slip
displacement. Persistent lithologic changes take place along the
southwest belt margin in rocks of Paleozoic and Mesozoic age. Changes
in crustal configuration also appear to occur along the boundaries.
In the Vidal-Parker region, the belt is also characterized by (1) an
almost total lack of seismicity; (2) no surface faulting in intermediate-
age alluvium, and very minor faulting in rocks younger than about
5 m.y.; (3) only minor faulting since about 13 my ago, although
evidence exists that faults are younger and have more displacement
toward the boundaries of the Moj ave-Sonoran Belt; and (4) a lack of

1

2 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

deep alluvium-filled basins. These geologic conditions are reflected in
the aeromagnetic and gravity maps as a scarcity of pronounced linear
gradients or anomalies. The combination of less volume of unmetamor-
phosed granite in the crust of the Colorado River Valley with a distinct
gravity high extending from Yuma to Lake Mead suggests the
possibility that the estuary that existed in Bouse Formation time and
the course of the Colorado River were influenced by isostatic ad-
justments.

As a possible result of major strike-slip faulting, the style of pre-
Tertiary structure may also change across the boundaries of the
Moj ave-Sonoran Belt. In the northern Riverside Mountains, the rocks
are repeated by reverse faulting semiconcordant with bedding, accom-
panied by only local appressed folding, plastic deformation, and at-
tenuation. which seem to characterize the structure farther to the
southwest.

Striking features of the Tertiary deformation of the region include
(1) restriction of structural disturbance to a relatively short interval
of time, between' about 22—14 m.y. ago; (2) regionally pervasive
northwest-striking, southwest-dipping attitudes in Miocene rocks, and
abrupt truncation of these highly deformed rocks by nearly flat-lying
fanglomerates and volcanic rocks, mostly of Miocene age; and (3) a
lack of deep structural troughs common elsewhere in the Basin and
Range province.

Lithology and distribution of Tertiary rocks suggest abrupt uplifts
along northeast trends followed by regional extension along curving
low-angle faults joining a surface of widespread dislocation. The lat-
ter feature, called the Whipple Mountains detachment fault, spans
the Mojave-Sonoran Belt and is the master feature of late Cenozoic
tectonism. It developed rapidly about 15 my. ago and the upper plate
moved relatively northeastward, probably more than 20 km. Struc-
ture in the upper plate, though locally highly complex, is basically
a series of low-angle basin-and—range type faults that formed contem-
poraneously to accommodate the extension. Tertiary mineralization
appears to have a spatial relation to the fault.

The direct cause of the Whipple Mountains detachment fault is not
known. but the consistency of style and movement suggests at least
a regional and probably a plate tectonics mechanism, and possibly
a plastically extending substratum. It may not be coincidental that
initiation of Miocene movement on the San Andreas fault and ending
of displacement on the Whipple Mountains detachment fault both oc-
curred about 14 my. ago. It is suggested that the relatively early end
of late Cenozoic faulting in the Vidal-Parker region may be a result
of anomalously shallow depth of the boundary between plastic and
brittle crustal failure, so that during about the last 10 m.y., exten-
sion has taken place, but almost entirely by plastic flow.

Pliocene-Pleistocene tectonic features in the region are limited to
a few faults. mostly with a few meters of displacement, except at the
northeast edge of the area where several faults may have significant
Pliocene displacement. A few small faults are known to cut the Bouse
Formation. and a persistent zone of small faults occurs northwest of
Parker in beds possibly as young as the older alluvium. About a dozen
such small faults, fault zones, or lineaments were found in the region.
Only local slight warping appears to have occurred in Pleistocene and
Holocene time.

INTRODUCTION

PURPOSE OF INVESTIGATION

Work leading to this report is an outgrowth of the
interest of southern California power companies in the
eastern Mojave Desert as a site for nuclear reactors for

 

generation of electricity. In their search for areas of tec-
tonic stability, these companies recognized the poten-
tial of this area for reactor siting. The Vidal, Calif., site
(fig. 1) selected by Southern California Edison Company
is about 16 km west of Parker, Ariz. Extensive in-
vestigations by the company suggested that the area
is tectonically stable and apparently has been so for
several million years.

METHODS OF STUDY

A scarcity of detailed geologic information for the
eastern Mojave Desert prompted the US. Nuclear
Regulatory Commission to support the Geological
Survey in the present investigation, begun in 1974,
which was aimed principally at determining the recen-
cy of faulting. The Nuclear Regulatory Commission also
funded a separate project by the Geological Survey to
monitor the seismicity of the eastern Mojave Desert.
In 1974 a number of seismic stations were installed to
cover the general region between Needles, Calif., and
the Imperial Valley.

Early in the studies it was apparent that the near lack
of seismicity in the region was matched by a virtual
absence of Quaternary surface displacement along
faults. The region around the Vidal site displayed none
of the features of active tectonism common to much of
the rest of the Basin and Range physiographic province.
To document this tentative conclusion and to provide
a partial basis for understanding this unusual geologic
situation, it was decided to map in detail an area
centered about the Vidal site, chiefly Vidal Valley and
adjoining parts of the Whipple Mountains, Riverside
Mountains, and Mopah Range (fig. 1; pl. 1). Six 71/2'
quadrangles and parts of four other 71/2' quadrangles
were mapped in this phase of work, which was followed
by reconnaissance mapping of a larger area generally
surrounding the core of more detailed work.

Throughout the study, emphasis was placed on
searching for evidence of youthful faulting, so that most
of the effort was directed toward the stratigraphy and
structure of the upper Cenozoic rocks. N o detailed study
was made of the pre-Tertiary, generally metamorphosed
rocks, except in the Riverside Mountains, where an
attempt was made to divide a sequence of probable up-
permost Paleozoic and Mesozoic metamorphosed
sedimentary rocks. The Paleozoic and Mesozoic rocks
probably hold most of the keys to full understanding
of the major structural evolution of the region, but the
complex structure and metamorphism, as well as the
widely scattered outcrops, make understanding of the
stratigraphy very diffith and beyond the scope of the
present work.

 

INTRODUCTION 3
116%]0' 115°00' 114°00' 113°00'
35"00' I \ I
\
Needles a \
O ‘7'? MOHAVE
'Y(\

SAN BERNARDINO

_________._____J—_ _
34000' — —__
RIVERSIDE )
Blytheo lQO YUMA
A?
/‘* '
SUNDESERT SITEA 0V0

 

IMPERIAL

 

 

/

___T____l_____._..____

 

 

\ 1

 

33°OD'

FIGURE 1.—Index map of the eastern Mojave Desert, showing location of 1:24,000 scale maps (A, B, C), Vidal-Parker region (D) mapped
at 12125.000 scale (this report). and Vidal and Sundesert former proposed nuclear power reactor sites.

Even though the Vidal site was subsequently aban-
doned for plant technical reasons, the region remains
attractive geologically and tectonically for the siting of
nuclear facilities.

The main purpose of this report is to record and,
where appropriate, to interpret new geologic informa-
tion gained by Geological Survey and power company
investigations on behalf of the Nuclear Regulatory Com-
mission. This report should be regarded as an attempt
to synthesize, however tentatively, some fragments of
the geologic history and preliminary geophysics of the
eastern Mojave Desert in both California and Arizona,
particularly those aspects that bear upon the structural
history of the region.

It should be emphasized that the fieldwork for this
report was completed in 1975, and the report itself was
finished in 1977, just before a tremendous amount of
new geologic information became available on the
region. I have tried to include a few references on the
earliest new work but have not taken into account or
discussed all the implications therefrom. For further

references and papers, see the report edited by Frost
and Martin (1982).

ACKNOWLEDGMENTS

I am much indebted to my colleague, D. D. Dickey,
who was largely responsible for painstaking mapping
of most of the Quaternary deposits in the area. Even
though the work was done independently, we were aided
by the geologic groundwork laid down by consultants
to Southern California Edison 00.; Woodward McNeil
and Assoc; and Fugro, Inc. We are particularly in-
debted to W. B. Bull of the University of Arizona for
his fundamental stratigraphic subdivision of the
Quaternary deposits.

I acknowledge with thanks the cooperation of
Dr. Shawn Biehler of the University of California at
Riverside in providing gravity data for part of the
region. These data were substantially supplemented by
further gravity observations and data reduction by

 

4 STRUCTURAL HISTORY, VIDAL—PARKER REGION, CALIFORNIA AND ARIZONA

Frank E. Currey and D. L. Healey of the US. Geological
Survey.

Several potassium-argon dates were determined by
R. F. Marvin, and a fission-track age was obtained by
C. W. N aeser.

Reviews of the manuscript by D. D. Dickey and K. A.
Sargent of the Geological Survey were most helpful.

Several other members of the Geological Survey
assisted in various ways. F. G. Poole and P. T. Hayes
visited several areas of outcrop of the upper Paleozoic
rocks in the region andgave suggestions concerning
their stratigraphic correlation. G. O. Bachman exam-
ined and sampled some of the Quaternary deposits and
gave several helpful suggestions concerning the char-
acter and origin of the caliche zones.

I thank the Colorado River Indian Tribes for permis-
sion to study the geology on their reservation.

PHYSIOGRAPHY AND THE
MOJAVE-SONORAN BELT

The Vidal-Parker region (fig. 2) is part of a larger
physiographic and geologic belt, which lies in the south-
central part of the Basin and Range province. It is south
of the predominantly linear north-trending structures
of the province, southwest of the southern periphery of
the Colorado Plateau province, and northeast of the
northwest-trending ranges within the San Andreas and
central Mojave fault system (Fenneman, 1931, pl. 1).
The Vidal-Parker region is within the Sonoran Desert
section of the Basin and Range province; I propose the
name Mojave-Sonoran Belt (fig. 2; pl. 2) for this area
as it connects or is transitional between the Sonoran
Desert of southern Arizona and the Mojave Desert of
southeastern California (Carr and Dickey, 1977). Aside
from its geologic and geophysical characteristics, the
belt is distinguished physiographically by diversely
oriented ranges, most of which are less linear and have
less relief than most other ranges elsewhere in the Basin
and Range province. Bedrock crops out in many of the
valleys, and the slopes at the foot of the mountains are
widely pedimented.

The Colorado River crosses the heart of the Moj ave-
Sonoran Belt between the towns of Needles and Blythe,
Calif. Except for contiguous drainage incision and con-
siderable regional erosion, the physiographic effects of
the river are relatively minor. The course of the Col-
orado River in the Vidal-Parker region was influenced
by several factors, some of which will be touched upon
at various points in this report. It should be noted that,
whereas all of western Arizona has an integrated
drainage system into the Colorado River, several areas
immediately west of the river in California are closed

 

depressions with internal drainage (Ford Dry Lake area
west of Blythe and Rice Valley-Danby Lake area).

The Mojave-Sonoran Belt may be viewed as a
physiographic and structural southeastward continua-
tion of the Walker Lane Belt or structural zone of
western Nevada (fig. 2). I consider the Walker Lane Belt
to be a structural-physiographic zone as much as
100 km wide, rather than the narrow zone originally de-
fined by Locke, Billingsley, and Mayo (1940). Its
southwest edge is along the Fish Lake Valley—Death
Valley—Furnace Creek fault zone; the northeast edge is
defined physiographically by the southern termination
of northerly trending basins and ranges. In much of
southern Nevada this boundary is the Las Vegas Valley
shear zone. Other similarities in structural style of the
Walker Lane Belt and Mojave-Sonoran Belt will be
brought out later.

STRATIGRAPHIC HISTORY

Rocks of the Vidal-Parker region are divisible into
three general groups, partly in accordance with their
involvement with a major structural feature, the
Whipple Mountains detachment fault: (1) pre-Tertiary
metamorphic, intrusive, and sedimentary rocks in the
upper and lower plates of the fault; (2) Tertiary volcanic
and sedimentary rocks older than the detachment fault
and, in most areas, displaced by it; and (3) Tertiary and
Quaternary volcanic and sedimentary rocks deposited
after movement of the fault. Except for a few details
that bear specifically upon the structural history, only
general characteristics of the rocks are described here.
For details of individual map units, the reader is referred
to geologic maps of the area at 1:24,000 scale (Carr and
others, 1980; Carr and Dickey, 1980; and Dickey and
others, 1980).

METAMORPHIC, INTRUSIVE, AND
SEDIMENTARY ROCKS

MESOZOIC, PALEOZOIC, AND 0LDER(?) ROCKS

These units form the resistant cores of most of the
mountain ranges of the region, but their structural and
stratigraphic sequence is complex and not well
understood. I believe that many rocks of this group,
shown as Precambrian on local and regional geologic
maps, are Paleozoic or younger in age.

ROCKS AT THE EAST FOOT OF THE RIVERSIDE MOUNTAINS

Within the mapped area (pl. 1), some of the oldest and
structurally lowest rocks (lp, pl. 1) lie at the east foot

STRATIGRAPHIC HISTORY 5

117"

 

U 25

 

116“ 115”

W P§§OENIXO

 

 

50 75 100 MILES

l_|_J__J____|

FIGURE 2.—Basins and ranges of Arizona, Utah, Nevada, and southeastern California showing the location of the Vidal-Parker region,
Walker Lane and Mojave-Sonoran Belt, and San Andreas fault zone. White areas are basins; dark areas are ranges.

of the Riverside Mountains, where they are overlain in
low-angle fault contact by a sequence of partly
metamorphosed sediments of late Paleozoic and
Mesozoic(?) age. The unit consists largely of gneiss and
migmatite of highly variable composition. The poly-
metamorphic character and structurally low position
strongly suggest a Precambrian age, but no normal
depositional contact of lower Paleozoic beds on this
sequence was observed, even though W. B. Hamilton
(written commun., 1974) reported a depositional contact
to the south in the Big Maria Mountains.

 

ROCKS OF PROBABLE LATE PALEOZOIC AGE

Sedimentary rocks, mostly of late Paleozoic age (units
lz1, |22, uz1, uz2, and uz, pl. 1), are recognized in the
lower plate of the Whipple Mountains detachment fault
in the Riverside and Big Maria Mountains, Calif., and
in the upper plate of that fault in the Buckskin Moun-
tains, Ariz. One of the best exposed and least metamor-
phosed sections of this sequence, however, occurs
outside the geologically mapped area of plate 1 in the
Arica Mountains, a small range about 15 km southwest

6 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

of Rice, Calif. (See unit Pz, pl. 2.) Metamorphism has
destroyed virtually all fossils except for a few crinoid
stems seen in rocks in the Riverside Mountains. The sec-

tion commonly rests structurally on gneissic rocks, .

which are probably Precambrian in some areas. Low-
angle faulting, resulting in both attenuation and repeti-
tion, makes mapping of individual units very difficult.
In general, however, the section consists of three main
parts, a lower rather thin-bedded carbonate and shaly
zone, a middle quartzite sequence, and an upper fairly

massive limestone and dolomite sequence. Were it not ,

for the presence of the quartzite, which is distinctive,
identification of this group of rocks would be difficult.
The quartzite is thin bedded, fine grained, and quite
uniform. It lacks prominent crossbedding and is dis-
tinctly finer grained than typical Coconino Sandstone.

The quartzite of the Vidal-Parker region is tentative-
ly correlated with the Queantoweap Sandstone of
McN air (1951) or the Esplanade Sandstone of the Supai
Group (McKee, 1975) in northwestern Arizona. Above
the quartzite, limestone and dolomite beds contain local
quartz sand zones overlain by more massive limestone
and dolomite that are probably generally correlative
with the Kaibab Limestone of northwestern Arizona.
The sandy zones may be stratigraphically equivalent
to the Coconino Sandstone. Keith Howard (written
commun., 1979) of the US. Geological Survey believes
that the quartzite in the Arica Mountains, as well as
similar rocks in the Kilbeck Hills and Little Piute Moun-
tains (pl. 2), is Coconino, even though the quartzite lacks
crossbedding.

More typical Coconino occurs in the Plomosa (Miller
and McKee, 1971) and Harquahala Mountains of
Arizona and in the southern Big Maria Mountains,
Calif. (W. B. Hamilton, written commun., 1974; fig. 3).
I visited the last two localities in company with F. G.
Poole, P. T. Hayes, and D. D. Dickey of the Geological
Survey, and all agreed that quartzites typical of the
Coconino are present. It was also concluded that the
quartzite of the Arica, Riverside, and Buckskin Moun-
tains is not typical of the Coconino; hence, the tentative
correlation of the quartzite with the Esplanade or
Queantoweap Sandstones. In my opinion, quartzite in
Miller and McKee’s (1971) deformed section in the
Plomosa Mountains resembles the Esplanade Sand-
stone, not the Coconino Sandstone. At the southern Big
Maria Mountains section, two arenaceous formations
are present. The lower, correlated by W. B. Hamilton
(written commun., 1974) with the Supai Group, is alter-
nating brown sandstone and gray silty and sandy car-
bonate rock. This unit has a soft slope at the top that
is somewhat loosely cemented gypsiferous sandstone.
Above it is typical Coconino, a fairly pure quartzite with
large crossbeds. This section of Pennsylvanian-Permian

 

rocks in the southern Big Maria Mountains is quite dif-
ferent from rocks of the same probable age in the River-
side Mountains only 40 km to the north, or in the Arica
and Buckskin Mountains to the northwest and north-
east; none of these localities, a short distance to the
north of the Big Maria and Plomosa Mountains, exhibit
any typical Coconino Sandstone. Structural thinning of
the sections has probably occurred in some areas, but
the difference in quartzite lithology in the northern
versus the southern sections appears to be real.

Above the sandstone or quartzite interval in all the
sections is a sequence of relatively pure but locally
cherty massive limestone, dolomite, or marble which
corresponds in a general way with the Permian Kaibab
Limestone. More carbonate rocks, possibly of Mesozoic
age, are present locally above the Kaibab-type lime-
stones. In several areas these units are overlain by
strongly foliated banded gneisses.

POSSIBLE STRUCTURAL SIGNIFICANCE OF CHANGES
IN CHARACTER IN THE UPPER PALEOZOIC ROCKS

The abrupt change of the Pennsylvanian-Permian sec-
tion between the Big Maria and Riverside Mountains,
and in a short distance within the Plomosa Mountains,
and the regional pattern of distribution of these rocks
to the north (fig. 3) strongly suggest structural displace-
ment. Miller and McKee (1971) cited thrusting to ex-
plain the dissimilar sections in the Plomosa Mountains.
Assuming northerly facies trends, the absence of
Coconino-like lithology in the Arica, Riverside,
Buckskin, and part of the Plomosa Mountains suggests
that strike-slip faulting as well as thrusting may be
responsible. Longwell, Pampeyan, Bowyer, and Roberts
(1965, p. 36) pointed out the anomalous presence of
Coconino Sandstone at Frenchman Mountain near Las
Vegas, and R. G. Bohannon and R. E. Anderson (oral
commun., 1978) believe that its presence there is due
to westward shift on a major zone of strike-slip faults
(fig. 3).

LOWER PLATE GNEISSES

The most extensively exposed pre-Tertiary rock in the
Vidal-Parker region is fairly uniform, finely banded, or
foliated feldspathic gneiss (lower plate gneisses, unit lg,
pl. 1) that makes up the cores of several of the moun-
tain ranges in the region. It is more than 500 m thick
in the Whipple Mountains. Much of the unit is mylonitic
and superficially resembles metamorphosed flow-
banded lava, but in many areas it consists of a smeared
and metamorphosed granitic complex. Some of these
rocks in the Whipple Mountains were placed in the am-
phibolite facies grade of metamorphism by Terry (1972).

STRATIGRAPHIC HISTORY

113" 115° 114‘1
i ll - I

37" _

  
 

Mountains X

   

éNorth Grand
Wash Cliffs

    

|

|

. . |
Virgin |
l
|

    
  

   

 

     
 

 

 

 

 

 

 

 

X H
Ocim‘é
®East Spring XS .
Mo t ns outh Hurricane
\ u" a" ‘ \ OCIiffs
South Springs \ \
{Mountains \\
\
\ \
\ i \\
\ \ \
\\ 1 \
\\ ) \\ X Aubrey
\l ARIZONA 0""3
35" — l \‘ __.
\K :
l
I
I
/
/
/
/
/
CALIFORNIA I BUCKS“? //\Approximate western limit
Arica /’OM°“""3'“S // of Coconino Sandstone
Mountains 1’ //
34" — \9 Riverside / “
- \ Mountains /
\ // Harquanala
South Big Maria 0 // X Mountains
Mountains J /
J //PI //
’ Max:513: / PHOENIXO
(
l
| [‘x I I
0 2.5 510 7? H110 MILES
i I I I r
[l 25 50 75 100 KILUMETEHS
EXPLANATION
® PERMIAN ROCKS—Coconino or Esplanade

Sandstone not separated

O ESPLANADE SANDSTONE (Queantoweop __4—_.__?_ FAULT OR FAULT ZONE—Arrows show dime
Sandstone Of MCNa'“ 195” tion of movement; queried where uncertain

X COCONINO SANDSTONE

FIGURE 3.—Postulated areal distribution of Permian rocks at localities in western Arizona. southern Nevada,
and southeastern California.

8 STRUCTURAL HISTORY, VIDAL—PARKER REGION . CALIFORNIA AND ARIZONA

Augen gneiss, quartzite, and marble of late Paleozoic
or Mesozoic(?) age are included in the lower part of the
unit in some areas. In the Vidal-Parker region, the well-
banded or laminated gneiss occurs only in the lower
plate of the Whipple Mountains detachment fault.
Davis, Anderson, Frost, and Shackelford (1980) and
Anderson, Davis, and Frost (1979) described these rocks
in the Whipple Mountains in some detail. These authors
pointed out that the mylonitic zone or “carapace” of
metamorphism cuts across these gneissic lower plate
rocks.

The age, structural history, and thermal history of
the banded gneiss and lower plate rocks in general are
not precisely known. A K-Ar (potassium-argon) date of
46.7il.1 m.y. (million years) (R. F. Marvin, written
commun., 1976) was obtained on feldspar from augen
gneiss near the base of the unit in the northeastern part
of the Riverside Mountains. Zircon from the same
sample yielded a fission-track age of 62.1:3.7 my
(C. W. N aeser, written commun., 1977). These ages must
be considered as only approximate minimums, but they
follow rather closely the end of major Mesozoic-early
Cenozoic plutonic activity in southern Arizona and
southeastern California (Armstrong and Suppe, 1973).
Support for a general correlation between the dated rock
in the lower plate of the Whipple Mountains detachment
fault in the Riverside Mountains and similar rocks in
the lower plate in the northeastern Whipple Mountains
is found in a K-Ar date on hornblende reported by Terry
(1972) of 41.5:t3 m.y. However, several nearly concord-
ant fission-track ages of about 19 my. were reported
by Dokka and Lingrey (197 9) from lower plate gneisses
in the eastern Whipple Mountains.

Metamorphic rocks of this general type have been
called Precambrian by previous w0rkers (W. B.
Hamilton, written commun., 1974; Bishop, 1963; Wilson
and others, 1969) in the Vidal-Parker region. Several
factors suggest that most of these rocks may not be
Precambrian, but Mesozoic in age. In two places in the
mapped area, gneisses with dolomite or marble and
quartzite intercalated near the lower contact overlie
sedimentary rocks of probable late Paleozoic age. In the
Riverside Mountains this carbonate rock-quartzite-
gneiss sequence occurs in the lower plate of the Whipple
Mountains fault; in the western Buckskin Mountains
northeast of Parker, a very similar sequence of upper
Paleozoic rocks is overlain by gneissic granite in the
upper plate of that fault. In the Big Maria Mountains,
W. B. Hamilton (written commun., 1974) mapped rocks
of this general type, which he called “Mesozoic
greenschist” or metavolcanic and metasedimentary
rock, as structurally overlying the upper Paleozoic sec-
tion. At most localities these probable Mesozoic rocks
have been mapped with low-angle faults separating

 

them from the underlying Paleozoic units, but the fact
that similar marble beds occur near this contact at
several widely separated places suggests that the
faulting is not major. Relationships with subj acent up-
per Paleozoic and lower Mesozoic(?) sedimentary rocks
suggest that the banded gneiss may be the thick
smeared-out margin of a large semiconcordant pluton.
The mylonitic gneiss is best developed in the range core
relatively near the Whipple Mountains detachment
fault of Miocene age, implying a relationship between
the gneiss and fault. However, the discordance between
the mylonite and other rocks of the lower plate suggests
separate tectonic episodes.

MESOZOIC(?) ROCKS

A separate group of rocks (unit Ix, pl. 1), found only
in the southeastern Riverside Mountains in the Vidal-
Parker region, is also believed to be Mesozoic (Hamilton,
1964) in age, but these rocks are somewhat different
from other probable Mesozoic sections in the region.
The rocks consist of mostly low-grade metasediments
including sandstone, minor amounts of conglomerate,
marble and dolomite with phyllite, greenschist, and one
interval of probable metatuff. Lower Triassic rocks
generally similar in description to the southeast River-
side Mountains sequence have been reported in the
Providence Mountains about 140 km to the northwest
(Hazzard and others, 1938). Pelka (1973, p. 35) has
pointed out the vague similarity between Mesozoic(?)
rocks of the Big Maria and Riverside Mountains and
his Palen formation of probable Triassic age in the
northern Palen Mountains about 50 km to the south-
west, which Pelka has called the Palen Formation for
those mountains. I was impressed, however, by the dif-
ferences in character of these rocks, particularly be-
tween those of the Riverside and Palen Mountains.

GRANITE GNEISS

Gneissic rocks (unit ug, pl. 1), making up part of the
upper plate of the Whipple Mountains detachment
fault, crop out on the flanks of the Whipple, Buckskin,
and Riverside Mountains. Although locally variable,
these rocks tend to be granitic in texture and composi-
tion and appear to grade laterally into gneissic granite
in several areas. Dark pyroxene- and sphene-bearing
phases of the unit are present locally. These rocks are
generally much broken by structural movements within
the upper plate of the Whipple Mountains detachment
fault. Some of the gneiss is locally incorporated as brec-
cia and megabreccia within the Tertiary section; in some
areas blocks are so large that determination of such
reworking is difficult.

STRATIGRAPHIC HISTORY 9

The age of the upper plate gneissic rocks has not been
definitely determined, but dates on the granitic rocks
(unit Kgg, pl. 1) into which the gneisses appear to grade
suggest that much of the gneiss is Mesozoic, probably
Cretaceous, in age.

METAMORPHIC ROCKS INTRUDED BY DIKES AND SILLS

Another unit (mr, pl. 1), shown separately on the
geologic map, occurs in the metamorphic rocks of the
lower plate in the western Whipple Mountains. An area
of similar rock, not separately mapped, occurs in lower
plate gneisses farther east, between Savahia Peak and
Chambers Well. The map unit consists of gneiss and
schist intruded by swarms of dikes and sills of rhyo-
dacite or diorite. Much of the intrusive rock is hydro-
thermally altered, and determination of texture and
mineralogy is difficult. It cannot be ruled out that these
intrusives are Tertiary in age, and, indeed, they occur
only a few kilometers east of a large area of Tertiary
rhyolite and rhyodacite lavas. However, field relations
suggest that the unit is cut by granitic intrusive rocks,
which elsewhere are mostly late Mesozoic in age.

GRANITE AND GNEISSIC GRANITE

Granites and gneissic granites (units Kg and Kgg, pl.
1) do not make up a large volume of the rocks in the
mapped area, except in the West Riverside Mountains
(pl. 1). Scattered smaller areas of granitic rocks occur
around the periphery of the Whipple Mountains, in the
Riverside Mountains, and in the vicinity of Moon Moun-
tain 35 km south of Parker. Medium- to coarse-grained
granite and quartz monzonite are the most common
rock types. As mentioned previously, the granites
typically grade into gneissic granite of similar composi-
tion. In most areas, as in the West Riverside Mountains,
the gradation is fairly abrupt.

Several K-Ar dates on granitic rocks have been ob-
tained on biotite and feldspar from scattered localities
in the mapped area and are listed in table 1.

Except for the date of 146 my. on hornblende
reported by Terry (1972) from the northeastern part of
the Whipple Mountains, these dates from the Riverside,
Turtle, and southern Whipple Mountains agree quite
well. The close agreement in age between the samples
from the West Riverside Mountains and those from the
southern Turtle Mountains suggest that these granites
are parts of the same plutonic episode, even though the
rocks in the Turtle and Riverside Mountains are
somewhat different mineralogically.

Two other K-Ar dates on granite outside the Vidal-
Parker area were obtained by consultants to San Diego

TABLE l.—Potassium-argon dates on granitic rocks in Vidal-Parker
region

 

 

Date and error

Sample Location (million years) Reference

 

-—- West Riverside Mts. 98.514.0 Bishop (1963).
SC-69'62 DO.
56-69-63 Turtle Mts., eastern

SC-69-64 Do.

92.8tl.9
95.6tl.9
93.6tl.9

Armstrong
and Suppe,
(I973).

MWC-39-74
biotite
orthoclsse.

Whipple Mts., southern
87.9:2.l
90.711.4

This report.1

KA 700
RA 704

146:10
81:2

Whipple Mts., northeastern

Whipple Mts., southeastern Terry (1972)'

R. E. Anderson
(U.S. Geological
Survey, oral
commun., 1975).

—-- Chemehuevi Mts. 60

 

1U.S. Geological Survey K—Ar ages given in this report have been
corrected for new constants.

Gas and Electric Co. (1976, v. 2, fig. 2.5-28). These dates
from the northeastern Mule Mountains southwest of
Blythe are 96.0:3.6 and 89.4:33 m.y.

All the above dates agree well with those on maps of
dated Mesozoic and early Tertiary igneous rocks in
southwestern United States prepared by Armstrong
and Suppe (1973). It would appear, however, that the
new dates serve to strengthen a pattern of northwest-
trending age (or metamorphic) belts of plutons in the
Mojave Desert region. These belts seem to crosscut the
boundary of the area of large volumes of granite (as
outlined by Armstrong and Suppe, 1973), and they may
persist southeastward into the region of the Colorado
River where granitic bodies are fairly numerous but
smaller in volume.

TERTIARY VOLCANIC AND SEDIMENTARY ROCKS

Rocks of Tertiary age in the Vidal-Parker region are
Miocene and Pliocene, but all the volcanic rocks of
significant volume are Miocene (table 2). Several K-Ar
dates support this conclusion, as will be discussed later.

Except possibly in the Mopah Range, the preserved
sequences of Tertiary rocks are normally less than
about 1,000 m thick, but they are characterized by
abrupt changes in thickness and lithology. These are
illustrated in figure 4, which shows a general strati-
graphic sequence for each of five areas. With the excep-
tion of a few discontinuous key units, correlations
between parts of the section are equivocal, owing to
complex structure, unconformities, and lateral changes.
One cannot normally find the exact section depicted in
figure 4 at any single locality. However, despite the
variability, certain general features of the section can
be recognized in most areas.

10 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

TABLE 2.-——Age of Tertiary volcanic rocks in Vidal-Parker region

 

 

 

Sample numberl/ Rock type, name or locality Age, millions of yearsg/
5 IO I5 20 25
W I I l I l I I I l I I l I I I
MWC—72-74 Andesite of West Portal I
ch-55-74 Andesite of Osborne Mash I
F—l Andesite of Osborne Wash [22:]
RD—l6 Basalt, Buckskin Mountains [:2] '“'e’°°'°'°d "it“
YU-l79-Pw Basalt, Buckskin Mountains l '°"9'°"‘e "“e °f
Osborne Wash
MNC—56—74 Basalt of Lake Moovalya -
RD—Zl Basalt, Black Peak [:23
MWC—3l-76 Basalt of the Mopah Range
ch-79-74 Peach Springs Tuff 335.129 T ‘
MWC-30-76 Andesite of Vidal -
V-l Andesite of Vidal -
MQ-4 Rhyolite lava, Mopah Range {mg-313“ ‘
2:33;} 3/ Andesite, south end Turtle Mountains :5
$233} y Andesite, south end Turtle Mountains E:
FK-l Andesite, South Whipple Mountains
FK—2 Andesite, South Whipple Mountains - —

 

 

 

 

 

1] Samples arranged in probable stratigraphic order.
Data sources: ’
MNC and MO: Marvin, R. F., and Dobson, S. w., 1979, Radiometric ages:
Isochron/west, no. 26, p. 6 and lO—ll. (Note:
(p. l0) for MMC-3l-76 directly beneath Peach Springs Tuff.
Range, which directly overlies the Peach Springs: hence, age is not unreasonable)

Compilation B, U.S. Geol. Survey:
Above reference erroneously places determination no. 66
This sample is from basalt of the Mopah

Dickey, D. D., and

others, l980, Geologic map of the Parker N.w., Parker, and parts of the Whipple Mountains s.w. and

Whipple Wash quadrangles, California and Arizona:

U.S. Geol. Survey Map I-l124; Carr, w. J., and

others, l980, Geologic map of the Vidal N.w., Vidal Junction and parts of the Savahia Peak SM. and

Savahia quadrangles, California: U.S. Geol. Survey Map 1-1126.
F-l, V—l, FK-l, FK—2, (3—597, —598, -599, -600:
generating station, Southern California Edison Co., l974, v. II, sec. 2.5, p. 36-37.

RD-l6, RD-2l: Early site review report, Sundesert nuclear plant, San Diego Gas and Electric (30., 1976,
Amendment l0, figs. 2.5—28.
YU—l79—Pw: Armstrong, R. L., and others, l976, K-Ar dates from Arizona, Montana, Nevada, Utah, and

Wyoming: Isochron/west, no. l6, p. 4.

Information concerning site characteristics, Vidal nuclear

9 Solid bar represents a date considered reasonable, and a sample whose stratigraphic position is known;
open bar, a sample whose age may be spurious or whose stratigraphic position is uncertain.

é/ Two samples from the same locality.

Virtually no detailed work had been published on the
Tertiary rocks of the Vidal-Parker region prior to our
field studies (Carr and others, 1980; Dickey and others,
1980;
described the stratigraphy in the southeastern Whipple
Mountains in an unpublished work which was done on

behalf of the Metropolitan Water District of Southern
California in the early 1930’s. He applied, informally,
the names Gene Wash and Copper Basin to formations
of Tertiary rocks along the route of the aqueduct
through the Whipple Mountains. His reports are in the
files of the Metropolitan Water District of Southern

Carr and Dickey, 1980). F. L. Ransome briefly

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12 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

California. Kemnitzer (1937) used these names in his
structural study of the Whipple Mountains. Because of
the abrupt stratigraphic changes in the region, these
names are not used in the present work.

VOLCANIC ROCKS

Lava flows and associated tuffs and breccias make
up the majority of the Tertiary section only in the
Mopah Range and western Whipple Mountains, and in
a small group of hills in Chemehuevi Valley west of Lake
Havasu City (pl. 1). Compositionally, they range from
rhyolite to basalt, but most of the rocks are rhyodacitic
to andesitic. Nearly all the volcanic rocks lack, or have
only very minor amounts, of phenocrystic quartz. A few
partial chemical analyses, representative of the major
rock types, are given on the geologic quadrangle maps
(Dickey and others, 1980; Carr and others, 1980).

ANDESITE LAVAS

In general the oldest volcanic rocks are andesites,
although in the western Whipple Mountains and Mopah
Range, andesites are intercalated with rhyodacite lavas.
Andesite lavas and breccia flows are prominent around
the periphery of the Whipple Mountains, reaching their
greatest volume in the southeastern Whipple Moun-
tains where they commonly intertongue with reddish-
brown granite gneiss breccia and arkosic conglomerate
and sandstone. Dikes of altered andesite are present in
the pre-Tertiary upper plate basement rock of the
eastern Whipple Mountains, and, together with the
distribution of the lava, point to that general area as
the source. However, as discussed later, the upper plate
rocks are allochthonous and have probably been
transported many kilometers in a northeasterly direc-
tion with respect to the lower plate. Characteristically,
the dark fine-grained lavas in the Whipple Mountains
are breccia flows—used here to mean lava breccia con-
sisting entirely of fragments enclosed in a lava matrix
of the same material. That these are not tectonic or land-
slide breccias is indicated by the fact that they contain
or are locally in depositional contact with sedimentary
rocks that are undisturbed. Breccia of this type has been
described in the Cane Spring quadrangle in Nevada
(Poole and others, 1965). Zeolites and calcite are
characteristic alteration products, and copper carbonate
stains are seen commonly on fracture surfaces.

A particularly distinctive unit, an andesite porphyry,
is locally present in many areas, generally near the base
or in the lower part of the Tertiary section. It is typically
a dark-purplish-gray rock crowded with flow-alined
plagioclase laths as much as 2 cm long—a kind of coarse
trachytic texture. It displays both extrusive and

 

intrusive relations and occurs in scattered small areas
throughout the Vidal-Parker region. If all the occur-
rences are the same age, the porphyry records a
widespread synchronous magmatic event.

RHYODACITE LAVAS

Rhyodacite lavas and flow breccias make up the bulk
of the Mopah Range and are present in the western
Whipple Mountains and hills in Chemehuevi Valley. In
the southern Mopah Range, eight separate flows were
mapped (Carr and others, 1980). Many of these cannot
be easily identified separately in the field, and in the
western Whipple Mountains where the lavas are exten-
sively altered and faulted they were not mapped
separately. At least one flow is a rhyolite. None of the
flows contain sanidine feldspar phenocrysts, and sparse
quartz occurs only in the rhyolites. The oldest units con-
tain prominent biotite and hornblende; the youngest
contain clinopyroxene and orthopyroxene as the pre-
dominant mafic minerals.

Thick flow breccias, thin air-fall tuffs, and one
nonwelded ash-flow tuff are associated with the lavas.
Several plug domes are present which probably served
as feeders for some of the flows. The location of these
plugs and the general characteristics and distribution
of the lavas and tuffs, together with a distinct gravity
low (pl. 2) just east of the Mopah Range, suggest that
area is the eruptive center.

Rhyodacites interfinger with andesites in the western
Whipple Mountains west of Savahia Peak. Unfortu-
nately, individual flows could not be mapped or cor-
related directly with andesites to the east or rhyodacites
to the west. It is reasonable, however, on the basis of
field relations, isotopic dates, and general lithology, to
conclude that the andesite of the Whipple Mountains
and rhyodacite lavas of the Mopah Range are at least
partly contemporaneous.

Dates were obtained on biotite and hornblende from
a rhyolite flow near the southern end of the Mopah
Range. The rock is a vitrophyre at the base of a flow near
the middle of the exposed sequence. Biotite gave an age
of 18.9:05 m.y., and hornblende, 18.2iO.8 m.y. (R. F.
Marvin, written commun., 1976). On the basis of this
date and field relations, an age of about 27 m.y., obtained
by consultants to Southern California Edison Co. (Infor-
mation Concerning Site Characteristics, Vidal Nuclear
Generating Site, v. 2, table 2.5-2) on a flow stratigraph-
ically higher in the sequence, appears to be erroneous.

BASALTIC ROCKS

Basalt and basaltic andesite are prominent in the up-
per part of the volcanic sequence. These flows appear

STRATIGRAPHIC HISTORY 13

to have originated from two separate areas—the Mopah
Range and the Buckskin Mountains. Exact source areas
in the Mopah Range have not been identified. Basalt
crops out near the center of Vidal Valley (pl. 1) and ex-
tends in a belt about 70 km northwestward to the
Stepladder Mountains (pl. 2). In the Mopah Range area,
a variety of mafic rocks are mapped in this group, in-
cluding a few dark trachyandesites. Several thin
scoriaceous basalt flows are intercalated with the
rhyodacite lava flows; most of these basalt flows con-
tain olivine, and one is characterized by a lack of
clinopyroxene. Basalts generally younger than the
rhyodacite lavas include the basalt near Vidal, which
contains rare olivine and a few quartz xenocrysts, and
another flow possibly related to the basalt near Vidal,
which contains both clinopyroxene and orthopyroxene
and lacks olivine. The most widely exposed series of
basalts in the Mopah Range area that overlie the
rhyodacite lava pile, are also probably younger than the
Peach Springs Tuff. They are typical olivine basalts.

Most, if not all, of the basaltic rocks of the Buckskin
Mountains and southern Whipple Mountains area
(fig. 4) are intercalated in the fanglomerate of Osborne
Wash; they are shown separately (pl. 1) only where they
are fairly thick and continuous. These basalts are
distributed in a poorly defined belt from the Cactus
Plain southeast of Parker northward through the
Buckskin Mountains and across the Bill Williams River
as far as the south edge of Dutch Flat (pl. 2). The
presence of pyroclastic deposits and feeder dikes in-
dicates that the vent area for most of these flows lies
in the Buckskin Mountains near the head of Giers
Wash, about 20 km northeast of Parker.

Basalts of the Buckskin Mountains area are also
variable in composition and mineralogy. One of the
distinctive flows, called the basalt of Lake Moovalya
(Dickey and others, 1980), is recognized only in the area
northeast of Parker, but similar rocks are mentioned
by Suneson and Lucchitta (1978) in the area northeast
of the Bill Williams River. The rock is a porphyritic
olivine basalt containing conspicuous megacrysts of
plagioclase and olivine as much as 1.5 cm across.

Younger flows in the group tend to be less mafic; some
are basaltic andesite and a few may best be called
trachybasalts. Commonly, they are diabasic in texture
with small olivine phenocrysts. One of the youngest
flows, the andesite of West Portal (Dickey and others,
1980), occurs in a small area north of Parker on the
flanks of the Whipple Mountains. It is characterized by
rare corroded quartz xenocrysts with clinopyroxene
coronas, indicating a stage of disequilibrium in the
crystallization history of the rock.

Several dates are available for basalts of the Vidal-
Parker region (table 2). A few additional dates have been

 

reported (Damon, 1970, p. 40; Eberly and Stanley, 1978;
E. G. Frost, San Diego State University, written
commun., 1960), but they are omitted here because
they appear too old based on present field knowledge.
Even so, it is obvious that basaltic volcanism in the
region continued sporadically for a long time—at
least 10 my. Most of the dated basalts are intercalated
in the fanglomerate of Osborne Wash, near the edges
of the basaltic eruptive center in the Buckskin Moun-
tains, which indicates an equally long period of time
for accumulation of that generally coarse detrital
deposit.

The youngest dated basaltic rock is the previously
mentioned andesite of West Portal, a relatively insignifi-
cant unit dated at about 6 my. (table 2). The only other
younger basalt occurs on the Cactus Plain, 22 km south‘
east of Parker, where a slightly eroded undated basaltic
cinder cone occurs in a sand dune area.

TRACHYTIC ROCKS IN THE BUCKSKIN MOUNTAINS

During reconnaissance mapping of the Buckskin
Mountains east of Parker, an interesting group of lavas
was found unconformably underlying basalts of the
fanglomerate of Osborne Wash (sec. D, fig. 4). Although
chemical analyses are not available, petrographic ex-
amination revealed that these rocks are trachytes and
trachyandesites with peralkaline affinities. They con-
tain phenocrysts of alkali feldspar in a groundmass of
glass or microlites of sodic plagioclase. Most flows ex-
amined contained a few phenocrysts of iron-rich olivine,
and iron- and soda-rich clinopyroxene, probably acmite
or aegerine. No biotite or phenocrystic quartz is present.

Age of these trachytic lavas is not precisely estab-
lished, but because they directly underlie basalts in the
fanglomerate of Osborne Wash, it is likely that they are
older than about 13 m.y.; their freshness and general
appearance suggest that they are probably not much
older than the basalts of Osborne Wash. An age of
about 14 my. is suggested, which is very nearly the
same as the age of two major centers that erupted
peralkaline rocks in the southern Great Basin (Noble,
1968; Noble and others, 1968).

PEACH SPRINGS TUFF OF YOUNG AND BRENNAN (1974»)

An important marker unit in the Tertiary of the Vidal-
Parker region is the Peach Springs Tliff. This ash-flow
tuff is widely distributed across the margin of the Col-
orado Plateau in northwestern Arizona (Young and Bren-
nan, 1974; Lucchitta, 1972). It was recognized in the
Vidal-Parker region during the present field studies. The
known distribution of the Peach Springs ’Iliff (fig. 5)

14

 

 

 

 

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EXPLANATION
>< PEACH SPRINGS TUFF OUTCROP
I LAVA FLOWS PETROGRAPHICALLY SIMILAR

TO PEACH SPRING TUFF

APPROXIMATE LIMIT OF PEACH SPRINGS TUFF;
queried where uncertain

FIGURE 5.—Distribution of the Peach Springs ’I‘uff of Young and
Bremen (1974). Data in northeastern two-thirds of area from Young
and Brennan (1974) and Ivo Lucchitta, US. Geological Survey (oral
commun., 1977).

shows an elongate pattern trending northeast more
than 200 km from Rice Valley in California to the
Hualapai Plateau in Arizona. The exposure localities
shown in figure 5 are generally quite small and irregu-
larly distributed and probably do not adequately repre-
sent the tuff distribution in the center of the belt,
particularly in the area between Needles and the
Hualapai Mountains. Anderson, Longwell, Armstrong,
and Marvin (1972) dated an ash-flow tuff in the Patsy
Mine Volcanics of the north-central Black Mountains
(fig. 5). This tuff gave widely divergent ages from
18.6 my on the whole rock to as much as 40.8 my. on
biotite. Anderson suggested that the younger age is

 

STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

more reasonable, and Young and Brennan (1974) men-
tion this tuff as a possible correlative of the Peach
Springs. I examined thin sections of ash-flow tuff in the
Patsy Mine Volcanics collected by R. E. Anderson and
found them similar petrographically to the Peach
Springs. It appears likely, but not certain, that the ash-
flow tuff in the Patsy Mine Volcanics of the northern
Black Mountains of Arizona and Eldorado Mountains
in Nevada is the Peach Springs.

Peach Springs Tuff apparently does not extend west
of Needles into the northern Sacramento Mountains
area. I examined ash-flow tuffs cropping out in the
north-central Sacramento Mountains and they are not
Peach Springs.

The distribution and thickness of the Peach Springs
and other volcanics, and the presence of lava flows
petrographically similar to the Peach Springs in the
southeastern Black Mountains point to that general
area as the probable source (fig. 5). Young and Brennan
(1974, p. 84) suggested a source in the same region. N o
caldera has been recognized, but if one is present, it may
be partly or entirely buried beneath the alluvium of
Sacramento Valley. In the Vidal-Parker region the tuff
is thin and very sporadically preserved, but it is pres-
ent in scattered locations throughout most of the region
(fig. 5; pl. 1). It commonly occurs at or near the top of
the most structurally disturbed section but is locally
faulted on a small scale. At most localities, sedimentary
rocks appear to overlie the Peach Springs with minor
disconformity.

The Peach Springs is nonwelded to moderately welded
in the Vidal-Parker area and is characterized by per-
vasive vapor-phase alteration. However, at localities in
Rice Valley near the probable distal edge, it is non-
welded, mostly vitric, and shardy. Petrographically, the
Peach Springs Tuff of the Vidal-Parker region appears
to be almost identical to the Peach Springs Tuff of the
type area in northwestern Arizona. (See table 3.) Quartz
appears to be rarer in the tuff in the Vidal-Parker
region—quartz is absent in some samples. Plagioclase
is somewhat variable in amount in the Vidal-Parker
samples. However, the large size (1—3 mm) of the
sanidine phenocrysts is characteristic of Peach Springs
Tuff from both areas.

Peach Springs Tuff from a locality near Parker was
dated by K-Ar at 19.21- 0.5 my on biotite and 18.6: 0.4
my on sanidinel (Marvin and Dobson, 1979, p. 10).
Whole-rock ages on basalt directly underlying and over-
lying the tuff at another locality between the Mopah
Range and Whipple Mountains gave ages of 17.4: 0.4
my. and 14.9iO.3 m.y., respectively. Dates reported

1US. Geological Survey K-Ar ages given in this report have been corrected for new
constants.

STRATIGRAPHIC HISTORY 15

TABLE 3.—Petrographic comparison of the phenocrysts of Peach
Springs Tuff of the Vidal-Parker region with those of the type area
in northwestern Arizona

 

Average percent

 

 

 

 

Vidal-Parker regionl NW. Arizona2

Phenocrysts ------------- 5-15 4-14
Sanidine ---------------- 76.0 74. 0
Oligoclase -------------- 16.0 18.9
Quartz ------------------ l. 0 l. 0
Hornblende —————————————— 2. 0 2. 0
Biotite ----------------- l. 5 0. 7
Clinopyroxene ----------- O. 5 0. l
Sphene ------------------ 1. 5 0.8
Opaques ----------------- 2. 0 2. 6

Total -------------- 100.5 100.1

 

1Average of eight samples.

2Young and Brennan, 1974.

by Damon (1964, 1966) on Peach Springs Tuff in the
Kingman region are 16.9:0.4 my. and 18.3:06 my
old. The latter age agrees well with the Peach Springs
dates of 18.8 and 18.2 m.y. obtained near Parker. The
16.9 my. date appears spurious, but this date does fit
the bracket defined by the two basalt ages from the
Vidal-Parker area of 17.0 and 14.5 m.y. Reasons for the
age discrepancies in both areas are not clear, but even
though Young and Brennan (1974) indicated that the
tuff in the Kingman-Peach Springs region is a single
cooling unit, my observations in a very limited recon-
naissance suggest that the Peach Springs is at least a
compound cooling unit, which might help to explain
some of the variation in dates.

The Peach Springs remanent magnetization has been
described by Young and Brennan (1974). The polarity
is normal, declination 32.3 °, and inclination 42.8 °. N o
paleomagnetic study was made of this unit in the Parker
area, but field polarity measurements indicate the tuff
is normally magnetized.

SEDIMENTARY ROCKS

Sedimentary material makes up at least half of the
Tertiary section in most areas of the Vidal-Parker region
(fig. 4). These rocks are characterized by abrupt vertical
and lateral changes in lithology which are difficult to
represent graphically (fig. 4). The coarser clastic
deposits and breccias tend to occur in the lower part
of the Tertiary section. The rocks are briefly described
here in three main groups: breccias; conglomerate, sand-
stone, siltstone, and limestone; and fanglomerate.

 

BRECCIAS

In the eastern and southern Whipple Mountains and
Riverside Mountains, the Tertiary section is locally
made up of wedge-shaped deposits of debris ranging
from megabreccias that commonly resemble basement
rock in place to fine-grained arkosic breccias associated
with sandstone and conglomerate. In some areas the
megabreccias include giant slide blocks of Paleozoic and
Mesozoic(?) sedimentary rocks. The best examples are
about 10 km northwest of Parker (Dickey and others,
1980), where broken but stratigraphically intact masses
of quartzite and overlying limestone lie at the base of
the Tertiary section. The quartzite is identified as the
Esplanade(?) Formation or Queantoweap Sandstone of
McN air (1951); the overlying carbonate rocks are prob-
ably the stratigraphic equivalent of the Kaibab
Limestone. In the Riverside Mountains, the basal Ter-
tiary breccias include predominantly Paleozoic and
Mesozoic(?) rocks apparently derived from nearby out-
crop areas of these rocks.

In most areas these breccias of Paleozoic and
Mesozoic(?) rocks are overlain by coarse and fine
sedimentary breccias and conglomerate almost entirely
derived from granite gneiss of the upper plate. Such
breccias are also commonly intercalated with andesite
lavas and breccia flows, particularly in the Whipple
Mountains.

The most extensive megabreccias of metamorphic
rocks are in the northeastern Whipple Mountains (sec.
A, fig. 4), where more than a thousand feet of gneiss
megabreccia overlies andesite lavas and finer grained
sedimentary rocks. The breccias were shown as Precam-
brian complex on the Needles sheet geologic map
(Bishop, 1963) and were mapped as Precambrian base-
ment complex by Kemnitzer (1937). These giant brec-
cias bear an interesting resemblance to the “Amargosa
chaos” of Noble (1941) and Hunt and Mabey (1966) in
the Death Valley region.

CONGLOMERATE, SANDSTONE, SILTSTONE, AND LIMESTONE

Sedimentary rocks of these lithologies occur
throughout the Tertiary section in most of the region.
They are thin or absent in the western Whipple Moun-
tains, and, if present in the Mopah Range, they are
buried beneath the thick pile of volcanic rocks. In some
areas it is possible to distinguish between sediments laid
down prior to the Peach Springs Tuff and those
deposited later.

Almost all the sedimentary rocks are shades of tan
to brick red. The conglomerates typically consist of
fairly well rounded cobbles of granite gneiss in a matrix
of coarse arkosic sandstone. This material commonly

16 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

grades into fine to coarse sedimentary breccias or sand-
stone. All the sandstones and siltstones tend to be
poorly sorted and the grains are subangular. Colorful
red and pink sandstones are well exposed at several
places in the Colorado River Valley between Parker and
Parker Dam. Brick-red sandstones are common, but in
many areas bleaching results in tan or subdued reds.

Many unconformities are present throughout the Ter-
tiary section, but one of the most persistent uncon-
formities is found in the southern Whipple Mountains
where it separates primarily lavas and breccias below
from sedimentary rocks above. Sediments above the un-
conformity consist of locally more than 300 m of red,
tan, and brown sandstone, limy siltstone and limestone,
much of which is fairly thin bedded. These beds are
generally less disturbed by faulting than the underly-
ing rock and display gentle dips and open folds. These
attitudes commonly steepen near the unconformity,
however, which shows that much of the apparent
folding is due to initial deposition on sloping surfaces.
Surprisingly, little reworking of coarse fragments of
older rocks occurs in these beds; some of the lacustrine
limestones, which are often difficult to distinguish from
limestones of pre-Tertiary age, occur abruptly within
the clastic sequence, or were locally deposited directly
on breccias and lava flows without incorporating any
of these rocks. Temporary blockage of drainage and
quiescent conditions are required to explain these
phenomena. Despite careful searches, no fossils were
found in the sedimentary rocks.

In some areas, such as the southern Whipple Moun-
tains, a still younger sequence of sedimentary rocks can
be mapped on the basis of an unconformity at the
stratigraphic position of the Peach Springs Tuff. Here
occurs an upward change to less well indurated con-
glomerate, and locally, the presence of cobbles of the
Peach Springs. Rocks of this type are poorly exposed
beneath the basaltic lavas on the north slopes of Black
Peak east of Parker. In some areas they cannot be read-
ily distinguished from the fanglomerate of Osborne
Wash, which locally contains detritus, apparently
reworked from these younger conglomeratic beds.
Though they are not common, there is a significant in-
crease above this unconformity in the number of clasts
of gneiss derived from the lower plate of the Whipple
Mountains detachment fault.

FANGLOMERATE OF OSBORNE WASH

A widespread deposit of indurated detritus occurs
between the tilted and faulted Tertiary volcanic and
sedimentary rocks and the overlying Bouse Formation.
In the western part of the Vidal-Parker region, the

 

fanglomerate contains little or no primary volcanic
material, but eastward in the Buckskin Mountains,
mafic lava flows and silicic tuffs are intercalated in it.

Rocks of this general type and age have been de-
scribed from many areas along the Colorado River
drainage from Lake Mead (Muddy Creek Formation,
Longwell, 1963; Anderson and others, 1972) to Needles
(Metzger and Loeltz, 1973), Parker (Metzger, 1965;
Metzger and others, 197 3), and Yuma, where it was ten-
tatively, and probably incorrectly, correlated with part
of the Kinter Formation (Olmsted and others, 1973,
p. H35). Similar clastic deposits are present throughout
much of the Basin and Range province, but they are well
exposed only in tectonically active areas (for example,
the Furnace Creek and Funeral Formations in the Death
Valley area (Noble, 1941; Hunt and Mabey, 1966)).

The fanglomerate is not very thick anywhere in the
region, particularly if basaltic lavas are excluded. Near
Parker, it is probably nowhere more than 500 m thick.

In the Vidal-Parker area the fanglomerate consists
largely of coarse brown to tan intimated colluvium, con-
taining predominantly cobble sized clasts, but locally
containing lenses of sand and boulders. In general, the
unit coarsens toward the mountains. In most exposures,
the deposit is sufficiently indurated to stand in near ver-
tical walls. The clasts are predominantly Tertiary
volcanic and sedimentary rocks, which help to distin-
guish the unit from some Pliocene-Pleistocene alluvium.

A silicic ash bed was found in the fanglomerate north-
west of Parker (1.3 km northeast of the Turk mine,
Parker NW. quadrangle). This ash is believed to be dif-
ferent from tuff beds occurring farther east in the
Buckskin Mountains, and from another ash found about
4 km farther west in what was mapped as a sandy phase
of the Bouse Formation (Dickey and others, 1980). A
comparison of the two ashes is given in table 4. The
samples are generally similar but differ in details.

At first glance these two ashes appear very similar,
but both are slightly contaminated (MWC—24—7 5 more
than MVC—59—75) with fine sand. This could explain
some of the differences, but it is concluded that the two
ash beds are probably different and that they are con-
tained in two stratigraphic units, Bouse Formation and
fanglomerate of Osborne Wash. Another similar ash bed
occurs in the fanglomerate on the north side of the
Whipple Mountains in sec. 6, T. 3 N., R. 25 E.

The fanglomerate of Osborne Wash, as mapped, prob-
ably spans a fairly long interval of time, as suggested
by the dates of included basaltic rocks (table 2) in the
Buckskin Mountains area. Even if some dates are in
error, at least 8 million years are involved. Thus, the
unit must be considered Pliocene and Miocene in age.
The age of the unit is important as its base is easily
recognized as a major unconformity in most areas. Only

STRATIGRAIWiKJHISTORY

17

TABLE 4,—Comparison of ash beds in sand of the Bouse Formation and fanglomerate of Osborne

 

thh
Sample No. ------------- MWC-24-75 MWC-59-75
Location --------------- SEl/4NWl/4 sec. 22 NW1/4NW1/4 sec. 25

Refractive index

of glass.

Heavy minerals
2. 88 sol—«—

Character ------------

Percent

Light fraction

Percent of raw sample
+325 mesh ----------
Percent 2.88 SGl----

Character ------------

T. 2 N., R. 24 E.
Parker NW quad.
Sandy phase of

Bouse Formation.

1.496

4.6

Well rounded to
angular. Biotite
absent, but bleached
biotite in light
fraction; abundant

green hornblende.

34
95.4
Shards relatively

transparent.

T. 2 N., R. 24 E.
Parker NW quad.
Fanglomerate of
Osborne Wash.
Slightly 1.500, but
shards a little more
devitrified than in

sample MWC-24-75.

1.0

Mostly angular
Biotite present;
scarce green

hornblende.

6
99.0
Shards tend to be

iron-stained;

"striated" shards
and bubble walls

more prevalent.

 

1SG = specific gravity, +325 mesh fraction.

a few faults displace the fanglomerate in the Vidal-
Parker region, and with but a few exceptions, they are
short and have less than 3 m of offset. The beds in the
fanglomerate rarely dip over 5 °, but locally near steep
bedrock slopes dips are as much as 35°. Most, if not
all, of this dip is probably initial.

BOUSE FORMATION

The Bouse Formation, named and described by
Metzger (1968), is a fine-grained, light-colored, marine-
to brackish-water deposit of late Miocene and Pliocene

 

age. It was laid down in an estuary that reached up the
present valley of the Colorado River beyond N eedles,
Calif. In addition, deposits lithologically and faunally
(Smith, 1970; Winterer, 1975) similar to the Bouse, and
probably of the same origin, occur throughout the
eastern Mojave Desert at elevations mostly less than
about 1,000 ft (300 m), but in most areas they are buried
by younger alluvium. The Bouse is an excellent strati-
graphic marker, but it is only sporadically exposed in
the Vidal-Parker area. A related tufa plastered on
bedrock and a thin basal white marl are easily identified.
Upslope, the Bouse grades into soft pink siltstone and

18 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

tan sandstone. This lithology is best exposed on the
south flanks of the Whipple Mountains above about
900 ft (275 m); sandy deposits believed to represent con-
temporaneous beach and eolian sands are found to
elevations of about 1,400 ft (425 m) in that area.

The Bouse was not studied in detail, but because of
its importance as a structural datum, it is discussed
later in that context. However, some refinement of
Metzger’s Pliocene age seems warranted. He (Metzger,
1968, p. D133) reported a K-Ar age of 3.02i 1.15 m.y.
obtained on partially vitric ash from a bed near the base
of the Bouse about 50 km southwest of Blythe. A subse-
quent date (Damon and others, 1978) on the same bed
yielded an age of 5.47:0.20 m.y. Porous glasses are
unstable chemically, however, and, where possible, are
avoided in potassium-argon dating. Fritts (in Early Site
Review Report, Sundesert Nuclear Plant, 1976, v. 3, sec.
2.5E, p. 4: San Diego [Calif] Gas and Electric Co.)
pointed out that statements by Smith (1970, p. 1415)
show that the Bouse carmot be older than a foraminifer
which underlies typical Bouse sedimentary rocks near
Yuma. This fossil is regarded as marking the Pliocene-
Miocene boundary (Smith, 1970, p. 1415). Considering
these dates, and often cited (for example, Metzger, 1968,
p. D133; Lucchitta, 1972, p. 1940) relationships between
fluvial gravels and dated basalts at the mouth of the
Grand Canyon (Damon and others, 1978), an age of
about 5 m.y. for the Bouse seems reasonable.

CORRELATION WITH SURROUNDING AREAS

Prior to 1975, most areas of Tertiary rocks adjacent
to the Vidal-Parker region had not been studied in
detail. To the east, in the Artillery Mountains area,
Lasky and Webber (1949) reported Eocene(?) sedimen-
tary rocks and mafic lavas, which they called the Ar-
tillery Formation, overlain by intermediate to silicic
Miocene(?) volcanic rocks, and by Pliocene(?) Chapin
Wash Formation, mostly sedimentary rocks. Basalts of
Quaternary(?) age capped their section. Both the silicic
volcanic rocks and the base of the Chapin Wash For-
mation have been dated as about middle Miocene in age.
(See Otton, 1977.)

Recent work by Suneson and Lucchitta (1979) to the
northeast of the Vidal-Parker region in the Bill
Williams—Rawhide Mountains area identified a strongly
bimodal rhyolite-basaltic sequence correlative with the
younger (post-Peach Springs ’I‘uff) volcanic rocks in the
Parker area. Rocks of the Bill Williams—Rawhide Moun-
tains area gave ages of 151—68 m.y.; they are underlain
by sedimentary rocks, chaotic depositional breccia, and
andesitic flows, one of which gave an age of 16.5 m.y.
(Suneson and Lucchitta, 1979). This age may be a little
too young as the unit is overlain by the Peach Springs

 

Tuff, which is 17—18 m.y. old (this report). An impor-
tant difference in volcanism between the area studied
by Suneson and Lucchitta and most of the Vidal-Parker
region is the increasing abundance to the northeast of
silicic volcanic rocks in the period from about 15-10
m.y. ago. The trachytes and trachyandesites of the
southwestern Buckskin Mountains, described earlier,
were erupted within this period and silicic ash-fall
deposits within the older part of the fanglomerate of
Osborne Wash increase noticeably northeastward from
Parker. It is also notable that the 15—10 m.y. silicic
volcanism in the Bill Williams—Rawhide Mountains area
is almost precisely a time correlative of the more
voluminous rhyolitic volcanism of the Nevada Test Site
region 350 km to the northwest. Interestingly, both of
these silicic volcanic fields lie at the northeast edge of
the Walker Lane—Mojave—Sonoran Belt.

Southeast of the Vidal-Parker area in the Quartzsite
quadrangle, Miller (1970) mapped a sequence of units
of rhyolite, andesite, rhyodacite, and basalt, most of
which are lava flows. He dated one unit, the rhyodacite,
which gave an age of about 20 m.y. (Miller and McKee,
1971). Later work by consultants to San Diego Gas and
Electric Co. dated four more samples of the lavas from
the same general area and obtained ages of 17.4: 0.7,
18.0: 1.0, 19.7i0.9, and 22.4i1.4 m.y. (Early Site
Review Report, Sundesert Nuclear Plant, 1976, Amend-
ment 10, figs. 25-28: San Diego [Calif] Gas and Elec-
tric Co.). The volcanic stratigraphy has not been
completely worked out in the Quartzsite area, but the
dates obtained suggest an age grouping similar to that
of the Vidal-Parker area.

Farther south, in one of the more detailed investiga-
tions of Tertiary rocks in the eastern Mojave Desert,
Crowe (1973; Crowe and others, 1979) mapped the
volcanic rocks of the Picacho area and made recon-
naissance studies of the rocks of the surrounding
southeastern Chocolate Mountains, Calif. He obtained
dates ranging from about 32 m.y. on the oldest rocks
to about 26 and 23 m.y. on an overlying ash-flow tuff
and an andesite lava higher in the section. A basalt,
which forms widespread capping flows, was dated at
about 13 m.y. He identified a tripartite stratigraphic
sequence as generally consisting of a lower unit of basalt
to rhyodacite lavas, a middle unit of rhyodacite to
rhyolite lava and ash flows, and an upper basalt-
andesite group of lavas. He suggested that the latter
group (13—m.y.-old lavas) corresponds to the change to
dominantly basaltic activity, which elsewhere in the
Basin and Range is accompanied by the inception of
basin-and-range faulting (Christiansen and Lipman,
1972). In the Picacho area, however, Crowe (1978 and
written commun., 1977) believes, on the basis of detailed
mapping and lithologic evidence, that basin-and-range

STRATIGRAPHIC HISTORY 19

faulting began earlier, before 26 my. ago. The evidence,
however, is based largely on the appearance low in the
section of coarse clastic deposits, which he believes
could only have been derived from rising fault scarps.

In the central Mojave Desert, Armstrong and Higgins
(1973) pointed out an apparent lack of volcanic rocks
older than 22 m.y., a date that agrees well with the age
of the oldest volcanic rocks in the Vidal-Parker region.

North of the Vidal-Parker region, in the area south-
west of Lake Mead, detailed mapping by Anderson
(1971, 1977), and studies by Anderson, Longwell, Arm-
strong, and Marvin (1972) have documented a sequence
of Tertiary rocks which appear to have an age distribu-
tion and general composition similar to those in the
Vidal-Parker region. There too, the change to predomi-
nant basaltic volcanism occurred around 12—14 m.y.
ago.

The evidence suggests that increasingly older
volcanic rocks are present from the southern Great
Basin southward into the eastern and southern parts
of the Mojave Desert. However, such generalizations
should be made with caution until more work is done
on the Tertiary stratigraphy in the large region between
Lake Mead and Yuma, Ariz.

TERTIARY AND QUATERNARY DEPOSITS

COLORADO RIVER DEPOSITS

Fluvial deposits laid down after retreat of the sea
from the Bouse estuary have been described in various
publications (Metzger and others, 1973; Metzger and
Loeltz, 1973; Lee and Bell, in San Diego Gas and Elec-
tric Co., 1976, v. 3, App. 2.5D). Lucchitta (1972) dis-
cussed the history of the river in the Basin and Range
province. Magnetostratigraphic studies were made by
Kukla (in Early Site Review Report, Sundesert Nuclear
Plant, 1976, v. 3, App. 2.5B: San Diego [Calif.] Gas and
Electric Co.) on river deposits south of Parker. He con-
cluded, on the basis of the remanent magnetization, that
the older Colorado River deposits were probably
deposited in the Gilbert Paleomagnetic Epoch, which
would place them in an approximate age range of
3.4—5.1 m.y. Most of the intermediate age river deposits
he found to be predominantly normally magnetized, and
therefore of probable Brunhes age (<730,000 years).

Fluvial gravels that predate the Bouse Formation had
not been identified prior to this study. The underlying
fanglomerate of Osborne Wash shows no evidence of
through-going streams. Mapping in the vicinity of
Parker (Dickey and others, 1980), however, identified
several small areas of fluvial sediments that underlie
the Bouse. The best exposure is at the west end of the

 

bridge over the Colorado River at Parker. Other un-
mapped small outcrops occur under the Bouse at Head-
gate Rock Dam, 2 km northeast of Parker (pl. 1). The
beds consist of well-sorted pebbles and sand, poorly in-
durated, and locally iron stained. Similar fluvial gravels,
which cannot be proven to underlie the Bouse, occur in
the valley that trends southeastward from near Cienega
Springs (7 km northeast of Parker; pl. 1) toward
Osborne Wash. At one locality about 3 km southeast
of Cienega Springs, indurated well-rounded gravel is
plastered on a stream-fluted outcrop of Paleozoic
limestone.

The probable oldest gravels that are definitely
younger than Bouse occur in a belt from Osborne Wash
near Black Peak southward to east of Mesquite Moun-
tain, and across the La Posa Plain south to Tyson Wash
near the north end of the Dome Rock Mountains (pl.
1). These gravels are commonly heavily coated with
desert varnish and are cemented by caliche. They occur
at a maximum altitude of slightly over 900 ft (275 m)
southeast of Mesquite Mountain and apparently record
an early high-level course of the Colorado River some
distance east of, and about 500 ft (170 In) higher than
its present course. The thick deposit of river sediments
exposed between Mesquite Mountain and Moon Moun-
tain (pl. 1) is probably a deltaic deposit laid down in the
early history of the river.

ALLUVIAL DEPOSITS

Alluvium of the Vidal-Parker region is fairly well ex-
posed, because of incision of drainage related to the Col-
orado River. The relations of alluvial units to the older
rocks and to Colorado River deposits are shown
diagrammatically in figure 6, which is adapted from the
geologic quadrangle map by Dickey, Carr, and Bull
(1980). Details of the alluvium are not discussed here,
but descriptions can be found in the geologic quadrangle
maps and in a report by Southern California Edison Co.
(Information Concerning Site Characteristics, Vidal
Nuclear Generating Station, 1974, v. 3, App. 2.5B).

On plate 1 the alluvium is subdivided into three ma-
jor units, an older, highly dissected fanglomerate-type
alluvium (QTa); alluvium of intermediate (Pleistocene)
age (Qa2), which has varying degrees of soil formation
and characteristically displays a fairly smooth surface
stained by desert varnish; and younger alluvium (Qa1)
that is largely of Holocene age and is related to present
drainages.

AGE OF THE ALLUVIAL UNITS

Because of the importance of the alluvium in
establishing an upper limit to the age of surface faulting

20

NORTH
Foot of Whipple Mountains

Approximately 1 km

 

STRUCTURAL HISTORY, VIDAL—PARKER REGION, CALIFORNIA AND ARIZONA

SOUTH

   

, COLORADO RIVER

 

 

EXPLANATION

 

COLORADO RIVER TERRACE

   

YOUNG ALLUVlUM—Associated in

Holocene {
general with present drainage

  

INTERMEDIATE ALLUVIUM—Deposited
during at least three periods of
aggradation

OLD ALLUVlUM—Dissected fans

 

Pleistocene {

Pleistocene

and ”been" COLORADO RIVER DEPOSITS—(B) and

(D) correspond to units "B" and “D" of
Metzger and others (1973)

 

Corresponds to unit "C" of

 

 

 

 

 

 

 

A BOUSE FORMATION—Tbs, sandy,

Q largely subaerial phase; Tbo, estuarine
C» “c’ deposits

1: 2 8 .......

U, Q) .9. ‘1 u ‘ .:x.

E E) E ijg FLUVlAL GRAVELS

5 mg To FANGLOMERATE OF OSBORNE WASH
C :’ 7X7;

‘° RE»? X‘"\‘>z‘x

B f@$\ BASALTIC ROCKS

o:

N

‘6

E

FIGURE 6.—Relation of Tertiary and Quaternary deposits between the Whipple Mountains and Colorado River in the vicinity of Parker,
Ariz. Units QTa and Qa2 correspond to unit “C," units QTr(B) and QTr(D) correspond to units “B” and “D”. respectively, of Metzger,
Loeltz, and Irelan (1973). Ages shown are K-Ar whole-rock determinations by R. F. Marvin. US. Geological Survey. Ages have been
corrected for new constants. Scale 11/4 in. = approximately 1 km. Large vertical exaggeration. Modified from Dickey, Carr, and Bull (1980).

in the region, a brief discussion of the age of these
deposits is worthwhile. All information obtained to date
indicates a complete absence of faulting in the Vidal-
Parker region in alluvium of intermediate age (unit Qa2)
and younger materials; a few minor faults are present
in deposits as young as the old alluvium (unit QTa).
Consultants for the power companies investigated the
age of the alluvium by several techniques, none of which
provide a wholly satisfactory solution to the problem
of absolute age of relatively young sedimentary
deposits. Kukla reported (p. 19, this report) on the
results of paleomagnetic studies of Colorado River
deposits (QTr) which intertongue in a complex manner,
principally with the old and intermediate age alluvium
(fig. 6). Bull originally described (in Southern Califor-
nia Edison Co., 1974, v. 3, App. 2.5B) the geomor-
phology and characteristics of the alluvium in the Vidal
region, and he estimated ages of the units based on their
similarity in weathering and soil development to
Pliocene-Pleistocene alluvium along the Rio Grande
Valley in New Mexico, pointing out that differences,

 

chiefly in rainfall, in the two areas tend to make his
estimates of age conservative; that is, the estimates in
the Vidal area are probably minimum ages. Ku (in In-
formation Concerning Site Characteristics, Vidal
Nuclear Generating Station, 1975, v. 5, App. 2.5G,
Southern California Edison 00.), reported several ages
obtained by the U-Th disequilibrium dating method on
carbonate in soils developed on the intermediate alluvial
unit (Qa2), and he reported a date on a mammoth tusk
recovered from Colorado River deposits. N 0 consistent
dates were obtained in the first samples; several of the
ages fell well outside the estimates made by Bull. A
second attempt was made to date a specific fan in the
intermediate alluvium (unit Qa2) by digging down
uniform distances from the varnished pebble surface
and carefully scraping caliche off pebbles. This method,
done on samples from two separate fans, gave fairly con-
sistent values that clustered around 80,000 years
(T. Freeman, Woodward-McNeill and Assoc., oral
commun., 1977).

With one exception, work for this report did not

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 21

attempt dating of carbonates. One sample of spring
travertine collected in the NW% sec. 3, T. 2 N ., R. 22
E., east of the Mopah Range (Carr and others, 1980)
gave a U-Th age of 20,000: 6,000 years (J. N. Rosholt,
US. Geological Survey, written commun., 1976). The
large possible error reported was due to the presence
of approximately 37 percent silicate minerals. The soft
travertine that was sampled is directly overlain by a
thin mantle of alluvium belonging to unit Qa2. The
usual varnished surface material of this alluvium con-
tained numerous worked flakes and several arrowheads
which also had varnish coatings. No spring is at this
location now, but the presence of the old artifacts in-
dicates that water was available at the spring that
deposited the travertine at times during the Pleistocene.
Relations at the site suggest, but do not prove, that the
alluvium is younger than all the travertine, but the date
of 20,0001- 6,000 years is in general agreement with ages
of two rat middens (Wells and Berger, 1967) in the near-
by Turtle Mountains dated at about 13,900 and 19,500
years. Both middens contain abundant evidence that
pine woodlands existed in the area at that time. Such
vegetation would have required considerably more
moisture than at present, as would the presence of
springs.

STRUCTURE AND TECTONICS OF THE
VIDAL-PARKER AREA AND
SURROUNDING REGION

GENERAL SETTING

The region discussed here lies in the Basin and Range
physiographic-structural province about halfway be-
tween the San Andreas fault zone and the southwestern
margin of the Colorado Plateau province (pl. 2; fig. 2).
Little structural detafl is known, and the great width
of the alluviated valleys and complexity of the geology
assure no early change in this situation. Plate 2 shows
the general tectonic setting of the Vidal-Parker region
in relation to the eastern Mojave Desert. The predomi-
nant structural grain of the region is northwest trend-
ing, but to the west are the Transverse Ranges
characterized by a series of active east-trending faults
and underlain by areally abundant granitic and meta-
morphic rocks. Tertiary rocks are absent or thin
throughout that area. The Transverse Ranges abruptly
terminate eastward at the Sheep Hole and Coxcomb
Mountains, which mark the west edge of a well-defined
zone of northwestward-trending ranges and valleys
which extends several hundred kilometers from the cen-
tral Mojave Desert southeastward into southwestern

 

Arizona. This structural-topographic trend spreads
westward into the western Mojave Desert north of the
Transverse Ranges, but there it is marked by a number
of northwest-trending active faults. About 150 km to
the southwest of the Vidal-Parker region lies the San
Andreas fault system and the Salton Sea tectonic
depression. Northeast of the Vidal-Parker region is a
persistent northwest-trending lineament—a discontinu-
ity marked by convergent topographic trends and
southward termination of northerly trending ranges and
valleys: in Arizona—the Big Sandy Valley, Hualapai
Valley, Hualapai-Cerbat Mountains, Sacramento
Valley, Black Mountains, Colorado River Valley; and
in Nevada and California—the Dead-Newberry Moun-
tains, Piute-Eldorado Valleys, and the McCulloch
Range. This lineament is one of the most prominent
structural-topographic trends in the southwestern
United States, as pointed out long ago by Hill (1902,
1928) and Ransome (1915), and more recently by Kelley
(1955), Albritton and Smith (1957), and Barosh (1969).

Distribution of rocks (pl. 2) is an important aspect of
the structure of the eastern Mojave Desert. Unmeta-
morphosed or slightly metamorphosed granites
decrease in volume eastward from the Transverse
Range area; along the Colorado River Valley they are
much less abundant, but farther northeast they are a
prominent part of the exposed rocks along the foot of
the Colorado Plateau. Recognizable Paleozoic rocks in
the eastern Mojave Desert are apparently limited to the
Moj ave-Sonoran Belt, although metamorphosed parts
of the Paleozoic section may be present in adjacent
areas. Clastic rocks of Mesozoic and Tertiary age (unit
Czle, pl. 2) of the Livingston Hills Formation type ap-
pear to be present chiefly in a zone paralleling and
southwest of the edge of the Mojave-Sonoran Belt.
Sedimentary rocks of Mesozoic age, and possibly
younger, are probably present in the belt, but they are
apparently much thinner within the belt and lack the
thick conglomerates of the Livingston Hills type se-
quence. This abrupt southwestward thickening and
coarsening of the Mesozoic rocks also occurs across the
Texas lineament in southwestern Texas (Albritton and
Smith, 1957).

At first glance Tertiary rocks seem to be rather widely
and uniformly distributed throughout the eastern
Mojave region (pl. 2). However, closer inspection reveals
that thicker volcanic rocks occur near major centers,
particularly for silicic extrusive rocks, located in the
Kofa, Castle Dome, and Chocolate Mountains of
Arizona, in the southern Black Mountains, Ariz., and
in the mountains 15—40 km northwest of Goffs, Calif.
In all these areas there are thick sequences of rhyodacite
and rhyolite lava flows, together with ash-flow and air-
fall tuffs. In addition, a major basaltic eruptive center

22 STRUCTURAL HISTORY, VIDAL—PARKER REGION . CALIFORNIA AND ARIZONA

occurs in the Mohon Mountains area at the edge of the
Colorado Plateau. Very little has been published about
these centers so that details of their eruptive history
are largely unknown. Smaller centers, largely rhyo-
dacitic, are scattered about the region from the
Eldorado Mountains of Nevada (Anderson, 1977) to the
Mopah Range, Calif. (Carr and others, 1980) and to the
Picacho area of California (Crowe and others, 1979)
35 km north of Yuma, Ariz. In most other areas in the
eastern Mojave Desert, volcanic rocks are of lesser
volume and are highly diluted with sedimentary
materials. These sedimentary rocks are commonly com-
posed of coarse detritus of Miocene and Pliocene age.

GEOPHYSICS

As more information becomes available, the role of
geophysics is increasingly important in understanding
the tectonic history of the eastern Mojave Desert. The
metamorphism, complexity of the geology, and the
presence of broad areas covered by alluvium, make the
need for geophysical studies in this region especially
critical. Fortunately, work in recent years has con-
tributed much new geophysical information. In this
report, work in the fields of seismology, gravity, and
aeromagnetics will be briefly discussed and attempts
will be made to relate some of this data to geology and
structure.

SEISMOLOGY

At the inception of the geologic studies in the Vidal-
Parker region, it was recognized that documentation
was needed to confirm the suspected aseismic character
of the eastern Mojave Desert. As a result, the US.
Geological Survey, on behalf of the Nuclear Regulatory
Commission, from 1974 to 1977 operated a seismic net
in the Mojave Desert as far east as Parker, Ariz. Sta-
tion locations are shown in figure 7. A similar, dense
network of stations has operated in the much more
seismically active area to the west of long 116° W.

According to Gary Fuis (written commun., 1976,
197 7 ) of the US. Geological Survey, then at the
Seismological Laboratory at the California Institute of
Technology, more than 2 years of monitoring recorded
only a very few small earthquakes in the area east of
the aseismic area boundary shown on plate 2. Two small
events of about magnitude 1 were recorded near lat 34 °
N., long 115° W. in May 1976, and one of magnitude
1.2 at approximately lat 34 °45' N ., long 115°05’ W. in
October 1974. A few other events recorded are probably
explosions judging from location and signal character.
The current extremely low level of seismicity in the

 

 

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EXPLANATION
A USGS Station

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Trough at base of crust showing dip and plunge

Western boundary of Eastern Mojave aseismic area

FIGURE 7.—Seismic stations in the eastern Mojave Desert, 1974-77.

eastern Mojave Desert confirms earlier records made
from more distant stations back to the 1930’s (Hileman
and others, 1973) that show the area to be essentially
aseismic. During the same recording period and earlier,
the western Mojave Desert, in contrast, has been seis-
mically very active.

The Mojave Desert has been considered to be a
somewhat anomalous part of the Basin and Range prov-
ince with an upper mantle velocity generally in excess
of 8 km/s (Prodehl, 1970; Stuart and others, 1964) and
a crustal thickness less than about 30 km.

Using explosions, Gary Fuis (written commun., 1976)
has examined travel times and depths to the base of the
crust in southeastern California. He tentatively con-
cluded that the crustal thickness varies from about
33 km near Barstow to around 20 km in the Imperial
Valley. In the area along the Colorado River, crustal

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 23

thickness was estimated to be about 26 km. The shape
of the Mohorovicic discontinuity (base of crust) obtained
by contouring depths suggests an asymmetric trough
plunging northwest along an axis lying about halfway
between Blythe and the Salton Sea (fig. 7). Refraction
profiles suggest a dip of about 3 ° SW. on the northeast
flank of the trough. The southwest side of the trough
appears to be steeper. On a refraction profile from
Corona, Calif., to Parker, Ariz., Gary Fuis (written
commun., 1976) noted a bend in the P" branch of the
traveltime curve in the vicinity of the Little Maria
Mountains seismic station, with a slightly lower veloci-
ty, about 8.0 km/s, farther east in the vicinity of Parker,
Ariz. Thus, the Vidal-Parker region probably lies just
northeast of a northwest-trending change in the upper
mantle velocity and is underlain by a crustal thickness
of about 26—27 km. To the west the “aseismic bound-
ary” crosses the crustal thickness trend lines at a fairly
small angle.

MAGNETICS

High-level aeromagnetic maps of the eastern Mojave
Desert are available for Arizona at a scale of 1:1,000,000
(Sauck and Sumner, 1971) and for California east of long
116 ° W. and north of lat 33 °30' N. at a scale of 1:250,000
(US. Geological Survey, 1975). In addition, a ground
magnetic map of the area between Blythe and Desert
Center, Calif., was made by Rotstein (1974). For this
report, aeromagnetic measurements of the region are
compiled on plate 3. A low-level aeromagnetic map
issued by the US. Geological Survey (1981) of the
Needles 2° sheet was not available at the time of the
compilation, but the new map provides some useful sup-
plementary data for the Vidal-Parker region.

Most of the Vidal-Parker region is characterized
magnetically by diffuse anomalies of variable orienta-
tion and relatively low amplitude. Exceptions include
areas of granitic rocks that produce two strong positive
anomalies, one between the Sacramento and
Chemehuevi Mountains, the other over the western
Turtle Mountains. Weaker positive anomalies are pres-
ent over the northwestern Whipple and western and
eastern Buckskin Mountains. Striking anomaly trends
are present both northeast and southwest of the Vidal-
Parker region; both are closely related to strongly
magnetic granitic plutonic rocks (pls. 2 and 3). In
general, the 100-km-wide belt between these two areas
of strong anomalies is magnetically weak, possessing
no more than a ZOO-gamma relief on either side of the
O—gamma contour. At the flight heights of about
8,000—11,000 ft, important structural details and
volcanic rocks in most of the region on plate 3 do not
produce significant anomalies; several exceptions are

 

worth noting: (1) At the north edge of the map area (at
about long 115 °15' W.), a strong negative anomaly is
present that coincides nicely with a gravity negative
anomaly suggested by Healey (1973) as due to a caldera
structure. Presumably, the caldera is filled with a thick
section of reversely magnetized lavas and ash-flow tuff.
(2) In the northeast corner of the map area, strong
positive anomalies are associated with the Mohon
Mountains volcanic center. (3) To the south, in Arizona,
volcanic rocks are at least partly responsible for
moderate anomalies in the Kofa, Little Horn, and
southern Plomosa Mountains area.

Despite the local diversity of trends, the regional
weak-anomaly magnetic belt has a distinct northwest
trend, as do many of the anomalies within it, reflecting
the important northwest-trending structural grain of
the region. Significantly, this trend is lacking northeast
of a line trending N. 55° W. from about lat 34 °00’ N .,
long 113°00' W. to lat 35 °00’ N., long 114°45' W. This
same geophysical trend continues both northwest
beyond the edge of the map area, closely following the
California-Nevada border, and southeast through
Arizona toward and beyond Phoenix. This change in
magnetic character coincides well with the northeast
edge of the MojaveSonoran Belt.

The aeromagnetic map also shows other large
features of structural significance. In Arizona, the
northeast-trending Buckskin, Harcuvar, Harquahala,
and Big Horn Mountains all have similar positive
magnetic anomalies, but the trend of the group of
anomalies is distinctly northwest; the lower gamma
levels between ranges probably are due partly to greater
distance of the bedrock from the flight level.

Likewise, in California, in the area at the east end of
the Transverse Ranges (Pinto-Eagle Mountains) there
is very little indication of the prominent east-west struc-
ture, but instead, a strong N. 60° W. magnetic trend.
This same distinct trend, but with weaker anomalies,
persists as far northeast as Cadiz Valley, and as far east
as the Granite, Little Maria, and Big Maria Mountains.
This northeast limit to the pattern of prominent north-
west magnetic trends, largely unaffected by the trends
of the Transverse Ranges, marks the southwest edge
of the Mojave-Sonoran Belt (pls. 2 and 3). The lack of
expression in the magnetics of the east-west trend of
the eastern Transverse Ranges is compatible with the
crosscutting nature and general youthfuhless of these
structures.

Another feature of note is the relatively flat, distinctly
negative magnetic gradient associated with the
Mesozoic-Tertiary sedimentary rocks of the Livingston
Hills Formation type. This gradient is evident in a zone
extending southeastward from the south end of the Cox-
comb Mountains through the Palen, McCoy, and Dome

24 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

Rock Mountains to the southern Plomosa Mountains
(pl. 3). Other areas of rocks (pl. 2) probably correlative
with the Livingston Hills Formation in southwestern
Arizona are likewise marked by low-amplitude negative
anomalies, as, for example, parts of the Castle Dome
and Middle Mountains. This magnetic signature re-
flects the thick, relatively nonmagnetic character of
these sedimentary rocks and the probable absence
of extensive granitic rocks beneath them. However,
the same magnetic trend continues northwestward
beyond outcrop areas of the Livingston Hills type
rocks, which suggests that deeper, more fundamental
factors are responsible, such as the subcrustal
northwest-trending boundary mentioned in the section
on seismology.

The US. Geological Survey (1981) aeromagnetic map
of the Needles 2 ° sheet was flown at 1,000 ft above ter-
rain and provides a much more detailed view of the
magnetic characteristics of the rocks in the Vidal-Parker
region. Volcanic rocks in two main areas, the Mopah
Range and western Buckskin Mountains, exhibit
typical high-amplitude small anomalies. In the Mopah
Range the anomalies are nearly all elongated in a north-
westerly direction, but in the Buckskin Mountains
trends are much less consistent. These trends reflect the
strong northwest structural grain caused by faulting
in the Mopah Range area, and general lack of such
faulting in the Buckskin Mountains. Both northwest
and northeast trends are visible on the low-level Needles
sheet; however, many areas, such as the Chemehuevi
and Whipple Mountains, fail to show prominent trends
associated with Tertiary rocks in the upper plate of the
Whipple Mountains detachment fault. This is perhaps
another indication of the “thin-skin” and highly
dismembered nature of the upper plate rocks, which
tend to be weakly magnetic in much of the area, despite
their high content of granitic material. One particular-
ly obvious regional magnetic lineament is shown by the
low-level map: a persistent gradient and discontinuity
trends about N. 60 ° E. and extends about 75 km from
the Turtle Mountains on the southwest to the Mohave
Mountains on the northeast (pl. 2). The linearity and
great length of this discontinuity in the magnetic con-
tours indicate a prominent fault zone probably occupies
this position. It lies just outside the geologically
mapped area on plate 1, and much of it is buried beneath
alluvium in Chemehuevi Valley. The trend and position
of this feature is very close to that shown farther south-
east by the northeast-trending parts of the Buckskin,
Harcuvar, and Harquahala Mountains (pl. 2). Similar
northeast structure trends are present in the Old
Woman Mountains to the northwest of the Vidal-Parker
area. The significance of these observations will be
discussed later in this report.

 

GRAVITY

A gravity map of the eastern Mojave Desert region
has been compiled for this report (pl. 2). Like the
aeromagnetic map (pl. 3), the Vidal-Parker region shown
on plate 2 also shows small gravity anomalies that
generally have nonlinear low gradients, except for a
relatively steep linear gradient that parallels the belt
margin on the northeast. Gravity does not appear to
define the southwest margin of the belt as well as
seismic information or aeromagnetic data, although far-
ther southwest, the Salton trough and San Andreas
fault zone are marked by a prominent northwest-
trending gravity high. With the principal exception of
the Salton trough, the gravity anomalies fit the present
topography and bedrock quite well—the gravity highs
are over the mountains, the lows over the basins. In this
regard, a good correlation appears to exist between the
gravity highs and areas of metamorphic rocks in
general, particularly the lower plate of the Whipple
Mountains detachment fault. Notably, there are only
a few steep linear gradients like those that characterize
deep structurally active valleys elsewhere in the Basin
and Range province.

Several linear gravity gradients suggestive of faulting
or correlative with known faults should be pointed out.
In the vicinity of Needles, a strong linear gravity gra-
dient trends northwest and is paralleled at the surface
by fault scarps in Quaternary alluvium. These faults
were called the Needles graben (Information Concem-
ing Site Characteristics, Vidal Nuclear Generating Sta-
tion, 1975, v. 2, p. 2.5-141 and Amendment 6, p. 25-141,
Southern California Edison Co.). Along Bouse Wash on
the northeast side of Mesquite Mountain is a 20-km-
long northwest-trending steep gravity gradient suggest-
ive of faulting; a small fault in the Bouse Formation has
been observed here (pls. 1, 4), but no younger beds are
known to be faulted. A similar linear gravity gradient,
but trending northeast, is present on the northwest side
of the Mule Mountains about 25 km southwest of.
Blythe, Calif. There, also, no faulting is observed in
Quaternary deposits, but the steepness of the gradient
indicates a density contrast that is probably due to a
steep contact between the metamorphic bedrock and
buried Bouse Formation or Colorado River deposits.
This contact could represent a fault scarp against which
the lower density Bouse or the river deposits were ac-
cumulated; they may or may not be involved in the
faulting.

About 20 km north of Blythe is another feature, the
Blythe graben (Information Concerning Site Character-
istics, Vidal Nuclear Generating Station, 1975, v. 2,
p. 25-141, Southern California Edison Co.) that is
similar in some ways to the Needles graben. Several

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 25

scarps in alluvium, probably alluvium of intermediate
age (Qa2), are present along the northeast side of the
northwest-trending gravity-defined trough that lies be-
tween the McCoy and Big Maria Mountains. This
trough is about 40 km long and is one of the best de-
fined valleys filled with low-density material in the
region. The feature is important to the interpretation
of the structural geology, not only because it has
associated Quaternary faulting, but also because it lies
near the southwestern margin of the tectonic belt de-
fined by other geophysical and geologic data.

A major gravity feature of importance is the regional
high that extends up the Colorado River Valley from
the Imperial Valley northward to the Lake Mohave
area, 50 km southeast of Las Vegas, Nev. On first ex-
amination it would appear that this high could be en-
tirely a result of topography (pls. 2, 5), and, indeed, a
fairly consistent general relation exists between eleva-
tion and gravity—the 1,000-ft elevation contour roughly
approximates the 50 mgal gravity contour, and the
2,000-ft contour, the 75 mgal contour. However, the
regional geologic map shows that the distribution of
relatively unmetamorphosed granitic rocks follows the
same general pattern; that is, granites are volumetrical-
ly more abundant in the western and northwestern
parts of the map area than they are along the Colorado
River Valley at elevations below 2,000 ft or so. This rela-
tionship suggests that isostatic compensation may have
influenced the course of the Colorado River, localizing
it in an area of slight sagging due to slightly heavier
crust, and that the general match between gravity and
topography is only partly the result of stripping of
bedrock from the valley.

The gravity map (pl. 2) suggests other significant rela-
tionships in the Vidal-Parker region. A closed gravity
high, highest in the Vidal-Parker region, coincides with
the Riverside Mountains and extends across the Colo-
rado River Valley to include the Mesquite Mountain
area, which suggests that the rocks making up the lower
plate of the Whipple Mountains detachment fault in the
Riverside Mountains extend across to Mesquite Moun-
tain. However, as exposures of metamorphic rock on
Mesquite Mountain include no Paleozoic carbonate
rocks like the Riverside Mountains, it seems likely that
the carbonate rocks are present at depth beneath Mes-
quite Mountain. Although a more or less continuous
gravity high encompasses the Big Maria and Riverside
Mountains and Mesquite Mountain, each area has a
separate, closed anomaly, and a suggestion of a right-
lateral offset of the Mesquite Mountain—Riverside
Mountains gravity highs occurs along a northwest-
trending fault zone that may extend from the Mopah
Range southeastward to the Plomosa Mountains
(pl. 4).

 

One of the more prominent gravity lows in the Vidal-
Parker region lies along the northeast flank of the
Mopah Range. A small closed low, partly over alluvium,
is present in this area in a location which suggests that
it may mark the main eruptive center for the rhyodacitic
lavas, tuffs, and breccias of the Mopah Range. Several
plug domes similar to adjacent lavas are exposed a short
distance southwest of this low.

LEVEL LINE
By D. D. DICKEY

In 1930—32, the Metropolitan Water District of
Southern California completed a line of first-order level-
ing extending along the route of the Colorado River
aqueduct from the Colorado River near Parker, Ariz.,
to Los Angeles, Calif. In the fall of 1975, about 20 miles
of this line was releveled by the Metropolitan Water
District under a contract with the US. Geological
Survey. The releveled segment was between the west
portal of the Whipple Mountain tunnel westward to a
point about 1.5 miles west of Vidal Junction, Calif. (fig.
8). Eighteen of the original 19 stations in this interval
were recovered. All stations in the 1975 survey were
found to be slightly positive with respect to an arbitrari-
ly chosen zero point at the east end of the level line. The
unadjusted measurements, bench to bench, were com-
pared for the two surveys (fig. 8). First-order closure for
the line permits a difference of 24 mm in elevation over
the length of the survey. One station had a change ex-
ceeding this amount, +54 mm at bench mark 966, (Sta.
20X), 11/2 miles northeast of Vidal Junction. The three
bench marks to the west of bench mark 966 had
measured differences of +21 mm and the next two east
of it had measured differences of +23 and +24 mm. All
these bench marks were inspected on the ground and
were apparently undisturbed.

The reason for the anomalous elevation change of
bench mark 966 is not known. As the anomalous sta-
tion was elevated, subsidence apparently may be elim-
inated as an explanation. Possible explanations include
surveying error in the original survey, uplift due to
geologic structure, and uplift due to expanding clays
in the Bouse Formation beneath the bench mark, which
is located about 200 ft from the aqueduct and slightly
downslope from it. The area immediately surrounding
the bench mark was examined for youthful geologic
structures, but none were found. It should be noted,
however, that bench mark 966 is located in a general
zone of buried northwest-trending faults (pls. 2, 4) and
is above the upthrown side of one of them. Thus,
preliminary evaluation of the releveling data indicates

26

STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

 

 

 

   

   

   

   
 

  
 
    
   

 

  
 
  
   

 

 

 

 

 

 

 

 

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5 E 20 20
I: j 0 , o
'1— 20U 20V 20W 20X 20Y 202 21A 21B 21C 21D 21E 21F 21G 21J 21L 21M 21N
> 2
Lu 21 H 21 K
_I
Lu

FIGURE 8.—Map and profile along part of the Colorado River aqueduct showing elevation differences between surveys in 1931 and 1975.
Station 21N held constant. Station 21D not recovered in 1975. Surveyed by Metropolitan Water District of Southern California. Arrows
on inferred fault zone show direction of movement; bar and ball on downthrown side.

changes that are within the allowable survey error, with
the exception of bench mark 966, whose anomalous posi-
tion is probably not related to structural movements,
but this cannot be proven with existing data.

The series of first-order bench marks along the aque-
duct, together with a trilateration net also surveyed by
the Metropolitan Water District in the 1930’s, offers
an opportunity to pursue geodetic measurements,
should reactor siting interest in the area be revived.

STRUCTURES IN PRE-TERTIARY ROCKS

Although structures in rocks older than Tertiary were
not mapped in detail in most parts of the Vidal-Parker
region, some important information was gained and is
summarized here.

As few places exist in the area where the older Ter-
tiary rocks are in originaldepositional contact with un-
disturbed basement rocks, determination of the age of
certain faults and other features is difficult. In addition,
the difficulty is compounded by juxtaposition of
basement rocks in two plates by middle Tertiary detach-
ment faulting. Considering the episode of extension
and dismemberment that accompanied this event, it
would seem reasonable to assume that pre-Tertiary
rocks, largely metamorphosed, would everywhere be
structurally complex. However, in some parts of the

 

Vidal-Parker region at least, this does not appear to be
the case. In the eastern Whipple Mountains, for exam-
ple, are large areas of nearly total exposure of mylonitic
lower plate metamorphic rocks (pl. 1). Reconnaissance
indicates that in much of this area these lower plate
rocks were not highly faulted and were not tightly
folded after mylonitization. Dips of the foliation rarely
exceed 25° and in most places are monotonously con-
sistent. Terry (1972, p. 62) described the Whipple Moun-
tains as an eroded dome elongated in a northeast
direction. Direction of dip is generally radial to the
center of the higher eastern part of the mountains. The
western one-third of the lower plate rocks in the
Whipple Mountains is somewhat more structurally com-
plex, however. A series of northwest-striking, probably
high-angle faults separates the western area from the
less disturbed rocks to the east. In addition, locally
numerous dikes and sills of dioritic rocks invade the
metamorphic country rock; attitudes of these intrusive
bodies are highly variable. Westward toward the Mopah
Range, structural disturbance of the metamorphic rocks
appears to increase, and granitic rocks of probable pre-
Tertiary age are separated by low-angle faults from
dike-riddled metamorphic rocks. Reasons for the
westward-increasing structural complexity in pre—
Tertiary rocks of the Whipple Mountains are unknown.
It seems likely, however, that two major regional fault
zones may be partly responsible: one located through

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 27

the narrow west-central part of the Whipple Mountains
(Chambers Well fault zone), the other between the
Whipple Mountains and Mopah Range (Vidal Valley
fault zone; pls. 1, 4). The northwest-trending part of
Chemehuevi Valley and the postulated Tertiary volcanic
center, suggested by gravity and aeromagnetic
anomalies, may be located along these fault systems.
A prominent northwest-trending fault in the Mopah
Range mapped by Carr, Dickey, and Quinlivan (1980)
shows good evidence of right-lateral strikeslip displace-
ment. To the southeast, 3 parallel major fault has been
mapped through the Tertiary rocks, and it may connect
across the Colorado River Valley with the fault that is
suggested by a gravity gradient at the northeast side
of Mesquite Mountain. Thus, faulting in the metamor-
phic rocks in the western Whipple Mountains appears
responsible for localizing some major Tertiary structure.

The Mesquite Mountain area (pl. 2) south of Parker
appears to be a fairly simple north-striking westward-
dipping monocline in the metamorphic rocks, but if, as
suggested under the section on gravity, it represents
a section similar to part of that in the Riverside Moun-
tains, structural complexity must intervene in the area
separating the two sections.

Another important fault zone of probable pre-Tertiary
age appears to be located along the Lake Havasu—
Colorado River course. It also trends northwest, and at
least one branch extends southeastward up the Bill
Williams River Valley. A little farther to the northeast,
still another important subparallel fault crosses the Bill
Williams River at a small angle and trends southeast-
ward about 40 km to the vicinity of Midway, Ariz.
(pl. 2).

The Riverside Mountains are the most structurally
complex of the ranges in the Vidal-Parker area (Carr and
Dickey, 1980). The northern Riverside Mountains ap-
pear to be essentially a faulted monocline or anticlinal
limb dipping northwest and striking northeast. In the
southeastern part of the range the strike swings gradu-
ally to a northwest direction (Hamilton, 1964). Upper
Paleozoic rocks in the eastern part are separated from
underlying, probable Precambrian rocks by a persistent
thrust fault that dips gently westward in most places.
Complicated faulting within the Paleozoic rocks is not
well understood, but the principal style is that of reverse
faults dipping westward at slightly steeper angles
(40 °—50 °) than the bedding, resulting in several repeti-
tions of the section. Interspersed with the reverse faults
are several low-angle normal faults dipping about as
steeply as the bedding. One of the main reverse faults
flattens eastward to become a thrust fault. Probably
many low-angle faults are present in addition to those
mapped. Although reverse and drag folding occurs on
some of the faults, only minor appressed folding and

 

no overturned folding was observed, at least in the
northern Riverside Mountains.

Origin of the structure in the lower plate rocks of the
Riverside Mountains is unknown. The northeast struc-
tural trend is counter to the persistent northwesterly
regional direction so widely developed in rocks of the
upper plate of the Whipple Mountains detachment
fault. It is possible the observed features are partly
related to forceful emplacement of the granitic intrusive
in the West Riverside Mountains. An alternative ex-
planation is that the structure in the Riverside Moun-
tains is a result of compression and drag folding along
major strike-slip faults passing between the Riverside
and Big Maria Mountains. If so, the direction of drag
would seem to fit left- rather than right-lateral faulting.
Right-lateral strike-slip faulting was suggested by
Hamilton and Myers (1966, p. 530—531) to be an exten-
sion of the Death Valley fault zone into the eastern
Mojave Desert. Faulting with northwest trend and a
component of right-lateral strike-slip displacement is
probably present between the Riverside Mountains and
Mesquite Mountain (See “Gravity,” p. 25). This zone
of faulting may be similar to that described by Miller
and McKee (1971, p. 720—721) in the southern Plomosa
Mountains, where Miller (1970) mapped thrust faults
cut by younger strike-slip faulting that offsets Tertiary
volcanic rocks. An area of deformed Paleozoic rocks in
the Plomosa Mountains is described by Miller and
McKee (1971, p. 718) as being unquestionably corre-,
lative with deformed Paleozoic rocks mapped by W. B.
Hamilton in the Big Maria Mountains. I agree that the
rocks are similar, but suggest that, on the basis of a
very similar style of faulting and lithology, the de-
formed Plomosa Mountains section of Miller is more like
the upper Paleozoic section in the Riverside Mountains.
Both sections lie beneath major thrust systems, but
they are different in that Miller has good evidence that
at least some of the thrusting in his area is older than
a 20-m.y.-old rhyodacite lava; whereas, in the Riverside
Mountains and elsewhere in the Vidal-Parker region,
some thrust or detachment-type faulting continued well
into the Miocene (to at least as late as about 14 my
ago). In both deformed sections in the Riverside and
Plomosa Mountains, bedding and fault planes are sub-
parallel, and one is never quite sure whether individual
parts of the section have been thickened or attenuated.
As stated previously, in most places in the Riverside
Mountains the reverse faults dip a little steeper than
the beds, resulting in repetition of the section. This also
seems to be the case in the deformed Plomosa Moun-
tains section, but in both areas faults that omit parts
of the section are also present, and it is not always possi-
ble to determine whether these are normal (hanging wall
down) faults or reverse faults dipping at angles less

28 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

steep than the bedding. In the Riverside Mountains,
however, I believe that most of the faults are reverse
(hanging wall up) and that the repetition or attenuation
is due to varying relationships between the dip of the
fault planes and bedding. No isoclinal folding appears
to be developed in the northern and central Riverside
Mountains, but Hamilton (1964) mapped fairly numer-
ous folds of this type in the southern Riverside Moun-
tains and Big Maria Mountains.

Hamilton (1971) described the Paleozoic rocks in
southeastern California as occurring mostly as “iso-
clinal synclinal keels in polymetamorphic plutonic base-
ment rocks.” Such a configuration requires overturning
of parts of the section; I found no evidence for large-
scale overturning in the northern Riverside Mountains.
I believe the basic style of pre-Tertiary structure, within
the Mojave-Sonoran belt, at least, is that of repetition
of sections by semiconcordant (with bedding) reverse
faulting, with only local appressed folding, plastic defor-
mation, or attenuation on near bedding-plane faults. It
is believed that strike-slip faulting at this stage may
have begun as a series of tear faults in major thrust
sheets whose roots are represented by reverse faults,
such as those found in the Riverside Mountains.

Whereas the northwest-trending extensional struc-
tural grain developed in mid-Tertiary time is the most
obvious structural feature of the terrain in the Vidal-
Parker region, it should be remembered that the older
rocks display evidence of largescale structures oriented
northeast-southwest. Basically, this trend in the pre-
Tertiary rocks appears to be a series of large northeast-
trending synclines and anticlines or “welts” displayed
largely in the cores or lower plate rocks of the Whipple
Mountains detachment fault (fig. 9). These features are
evident in the geophysics (pls. 2, 3), topography (pl. 5),
and local structural trends as seen in the Riverside and
western Buckskin Mountains (pl. 4). As pointed out
earlier, geophysical trends show evidence of northeast
trends. One such geophysical lineament (pl. 2), shown
best by the low-level aeromagnetic map (US. Geological

 

Survey, 1981), is probably a fault zone, but the extent
of its involvement with Tertiary rocks has not been
determined.

TERTIARY STRUCTURES

Several authors have referred the cores of the Whipple
Mountains and some adjacent ranges to a tectonic style
termed “metamorphic core complex” (Davis and Coney,
1979; Shackelford, 1980). The exact timing, cause, and
interrelationship of events in this process remain to be
determined. In the Vidal-Parker region, stratigraphic.
isotopic, and structural information point rather clearly
to a Tertiary, probably middle-Tertiary, age for the prin-
cipal development of the gneissic mylonitic range cores.

A number of aspects of Tertiary tectonics in the Vidal-
Parker region are striking: (1) semicircular or northeast-
erly elongated uplifts exposing range cores with
well-developed mylonitic carapaces; (2) a low-angle
regional detachment surface separating the underlying
range cores from highly extended, less metamorphosed
crystalline rocks of Paleozoic and Mesozoic age, and
unmetamorphosed volcanic and sedimentary rocks of
Miocene age; (3) a regionally persistent, almost per-
vasive, northwest-trending structural grain in the rocks
above the detachment surface; (4) abrupt truncation of
the highly deformed rocks by essentially undeformed
fanglomerates and volcanic rocks of late Miocene and
Pliocene age; and (5) an obvious lack of deep structural
basins typical of the Great Basin and other parts of the
Basin and Range province.

Working out details of the structure in Tertiary rocks
of the eastern Mojave Desert region is difficult because
of the abruptly changing stratigraphy and the scarcity
of recognizable marker beds. Fortunately, a distinctive
unit, the Peach Springs 'I‘uff, is found at scattered loca-
tions and provides a partial key to correlation of major
unconformities and episodes of faulting frOm one range
to the next.

 

WHIPPLE MOUNTAINS

 

FEET

 

| l
2 4

 

0—7.0

 

4000
2000
0
2000
4 6 MILES
| |
|
6 KILOMETERS

 

FIGURE 9.——Section through the eastern Whipple Mountains showing configuration of the Whipple Mountains detachment fault. Location
of section shown on plate 1. Alluvium omitted. Tbo, Bouse Formation (late Miocene and Pliocene); To, fanglomerate of Osborne Wash
(Miocene); Tu, Tertiary rocks. upper part (Miocene); Ts, sedimentary rocks (Miocene); Ta, andesite and granitic breccias (Miocene); Tud,
Tertiary rocks, undivided (Miocene); Tbr, breccia (Miocene); Kgg, gneissic granite (Cretaceous); upg, upper plate granite gneiss (Mesozoic,
Paleozoic, and older(?)); lpg, lower plate gneiss (Mesozoic(?) and older). Heavy lines, faults; arrows show direction of movement.

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 29

STRATIGRAPHIC-STRUCTURAL RECORD

The Tertiary stratigraphic section, though variable
in detail, records some general episodes that provide
clues to the structural development of the area. In the
eastern Whipple Mountains and Riverside Mountains,
the lower part of the section, as described earlier,
contains much very coarse breccia and poorly sorted
conglomerate interspersed with andesitic lava flows
(secs. A, C, E, fig. 4). These breccias consist in large part
of clasts whose derivation is recognizable. They have
not been precisely dated, but some must be as young
as 20 m.y., as they intertongue locally with andesites
of that age. Clearly, these breccia deposits came from
nearby topographically steep slopes if they traveled by
conventional sliding downslope. However, other
evidence of nearby steep slopes is not abundant; the
breccias lie depositionally on a surface developed across
the gneiss, which, prior to extensional faulting, ap-
parently had little relief. In the Whipple Mountains, the
breccias apparently contain no rocks derived from the
now-exposed core or lower plate, but, in the Riverside
Mountains, rocks from both the upper and lower plates
are found, indicating that in the latter area denudation
of the lower plate rocks had begun. Similar breccias are
reported by Shackelford (1980) and Lucchitta and
Suneson (1977b) in the Rawhide Mountains area. In the
Buckskin and western Whipple Mountains and outside
the Vidal-Parker region in the Chemehuevi and
Sacramento Mountains, reconnaissance indicates brec-
cias are locally present but less common. Despite the
now pervasive northwest structural grain in the region,
there is a strong suggestion that considerably less
lithologic change takes place in the Tertiary rocks in
a northeast to southwest direction than in a northwest
to southeast direction. Stated another way, lithologic
similarities appear much stronger athwart the present
structural grain in a direction parallel to that of later
extension. For example, Tertiary rocks in the Riverside
Mountains are generally similar to those in the Buck-
skin and eastern Whipple Mountains, but volcanic rocks
of the Mopah Range are most like those found in the
outlying hills in eastern Chemehuevi Valley. Supporting
this conclusion is the strong northeast-southwest
regional trend of the distribution of the Peach Springs
Tuff (fig. 5). To the east, where a series of ranges, par-
ticularly the Harquahala, Harcuvar, and southeastern
Buckskin Mountains, also have a conspicuous northeast
trend (pl. 2), very few Tertiary rocks are exposed in the
intervening valleys.

It appears possible that the coarse clastics of the
lower Tertiary section were derived from northeast-
trending uplifts or “welts”; the axis of one such uplift
may have extended from the West Riverside Mountains

 

northeastward through the Buckskin and Rawhide
Mountains. This ancestral northeastward trend in the
topography would have influenced Miocene depositional
patterns throughout the region.

Numerous unconformities exist within the lower part
of the Tertiary section, but these are mostly local
changes in depositional conditions and have not been
interpreted as regionally meaningful. One impressive
unconformity within the Tertiary section, which is par-
ticularly well displayed in the southern Whipple Moun-
tains (sec. C, fig. 4), records a change from breccias,
conglomerates, and lavas to limestones, sandstones, and
siltstones. These sediments were deposited in relative
1y small basins but show locally strong discordance
upon the older rocks. Tilting and faulting of the older
Tertiary rocks had thus begun, at least in some areas,
and local blockage of drainage was occurring. This event
can be dated as generally between 20 and 17 my ago,
the age of underlying andesites and the overlying Peach
Springs Tuff.

The Peach Springs Tuff is apparently conformable
with underlying rocks at a few localities, but at most
outcrops it is unconformable on a variety of sedimen-
tary and volcanic rocks. The upper contact of the tuff
and its erratic preservation indicate considerable ero-
sion after its emplacement as well. Younger con-
glomerates commonly contain boulders and cobbles of
the tuff, but in most areas these rocks are not well ex-
posed. The Peach Springs does not cover sufficient area
in most places in the region to provide a consistent
structural datum. However, in some locations, such as
Chemehuevi Valley, it is sufficiently widespread to
record moderate displacement by normal faults. It is
behaved that faults that affect the Peach Springs are
part of the important system of extensional faults that
are clearly related to the Whipple Mountains detach-
ment fault.

MIDDLE MIOCENE UNCONFORMITY

The most significant Tertiary unconformity in the
Vidal-Parker region occurs at the base of the fanglom-
erate of Osborne Wash, a complex .unit that probably
spans a long interval of time. In the extreme case,
sedimentary rocks younger than the Peach Springs Tuff
are standing vertical and are overlain by the nearly flat
lying fanglomerate. Though not everywhere spec-
tacular, this is a consistent angular unconformity of
regional importance. Age of the unconformity has not
been precisely established, but the youngest rock
thought to predate the unconformity is the basalt of the
Mopah Range (sec. B, fig. 4), about 14.5 my old. Near
Parker, basalts intercalated in the lower part of the
fanglomerate gave ages (table 2) from about 16.5 to

30 STRUCTURAL HISTORY, VIDAL—PARKER REGION, CALIFORNIA AND ARIZONA

12.5 m.y. ago. General relationships suggest that the
younger of these ages is probably more nearly correct.
If so, this would indicate that the unconformity devel-
oped about 13 or 14 my. ago, an age which is a little
older than that for a similar change in tectonism
described south of Lake Mead by Anderson, Longwell,
Armstrong, and Marvin (197 2), in which volcanic rocks
(Mount Davis and Patsy Mine Volcanics), highly ex-
tended and tilted, are overlain unconformably by the
Muddy Creek Formation, including the Fortification
Basalt Member consisting of several flows dated at
about 5—11 m.y. This range of ages is close to those
available for basaltic rocks of the fanglomerate of
Osborne Wash in the Parker area.

Damon, Shafiquallah, and Lynch (1973) date forma-
tion of this unconformity at between 17 and 12 my. ago
in northern Arizona; and Eberly and Stanley (1978), in
a synthesis of Cenozoic stratigraphy and geologic
history of southwestern Arizona, restrict formation of
the unconformity to 13-12 m.y. ago. Their restriction
does not seem to apply to the Vidal-Parker region where
only minor block faulting occurred after about 14 my.
ago.

WHIPPLE MOUNTAINS DETACHMENT FAULT

The most significant and spectacular Tertiary struc-
tural feature of the Vidal-Parker region is a major
detachment fault (fig. 9) named for the Whipple Moun-
tains where its relations are well exposed. Only faults
of this type in the Mojave-Sonoran Belt are here re-
ferred to the Whipple Mountains detachment fault. The
significance, and even the existence, of this fault has
been debated for many years. Probably the first to
recognize the fault was F. L. Ransome in unpublished
reports for the Metropolitan Water District of Califor-
nia in the 1930’s. He described it as an overthrust of
Tertiary age, and he believed that it occurred prior to
the main normal faulting of the region. Ransome’s
observations were later discounted by Kemnitzer (1937),
who did not recognize the nature of the detachment
fault and emphasized the higher angle faulting of the
eastern Whipple Mountains. Terry (1972) studied the
fault in detail in the eastern Whipple Mountains, but
she, too, called it a thrust fault and did not recognize
its involvement with rocks of Tertiary age. She did,
however, suggest that the fault has regional extent.
Shackelford (1976, 1980), on the basis of a thesis study
in the Rawhide Mountains, identified the fault as a
major Miocene gravity detachment surface, which he
called the Rawhide Mountains detachment fault. Fur-
thermore, he recognized the northeasterly transport of
the allochthon and the close relation between shingling
listric normal faults and the detachment surface. His

 

description indicates a structural situation in the Raw-
hide Mountains nearly identical with that mapped in
the Vidal-Parker region. More recently, Lingrey, Evans,
and Davis (1977) described the Whipple Mountains fault
as a denudational fault of Tertiary age, between 14 and
19 my. in age, and they indicated a northeasterly
transport for the allochthon.

Geologists for the Southern Pacific Company mineral
survey in 1960 mapped fairly continuous low-angle
faults in the Chemehuevi, Sacramento, and Piute Moun-
tains, Calif. (pl. 2). According to Keith Howard (US.
Geological Survey, oral commun., 1979), however, the
fault in the Piute Mountains is not the typical detach-
ment type found farther southeast. In the present
study, reconnaissance of some of these faults showed
that many of them do have the characteristics of the
Whipple Mountains detachment fault (pl. 2). Study of
aerial photos, and limited reconnaissance, indicate that
faulting of this type may also be present in the Mohave
Mountains, Ariz.

Plate 2 shows the distribution, both mapped and in-
ferred, of the Whipple Mountains detachment fault in
Arizona and California. The structure probably extends
into areas beyond those shown, particularly to the
northwest and southeast. It has not been identified
beyond the general boundaries of the Moj ave-Sonoran
Belt.

My interpretation of the subsurface extent of the
fault is shown on plates 2 and 4. Connection of the fault
from range to range beneath cover of upper Cenozoic
rocks has not been proven, but characteristics, at least
in the Vidal-Parker region, are so similar in different
places that it is reasonable to postulate such connec-
tions. Furthermore, estimates of the amount of trans-
port on the fault require that it extend distances at least
equal to that between ranges.

Physical characteristics of the Whipple Mountains
detachment fault are easily recognized in most ex-
posures. The fault surface is normally a planar, smooth,
locally polished surface, with very few abrupt changes
in attitude. Multiple splays or wide gouge or breccia
zones are not common. Slickensides or grooves are local-
ly present and nearly always indicate relative northeast-
ward motion of the upper plate—regardless of the
direction of dip of the fault. Small, thin wedges of Ter-
tiary sedimentary rocks have been observed caught
along the fault between upper and lower plate metamor-
phic rocks. Adjacent to the fault, a finely crushed zone
several meters thick is commonly present, principally
in the lower plate metamorphic rocks. This material is
stained dark bluish green to orange locally, and copper
carbonates are present along the fault in some areas.
Most of the copper and gold mines and prospects of the
region are located on or near this detachment surface.

STRUCTURE AND TECTONICS OF THE VIDAL-PARKER AREA AND SURROUNDING REGION 31

Mineralization occurs in both upper and lower plates of
the fault, and deposits are found in metamorphic rocks,
in Paleozoic carbonate rocks, and in volcanic and sedi-
mentary rocks of Miocene age. Terry (1972) and Davis,
Anderson, Frost, and Shackelford (1980) have described
a thick mylonitized zone below the fault in the eastern
Whipple Mountains. I observed similar mylonitic rock
in association with the Whipple Mountains detachment
fault in the Riverside and Buckskin Mountains.

The fault is rarely cut by other faults or intrusive
rocks in the Vidal-Parker region. However, in the south-
ern Riverside Mountains, rhyolite bodies were intruded
along it (see map by Hamilton, 1964), and subsequently
they were brecciated but not sheared off, offering a
possible means for more exact dating of the latest fault
movement in that area. In the western Whipple Moun-
tains, the Chambers Well and Vidal Valley fault zones
appear to offset the Whipple Mountains fault a small
amount (pl. 4). In the Buckskin Mountains, offsets of
several hundred feet, also on northwest-trending faults,
are probable (pl. 2).

In cross sectional view (fig. 9), the fault dips away
from the Whipple Mountains at about 5°. However,
measured dips on the fault surface around the edge of
the Whipple Mountains range from 5 ° to 30° and aver-
age about 20 °. The reason for the discrepancy between
these two figures, 5 ° and 20°, is not readily apparent,
but it may be due to the presence of a semicircular in-
flection in the fault surface near the foot of the Whipple
Mountains, to a tendency for the best fault plane ex-
posures to be where dips are about 20°, or to bias in-
troduced by measurements made on shoaling normal
faults very near their juncture with the main detach-
ment plane. In order to gain a better perspective of
these problems, a regional structure contour sketch (fig.
10) was prepared of the known and postulated exten-
sions of the fault. Only where structure contours in-
tersect the fault is there good elevation control;
elsewhere, the map is based on generalized topography
over the lower plate and on estimates of elevation where
the fault is buried. Crude as it is, the map shows several
interesting features. The inflection mentioned previ-
ously is noticeable, particularly on the northeast side
of the Whipple Mountains. Steeper than average dips
are also suggested by the contours in the Chemehuevi,
Mohave, and Rawhide Mountains. These steeper gra-
dients appear to face the Colorado River, and locally the
Bill Williams River, and together with the fractured
nature of the upper plate must have strongly influenced
the early courses of the rivers. The map also suggests
the interplay of two structural trends, northeast-
southwest oriented uplifts, and the subsequent local
modification of these by northwest-trending faults. No
regional trend in elevation of the fault surface is evident.

 

Detailed regional study of the fault is needed for closer
definition, but it is clear that development of present
topography was closely controlled by the Whipple
Mountains detachment fault and associated structure
and lithology.

Several northeast-trending troughs are present in the
detachment fault plane. One of the most notable is in
the Riverside Mountains (pls. 1, 4) where such a trough
contains Tertiary rocks of the upper plate striking
northwest and dipping southwest at angles as high as
80°. This attitude is maintained from one edge of the
trough to the other, which indicates that the rocks were
transported into the trough by the detachment fault.
This trough, or one adjacent and parallel to it, may ex-
tend northeastward up the Colorado River Valley as far
as the Bill Williams River (fig. 10). It was suggested
previously that in some areas coarse Tertiary deposits
probably accumulated next to northeast-trending ridges
in the basement rocks. These ridges seem to have
strongly influenced the shape of the fault plane in some
areas. Other northeast-trending basins, such as
Mc Mullen and Butler Valleys, lying between the
Buckskin, Harcuvar, and Harquahala Mountains (pl. 2),
are suspected as additional areas where the detachment
fault is present but buried in most places. Terry (1972)
also suggested this possibility.

In the Vidal-Parker region, there are few exceptions
to the persistent northwest strike and southwest dip
of the Tertiary rocks in the upper plate of the fault. To
the east, however, in the Buckskin and Rawhide Moun-
tains, attitude of the rocks becomes locally more
variable, although regionally the northwest-trending
structural grain of faulting and southwestward rotation
of beds persists (Lucchitta and Suneson, 1977a; Lasky
and Webber, 1949; Otton, 1977). In one narrow
northeast-trending trough located northwest of Clara
Peak in the Buckskin Mountains (pl. 2), the Tertiary
rocks strike parallel to the trough and dip to the
southeast. Shackelford (1980) reported that in the
Rawhide Mountains the tectonic transport direction of
the upper plate was dominantly northeastward, but he
added that the direction was locally controlled by con-
figuration of the basement structure. Perhaps toward
the northeast margin of the Moj ave-Sonoran Belt, struc-
tural complexities in the basement rocks and lessening
cover of Tertiary rocks favored more diverse local
movements of the allochthon.

REGIONAL IMPLICATIONS

In this report the Whipple Mountains detachment
fault has been documented by mapping in the Whipple,
Buckskin, and Riverside Mountains. In addition,
reconnaissance has confirmed its presence in the Cheme-
huevi and the northeastern part of the Sacramento

32 STRUCTURAL HISTORY, VIDAL—PARKER REGION, CALIFORNIA AND ARIZONA

115“UU'

 

 
    
   

 

34"UU' —

 

  

 

35°00 ll4”[]U’ 113°22'45"
) l
l
l
) \O\Needles
Trace of Whipple Mountains
detachment fault \
000?:
’9
109$
0$ _
$0
00404
Ill/S
l

 

[] 10 20 30 4f] 5'0 KILDMETEHS
|

FIGURE 10.—Structure contour sketch map of the Whipple Mountains detachment fault. Shaded areas, lower plate (mapped and inferred);
dotted line, trace of detachment fault. Heavy dashed lines, faults; bar and ball on downthrown side; arrows show direction of lateral
movement, queried where uncertain. Contour interval 500 ft; contours dashed where fault is beneath surface, queried where control is

especially poor.

Mountains. Studies by others indicate that a similar The faulting of the Whipple Mountains detachment
structure is also present in the Rawhide Mountains, type is similar in many ways to Tertiary low-angle faults
Ariz., and probably in the valleys between the Harcuvar mapped elsewhere in the Basin and Range province, but
and Harquahala Mountains. It seems reasonable to con- particularly to those in the Walker Lane Belt (as defined
clude, therefore, that a detachment fault, possibly a here, p. 4) to the northwest, and in the Texas lineament
nearly continuous surface, is present in an area about (Albritton and Smith, 1957) to the southeast in Arizona.
100 km wide by at least 150 km long (fig. 9). Barosh (1969) called the southwestern edge of these

STRUCTURE AND TECTONICS OF THE VIDAL-PARKER AREA AND SURROUNDING REGION 33

belts the Mojave lineament and emphasized its great
length and strike-slip faulting character. Albritton and
Smith (1957), in their review of the history of the linea-
ment, pointed out that Kelley (1955) mentioned the
Texas lineament as one of the most prominent in North
America. Kelley also implied that the Walker Lane and
Texas lineaments should be connected, a view I share.
Most authors except Kelley and Barosh had envisioned
the Texas lineament as bending westward to join the
Transverse Ranges of Southern California. The physiog-
raphy and structure of the eastern Mojave Desert seem
to argue against such an interpretation. Connecting the
Walker Lane and Texas lineament provides an effective
eastward terminus for the major left lateral faults of
southern California—the Garlock fault and those of the
eastern Transverse Ranges. Connecting the Texas linea-
ment and the Transverse Range structure has led some
authors (Albritton and Smith, 1957) to imply that the
zone is one of left-lateral strike-slip; whereas, evidence
in hand strongly suggests that in Arizona and south-
eastemmost California right-lateral, probably oblique
slip, at least in Tertiary time, is the most likely style
of displacement.

I believe that major detachment faulting of Tertiary
age is an important feature of the structural corridor
from southeastern Arizona to northwestern Nevada.
Faulting of this type, not everywhere proven to be
Tertiary in age, has been described in the Tucson area
(Drewes, 1973; Davis, 1975; Thorman, 1977), at Old Dad
Mountain (Dunne, 1977), and in the Kingston Range,
Calif. (Hewett, 1956), in southeastern Nevada (Ander-
son, 1971), in the Death Valley region (Noble, 1941;
Hunt and Mabey, 1966; Wright and Troxel, 1973;
Wright and others, 1974), and in the Yerington, N ev.,
area (Proffett, 1977). Armstrong (1972) has summarized
evidence for Tertiary low-angle denudational-type
faulting in the Sevier orogenic belt area of eastern
Nevada and western Utah. In that region the evidence
for Tertiary age of the low-angle faulting is not always
as clear as it is in the Mojave-Sonoran Belt. Never-
theless, a number of well-documented cases have been
described. Many other areas, such as the Kingston
Range, Calif, for example, lack Tertiary rocks, so that
determination of the age of the faults is difficult, but
the listric or flattening normal faults in the upper plate
and their mergence into a single sharp plane of disloca-
tion, together with steeply rotated beds in the fault
blocks, are features that serve to characterize and iden-
tify the structure.

Perhaps the most striking structures similar to the
Whipple Mountains detachment fault are the turtle-
backs of the Death Valley area (Curry, 1938), which
have been interpreted by some authors (Hunt and
Mabey, 1966) as part of a continuous fault, the

 

Amargosa thrust. A number of different mechanisms
have been proposed for formation of the turtlebacks or
Amargosa thrust, but I prefer the interpretation of
Wright, Otton, and Troxel (1974), which relates the
faulting to extensional tectonics. Specifically, they
believe the individual turtlebacks to be giant fault
mullions; they conceived of the surfaces developing
along preexisting planes of weakness, closely followed
by deposition of the Tertiary rocks and by pulling apart
of the Death Valley area in a northwest-southeast direc-
tion, giving impetus to continued gliding on the fault
surfaces. This structural development could apply to
the Whipple Mountains detachment fault, except that
major movement occurred after most of the Tertiary
rocks were deposited and the direction of extension was
at right angles (northeast-southwest) to that in the
Death Valley area; significantly, there was no develop-
ment in the Vidal-Parker region of deep structural
basins, and, therefore, no driving force for continued
downslope movement on the Whipple Mountains fault.

ORIGIN OF
WHIPPLE MOUNTAINS DETACHMENT FAULT
AND REGIONAL EXTENSION

Before speculating on tectonic reasons for develop-
ment of the fault, it is well to summarize some perti-
nent facts. First, abundant stratigraphic and structural
evidence restricts the major movement on the fault to
a period of less than a 5 my. range—younger than about
18 my, the approximate age of the Peach Springs Thff,
and older than about 13 my, the probable oldest age
of basalt of the fanglomerate of Osborne Wash, which
is not cut by the fault. Basalt of the Mopah Range, dated
at 14.5 my. old, probably is involved in the faulting, but
this has not been proven. The fact that a few of the
major faults that cut the younger ’Ibrtiary rocks also
displace the Whipple Mountains detachment fault sug-
gests that movement on the latter may have been com-
pleted even earlier. Shackelford (1976) gave a maximum
age of 15.9 m.y. for the deformation in the Rawhide
Mountains, and Lingrey, Evans, and Davis (1977)
assigned an age of between 14 and 19 my. for the
Whipple Mountains fault. All the available evidence,
therefore, suggests that most, if not all, of the movement
was accomplished in a few million years or less.

Fission-track studies (Dokka and Lingrey, 1979) on
metamorphic rocks from the eastern Whipple Moun-
tains show that rapid cooling occurred there in the
period between about 20—18 m.y. ago. As they pointed
out, this agrees well with the age of volcanism in that
area, but since these same volcanic rocks are displaced
by the Whipple Mountains detachment fault, that fault-
ing appears to be a somewhat younger event.

34 STRUCTURAL HISTORY, VIDAL—PARKER REGION, CALIFORNIA AND ARIZONA

Slickensides and grooves in the fault surface trend
rather consistently northeast-southwest, from the
Rawhide Mountains to the Riverside Mountains. Low-
angle normal faults in the upper plate are also fairly con-
sistent, trending at right angles to the direction of
transport and dipping northeast. Thus, the dominant
apparent direction of movement of the allochthon was
to the northeast in an area at least 100 km wide. The
actual amount of displacement was considered by
Lingrey, Evans, and Davis (1977) to be at least 15 km,
based on dissimilarity of upper and lower plate base-
ment rock in that distance in the Whipple Mountains.
Comparison of metamorphic rocks in the two plates in
the eastern and western Whipple Mountains suggests
that the amount of displacement probably exceeds
20 km; metamorphic rocks similar to those in the upper
plate in the northeastern Whipple Mountains do not ap-
pear in the lower plate east of the Chambers Well area
(pl. 1). If the Paleozoic rocks in the upper plate northeast
of Parker came from similar rocks in the lower plate in
the Riverside Mountains area, the transport distance
may have been as much as 35 or 40 km.

Apparently, at the original location of the upper plate,
prior to faulting, exposures of rocks typical of the lower
plate in the eastern Whipple Mountains were very rare.
The evidence of this lack of exposure is the scarcity of
clasts of lower plate rocks in the Tertiary breccias in
the eastern Whipple Mountains. Davis, Anderson,
Frost, and Shackelford (1980, p. 94—95) emphasized the
presence of a few clasts of the lower plate mylonite—or
banded gneiss—in the Tertiary section of the eastern
Whipple Mountains. In my experience, such occur-
rences are very rare, and one is impressed by the ex-
treme scarcity of such material. Some occurrences
(Davis and others, 1980) of lower plate gneiss cobbles
in the Tertiary section may well be in rocks high in the
section, quite possibly in units that should properly be
assigned to the fanglomerate of Osborne Wash. (See pl.
1.)

Davis, Anderson, Frost, and Shackelford ( 1980,
p. 1 1 1) have offered evidence that the mylonite zone was
developed well before the Whipple Mountains detach-
ment faulting. They have obtained early to middle
Tertiary K-Ar ages (oral commun., 1980) on the
mylonitic gneiss and have associated the zone with in-
trusive rocks beneath the fault; .they also pointed out
that in the west-central Whipple Mountains the detach-
ment fault diverges from what they call the “mylonitic
front.” In addition, mineral lineations in the lower plate
gneiss are commonly not parallel with the detachment
surface. The evidence for two separate tectonic events,
mylonitization and detachment faulting, is compelling,
yet the close spatial association of the two features is
puzzling, as is the obvious active tectonism indicated

 

by the lithology of the Miocene rocks. I believe that the
close spatial association of'the detachment fault with
the mylonitization is the result of a strong tendency for
the shearing to occur near the top of the competent
mylonitized rocks. I have seen no good evidence for
significant post-detachment doming. Radial dips in Ter-
tiary rocks away from structural highs are nonexistent
in the Vidal-Parker region, and there is no indication
that radial faulting occurred. In the Riverside Moun-
tains, however, Tertiary breccias do contain abundant
Paleozoic rock clasts typical of the lower plate im-
mediately to the east. This could mean that the amount
of effective transport lessened close to the southwest
edge of the Mojave-Sonoran Belt. .

Thus, available evidence points strongly to a fairly
rapid and directionally consistent extension of as much
as 40 km in a period probably occurring mostly between
about 17 and 14 my. ago. These figures yield a rate of
movement of a little over 1 cm per year, a figure con-
sistent with estimates (Stewart, 1971, p. 1036) for Great
Basin extensional rates.

The mechanism and driving forces of the Whipple
Mountains detachment fault are not well understood.
Its wide distribution and consistently northwest-
trending upper plate structure, as well as the lack of
a regional northeasterly slope, all argue strongly against
a pure gravitational origin. Transport between strike-
slip faults and volume compensation by concurrent
plutonism, as envisioned by Anderson (1971, p. 57), is
an appealing explanation, but important northeast-
trending strike-slip structures or sizeable Tertiary
intrusives have not been recognized in the area.

As mentioned earlier, possible northeast-trending
“welts” are a feature of at least part of the region. These
may be a clue that older northeast-trending zones of
weakness may have existed, and they probably record
a regional Tertiary thermal event that brought laminar
flow fairly close to the surface. This concept of a
plastically extending substratum, as suggested by
Hamilton and Myers (1966), Anderson (1971, p. 56), and
SteWart (1971, p. 1038), is an attractive mechanism for
the deformation.

The overprint of Tertiary volcanism, none of it
voluminous in this area, may also have been localized
by the welts. The shift to bimodal rhyolite-basalt
volcanism so often cited (Christiansen and Lipman,
1972) as accompanying the beginning of basin-and-
range faulting, seems reasonably coincident with
faulting in the Vidal-Parker region, but contrary to
events in most of the Basin and'Range province, this
faulting ended as abruptly as it began. It is interesting
to note that the virtual cessation of extension and major
faulting in the Vidal-Parker region is essentially syn-
chronous with the generally accepted age of inception

STRUCTURE AND TECTONICS OF THE VIDAL—PARKER AREA AND SURROUNDING REGION 35

of the present San Andreas fault, about 14 my. ago.
This is another strong indication that the structure in
the region is related to plate tectonics and underflow
of the continental margin by the Pacific plate.

EARLY END OF FAULTING

The low intensity of Pliocene and virtual lack of
Pleistocene faulting, in coincidence with a near absence
of even low-level seismicity, make this region unique in
the Basin and Range province. Until we better under-
stand the cause of presently active basin-and-range
faulting elsewhere, it is difficult to explain its absence
here. N o obvious differences in the geologic history can
be called upon to explain the rather abrupt early end
to structural movements. The region in which this
quiescence is best displayed seems to be generally coin-
cident with part of the Moj ave-Sonoran Belt, which in
turn is geophysically characterized by rather subdued
anomalies. The Belt can be viewed geophysically as a
relatively quiet bench between the foot of a regional
northwest-trending gravity gradient (pl. 2) and the
northwest trends associated with the San Andreas and
older structures. According to seismic refraction data
(see p. 23), the Vidal-Parker region is only slightly
anomalous; the crust is probably a little thinner
(26—27 km) than in most of the Basin and Range area,
and the upper mantle velocity (about 8 km/s) is perhaps
a little higher than average for the province. Perhaps
a partial explanation can be found in the possibility that
the boundary between plastic and brittle crustal failure
may lie at a shallower depth than elsewhere in the Basin
and Range, and therefore that during the last 10 my.
or so, extension has taken place almost entirely by
plastic flow at depth.

PLIOCENE-PLEISTOCENE TECTONICS

Faults and lineaments of Pliocene and possibly early
Pleistocene age in the Vidal-Parker region are listed in
table 5. Available information indicates that faulting
of this age becomes a little more intense near the north-
east edge of the Vidal-Parker region and increases
northeastward toward the margin of the Moj ave-
Sonoran Belt. Northwest-trending faults along the Bill
Williams River and in the Buckskin Mountains cut
basaltic rocks and some of the fanglomerate of Osborne
Wash. Several of the northwest-trending faults in the
northeastemmost Whipple Mountains produce tilting
of as much as 35 ° in the fanglomerate (pls. 1, 4). Farther
east, about 10 km above the mouth of the Bill Williams
River, another fault displaces basalt of the Osborne at
least 100 m vertically. Examination of aerial photos and

 

discussion with Ivo Lucchitta and Neil Suneson of the
US. Geological Survey indicate that significant faulting
of probable Pliocene volcanic rocks and sediments con-
tinues to occur to the northeast in the Bill Williams
Mountains area. As mentioned previously, similar faults
cut alluvium of probable Quaternary age a few miles
northeast of Topock, Ariz. (pl. 2).

The youngest rocks known with certainty to be
faulted at the surface in the Vidal-Parker region are the
marine and supra-littoral equivalents of the Bouse For-
mation (age about 5 my). Several faults with only a
few meters of displacement in sandy Bouse Formation
were mapped (Dickey and others, 1980; Carr and others,
1980) along the south flank of the Whipple Mountains.
At the north end of Mesquite Mountain, along Bouse
Wash, is a fault (pl. 1) with at least 3 m of offset in the
Bouse. It is close to the only steep linear gravity gra-
dient in the Vidal-Parker region. Another fault offset-
ting the Bouse is present on the northwest side of
Mesquite Mountain. A zone of small faults occurs in
sandy fanglomerate in the Parker NW. quadrangle
(Dickey and others, 1980). Rocks cut by these faults are
mapped as fanglomerate of Osborne Wash, but it is
possible that they are coarser grained subaerial time
equivalents of the Bouse Formation. Individual faults
in the zone are generally less than 300 m long and have
less than 5 m of vertical offset. On this same trend,
Metzger and Loeltz (1973, pl. 1) showed a buried fault
in the Bouse 2 km south of Parker. The fault or fold is
based on drill hole information and is shown as having
about 15 m of offset in the Bouse Formation-
fanglomerate of Osborne Wash contact.

Several low-angle faults, judged to be slump features,
were observed in fine-grained sediments of the Bouse,
particularly in the areas between the Whipple Moun-
tains and Lake Havasu City. Because of the limited ex-
posures of the Bouse, other small faults may well be
present, but buried.

Several strong photo lineaments, some of which are
definitely faults, occur in the old alluvium (unit QTa,
pl. 1). In addition, there are a number of small faults
that do not show up on aerial photos. These features
are summarized in table 5, and most are shown on plate
1. None of the faults in table 5 are considered to cut
alluvium less than about 1 my. in age, and most are
probably latest Pliocene in age.

The youngest faults of the region are difficult to
interpret. There is no evidence that any of them repre-
sent more than minor adjustments, mostly along pre-
existing structures. The only such faults that constitute
any sort of continuous zone are those in a north-
trending belt on the south side of the Whipple Moun-
tains, and nearly all of these are older than the old
alluvium (loc. 4, table 5). They could represent shears

36

STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

TABLE 5.—Faults and photo lineaments in old alluvium of the Vidal-Parker region

 

 

Location Strike Dip Displacement Length Remarks
1. Unsurveyed NW1/4 sec. 5, N. 45° W. 60° NE. 1 m About Very slight topographic
T. 2 N., R. 23 E., 600 m. expression.
between Savahia and
Pyramid Peaks.
2. Unsurveyed sec. 8, T. 9 N., N. 40° W. Unknown Unknown About Slight topographic
R. 17 W., upper Osborne 600 m. expression, distinct
Wash area. color lineation.
3. NEl/4 sec. 24, T. 2 N., Northeast 55° NW. 0.5 m Unknown Cuts caliche at base
R. 23 E. About 0.2 km NE of old alluvium
of jeep trail between (unit QTa, pl. 1).
Savahia Peak and Chambers
Well road.
4. Unsurveyed: sec. 5, Northerly 65° to Mostly I m; As much as Zone of small short
T. 1 N., R. 25 E., and vertical. one at 300 m. faults about 2 km
sec. 31 and 32, T. 2 N., least 5 m. long, a few of which
R. 25 E., in aqueduct cut cut beds possibly as
and north and south of it. young as the old
alluvium.
5. Near north edge of N. 100 W. 80° NE. At least At least Same zone that cuts
unsurveyed sec. 30, 2 m. 100 m. sandy phase of Bouse
T. 2 N., R. 25 E. Formation.
6. NWl/4 sec. 2, T. 2 N., N. 15° W. Probably Unknown At least Very slight topographic
R. 22 E., about 400 m eastward. 100 m. scarp.
east of U.S. Highway 95.
7. Unsurveyed E1/2 sec. 20 North and Unknown Unknown About Not exposed, but probably
T. 2 N., R. 22 E. northwest. 300 m. displaces caliche
cemented old
alluvium.
8. 5-7 km N. 70° W. of Whipple N. 45° W. to Unknown Unknown 1.5 km Noticeable photo
Well, north side Whipple N. 800 W. lineament.
Mountains.
9. Sec. 4, T. 2 8., R. 21 E., N. 50° W. Unknown Unknown 2 km Noticeable photo
near middle of Rice Valley. lineament; possible
ground water barrier.
10. Sec. 25, T. 2 N., R. 22 E. N. 80° W. Unknown Unknown 1.7 km Weak, but distinct
and sec. 30, T. 2 N., lineation.
R. 23 E., north-northwest
of Vidal Junction.
11. Sec. 18, T. 1 S., R. 24 E.; N. 65° W. Unknown Unknown 1 km Noticeable photo
south-southeast of Vidal. lineament.
12. Near north end of valley North- Unknown Unknown Unknown Cuts old alluvium (QTa).
between Mopah Range and northwest. Found in reconnaissance

Turtle Mountains, about
3 km west of Mopah Peaks.

for Southern California
Edison Company by
Woodward-McNeill, Inc.

 

in the surficial materials caused by right-lateral stresses
on nearby northwest-trending faults in the bedrock. As
such they might be considered as incipient basin-and-
range faults that never developed further.

If there is significant structural displacement of the
Bouse Formation, it is buried beneath the alluvium. All
evidence, however, indicates that the Bouse has not

been greatly disturbed by structural movements in the
Vidal-Parker region, although Lucchitta (1979)
demonstrated differential uplift of the Bouse about
50 km to the north, along the margin of the Mojave-
Sonoran Belt. There is a suggestion of some warping
of the Bouse, particularly on the north side of the
Whipple Mountains, but even most of this could be

REFERENCES CITED 37

explained by initial dips. However, as the Bouse is more
than 500 ft below sea level beneath the Colorado River
flood plain near the south edge of the mapped area (pl.
1; Metzger and Loeltz, 1973, pl. 1), it seems likely that
some downwarping and faulting has occurred in that
part of the area at least. Between Parker and the Big
Maria Mountains, the Colorado River now maintains
a course at the west side of the wide flood plain of
Parker Valley, which suggests a possible slight regional
tilt to the west in Holocene time.

SUMMARY OF STRUCTURAL HISTORY

Geologic studies in the Vidal-Parker region permit a
tentative interpretation of some of the Mesozoic and
Cenozoic structural events.

The age, or even the existence, of Mesozoic faulting
in this region has not been proven; rocks of Mesozoic
age are involved in low-angle normal and thrust faulting
along the southwest side of the area, but the maximum
age of this faulting has not been determined. Possible
influence on later structural events suggests there may
have been an early conjugate fault system of northeast
and northwest trends.

Intrusion of small granitic batholiths took place in
Late Cretaceous time. Margins of these intrusives and
adjacent Paleozoic and Mesozoic sedimentary rocks
underwent varying degrees of dynamic metamorphism.
This metamorphic event probably ended about 60 my
ago and was followed by uplift and erosion.

In middle Tertiary time it is postulated that magma—
tism in the crust caused tumescence or welts that
tended to localize on preexisting northeasterly trend-
ing structural zones of weakness, or, because of ten-
sional stress, between offset ends of concurrently
developing northwest-trending strike-slip faults. Core
complex metamorphism and intrusive activity was
accompanied by large-scale mylonitization. The welts
or uplifts, though fairly gentle, probably occurred
rapidly enough to shed considerable debris, which ac-
cumulated on the flanks as conglomerate, breccia, and
megabreCcia. In Miocene time, volcanism, mostly
andesitic and rhyodacitic, occurred at scattered centers
possibly related to these magmatic uplifts.

About 17 my. ago rapid extension began in the
Mojave-Sonoran Belt, possibly driven by southwest-
ward movement of the lower crust. As much as 40 km
of extension may have occurred in the Belt in a few
million years. The extension resulted in stretching and
thinning of the crust and formation of a regional low-
angle shear or detachment fault at fairly shallow depth,
which was probably controlled by the abrupt upper limit
of mylonitized rocks. This shearing off was accompanied

 

by synchronous northwest-trending low- to moderate-
angle normal faults and attendant rotation of fault
blocks. Abruptly, about 14 my. ago, this style of struc-
tural development ceased, perhaps in response to
changes in regional stress brought about by the begin-
ning of transform movement on the initial stages of the
San Andreas fault system.

Only minor dip-slip and right-lateral slip occurred in
late Miocene and Pliocene time on a few of the
northwest-trending faults. Toward the northeast and
southwest edges of the region, these faults had more
and perhaps slightly younger displacement. Eruption
of basaltic and minor rhyolitic rocks began about
14 my. ago and continued sporadically until about
6 my. ago. Very small normal faults, mostly high-angle
and having north and northwest trends, developed local-
ly in late Pliocene time. Slight regional and local warp-
ing has been the only structural disturbance in the
Pleistocene.

REFERENCES CITED

Albritton, C. C., J r., and Smith, J. F., Jr., 1957, The Texas lineament,
in v. 2 of Relaciones entre la tecténica y la sedimentacién: Inter-
national Geological Congress, 20th,‘Mexico D. F., 1956, sec. 5,
p. 501—518.

Anderson, J. L., Davis, G. A., and Frost, E. G., 1979, Field guide to
regional Miocene detachment faulting and early Tertiary(?)
mylonitization, Whipple-Buckskin-Rawhide Mountains, in south-
eastern California and western Arizona, in P. L. Abbott, ed..
Geologic excursions in the southern California area: Geological
Society of America Guidebook, p. 109—133.

Anderson, R. E., 1971, Thin skin distension in Tertiary rocks of
southeastern Nevada: Geological Society of America Bulletin, v.
82, no. 1, p. 43—58.

._1977, Composite stratigraphic. section of Tertiary volcanic rocks
in the Eldorado Mountains, N evade: US. Geological Survey Open-
File Report 77-483, 2 p., 1 table.

Anderson, R. E., Longwell, C. R., Armstrong, R. L., and Marvin, R. F.,
1972, Significance of K-Ar ages of Tertiary rocks from the Lake
Mead region, Nevada-Arizona: Geological Society of America
Bulletin, v. 83, no. 2, p. 273—288.

Armstrong, R. L., 1972, Low-angle (denudation) faults, hinterland of
Sevier orogenic belt, eastern Nevada and western Utah: Geological
Society of America Bulletin, v. 83, no. 6, p. 1729—1754.

Armstrong, R. L., and Higgins, R. E., 1973, K-Ar dating of the begin-
ning of Tertiary volcanism in the Mojave Desert, California:
Geological Society of America Bulletin, v. 84, no. 3, p. 1095—1100.

Armstrong, R. L., Speed, R. C., Graustein, W. C., and Young, A. Y.,
1976, K-Ar dates from Arizona, Montana, Nevada, Utah, and
Wyoming: Isochron/West, no. 16, p. 1-6.

Armstrong, R. L., and Suppe, John, 1973, Potassium-argon
geochronometry of Mesozoic igneous rocks in Nevada, Utah, and
southern California: Geological Society of America Bulletin, v.
84, no. 4, p. 1375-1391.

Barosh, P. J ., 1969, The Mojave lineament—a zone of possible wrench
faulting of great length, in Abstracts for 1968: Geological Socie-
ty of America Special Paper 121, p. 482.

Biehler, S. H., 1976, Regional Bouguer gravity map, in San Diego Gas

38 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

and Electric Co. Early Site Review, Sundesert Nuclear Plant:
Amendment 11, fig. 2.5K—1.

Bishop, C. C., 1963, Geologic map of California, Needles sheet: Califor-
nia Division of Mines and Geology. scale 1:250,000.

Carr, W. J ., and Dickey, D. D., 1977, Major tectonic zone in the eastern
Mojave Desert, in Geological Survey research, 1977: U.S. Geo-
logical Survey Professional Paper 1050, p. 70.

1980, Geologic map of the Vidal, California, and Parker SW,
California-Arizona. quadrangles: U.S. Geological Survey Miscel-
laneous Investigations Map I-1125, scale 1:24.000.

Carr, W. J ., Dickey, D. D.. and Quinlivan, W. D., 1980, Geologic map
of the Vidal NW, Vidal Junction, and parts of the Savahia Peak
SW and Savahia Peak quadrangles. San Bernardino County,
California: U.S. Geological Survey Miscellaneous Investigations
Map I—1126, scale 1:24,000.

Chapman, R. H., and Rietman, J. D., 1976, Bouguer gravity map of
California, Needles sheet: California Division of Mines and
Geology, scale 1:250.000.

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Damon, P. E., Shafiquallah, M., and Scarborough. R. B., 1978. Revised
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Davis, G. A., Anderson, J. L., Frost, E. G.. and Shackelford, T. J .,
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Memoir 153, p. 79—130.

 

 

 

 

 

Davis, G. H., 1975, Gravity-induced folding off a gneiss dome com-
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Davis, G. H., and Coney, P. J., 1979, Geologic development of the
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Dickey, D. D., Carr, W. J., and Bull, W. B., 1980, Geologic map of
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Dokka, R. K., and Lingrey, S. H., 1979, Fission track evidence for
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Drewes, Harald, 1973, Large-scale thrust faulting in southeastern
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Dunne, G. C., 1977, Geology and structural evolution of Old Dad
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Eberly. L. D.. and Stanley, T. B., J r., 197 8, Cenozoic stratigraphy and
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Fenneman, N. M., 1931, Physiography of Western United States: New
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Frost. E. G., and Martin, D. L., eds., 1982, Mesozoic-Cenozoic tectonic
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Hamilton, W. B., 1964, Geologic map of the Big Maria Mountains
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1971, Tectonic framework of southeastern California: Geological
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Hamilton, W. B., and Myers. W. B., 1966, Cenozoic tectonics of the
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Hazzard, J. C., Gardner. D. L., and Mason, J. F., 1938, Mesozoic(?)
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Healey. D. L., 1973, Bouguer gravity map of California, Kingman
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Healey, D. L., and Curry, F. E.. 1980. Complete Bouguer gravity
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Hewett, D. F., 1956, Geology and mineral resources of the Ivanpah
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Hileman, J. A., Allen, C. R., and Nordquist, J. M., 1973, Seismicity
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Hunt, C. B., and Mabey, D. R., 1966. Stratigraphy and structure.

 

 

REFERENCES CITED 39

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40 STRUCTURAL HISTORY, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

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‘9 U.S. GOVERNMENT PRINTING OFFICE: 1991 -573-049/26030

 
 
 
 

 

 

 

 

 

 

(DE

75
P6
Vi 141/30
DEPARTMENT OF THE INTERIOR PROFESSIONAL PAPER 1430
US. GEOLOGICAL SURVEY PLATE 1
CORRELATION OF MAP UNITS
081 Holocene
QUATERNARY
Pleistocene
Pleistocene QUATERNARY
and AND
Pliocene TERTIARY
Pliocene
and
Miocene

 

  
 
 

Unconformity

_ TERTIARY

Unconformity

 

Miocene

  
 
  

 

    

Unconformity

UPPER PLATE LOWER PLATE

 

} Cretaceous MESOZOIC

MESOZOIC
AND
PALEOZOIC

 

PALEOZOIC

MESOZOIC
PALEOZOIC
OLDER (?)

 

|
} PRECAMBRIAM?)

 

DESCRIPTION OF MAP UNITS

 

Young alluvium (Holocene)

 

Young alluvium aeolian deposits (Holocene)

 

 

Intermediate alluvium (Pleistocene)

Old alluvium (Pleistocene and Pliocene)

 

 

Colorado River gravel (Pleistocene, Pliocene and
Miocene(?))

Colorado River deposits (Pleistocene and Pliocene)
Bouse Formation (Pliocene and Upper Miocene)
Fanglomerate of Osborne Wash (Pliocene and Miocene)

Trachytes and trachyandesites of Buckskin Mountains
(Miocene)

Basaltic rocks (Pliocene and Miocene)

 

Peach Springs Tufl' (Miocene)

Tuff and tuffaceous sedimentary rocks (Pliocene and
Miocene)

Sedimentary rocks (Pliocene and Miocene)

Volcanic and sedimentary rocks undifferentiated (Plio-
cene and Miocene)

Volcanic and sedimentary rocks undifferentiated, upper
part (Pliocene and Miocene)

Breccia,volcanicand sedimentary rocks undifferen-
tiated, lower part (Miocene)

Intrusive rocks (Miocene)

Rhyodacite lava flows and breccia (Miocene)
Andesite lava flows and breccia (Miocene)
Sedimentary breccia and megabreccia (Miocene)

Granite quartz monzonite, and quartz diorite (Creta-
ceous)

 

K99, Granite gneiss (Cretaceous)

I Upper platel sedimentary rocks undivided (late Paleo-
zoic and younger?)

Upper platel sedimentary rocks—Queantoweap Sand-
stone of McNair. (1951) or Esplanade Sandstone. and
overlying units (late Paleozoic)

Upper platel sedimentary rocks below Queantoweap or
Esplanade Sandstone (late? Paleozoic)

Upper plate1 gneisses (Mesozoic, Paleozoic, and
older?)

Lower platel sedimentary rocks of the Southern River-
side Mountains (Mesozoic? and older)

sf

 
  

Lower plate1 gneisses (Mesozoic? and older)

       
 
  
 

  

E .1 I.
7‘s

poets

W “”me
coawyy
’1‘?» I x"

   
 

Lower platel sedimentary rocks—Queantoweap Sand—
stone or Esplanade Sandstone and overlying units
(late Paleozoic)

Lower platel sedimentary rocks below Queantoweap
or Esplanade Sandstone (late? Paleozoic)

     

Lower platel metamorphic rocks (Precambrian?)

Metamorphic rocks intruded by numerous dikes and
sills of probable Tertiary age (Tertiary?-Precam-
brian?) v

 

1Upper and lower plates of the Whipple Mountains detachment fault

Contact
—————— Back of Colorado River terrace

fl Fault—Showing dip. Bar and ball on downthrown side;
50 Dashed where location uncertain. Dotted where con-
cealed, queried where doubtful

.- . , . , A—FA— Thrust Fault—Sawteeth on upper plate
1 WT ,,,,,,,, 5’. H , ' i 1, I __ I j, V i h —‘—‘-L‘—‘- Whipple Mountains detachment fault—Showing dip.

Dotted where concealed; queried where doubtful;
hatch marks on upper plate

——-I— Anticline—Showing approximate trace of axial plane

Syncline—Showing approximate trace of axial plane

—1’0— Strike and dip of beds or flow layering—Inclined

i Attitude of foliation

 

/

 

 

APPROXIMATE MEAN ARIZONA
DECLINATION, 1991

MAP LOCATION

SCALE 1:125 000
2 O 2 4 6 8 MILES

 

 

2 O 2 4 6 8 KILOMETERS
1

CONTOUR INTERVAL 200 FEET
NATIONAL GEODETIC VERTICAL DATUM OF 1929

NOTE: Owing to loss ofthe original compilation during report
processing, registry of geology with respect to topography
and culture is not precise, and this map contains un-
resolved errors in detail.

 

GEOLOGIC AND STRUCTURAL UNIT MAP
()I3'TIIIE‘VOI)[\LnIMAIII(EflR [{EK31()PJ,
CALIFORNIA-ARIZONA

 

 

Base by US. Geological Survey, 1:500 000 Geology by W.J. Carr, 00. Dickey, and
Needles, 1958-62, Phoenix, 1854—89, W.D. Ouinlivan, 1974—1977
Prescott, 1954—62, Salton Sea, 1959787

 

GE
75

PL,

’10. 1’7'30
PROFESSIONAL PAPER 1430

PLATE 2

 
 
 
  

DEPARTMENT OF THE INTERIOR

U.S. GEOLOGICAL SURVEY

116°
35°

 
  
 
 

PA . , _ 115°
. . , 113°

QUATERNARY

TERTIARY

MESOZOIC

PALEOZOIC

PRECAMBRAIN

EAESDTCEER , 3_ . 7 , p _ . Volcanic rocks (Quaternary)
85 \. V“ T . ~ : (/1 V ‘ a , I . K3 ‘ ' ,,
ISM' c- -, " y," / . i ‘ 3 -- ' ~ 1' ,7 ‘ 3' 0T3 Alluvium (Quaternary and Tertiary)—Includes Colorado
‘ I I L' ’ I I I ' I 7 River Deposits. Bouse Formation, and fanglomerate of
Osborne Wash
Tu Volcanic and sedimentary rocks (Tertiary)

TMzr Rhyodacite (Tertiary and Mesozoic)

Sedimentary rocks of the Livingston Hills Formation
type (Tertiary and Mesozoic)

Volcanic and sedimentary rocks, locally metamor-
phosed (Mesozoic)

Sedimentary and volcanic rocks, locally metamor-
phosed (Mesozoic and Paleozoic)

Sedimentary rocks, locally metamorphosed (Paleozoic)

 

Sedimentary rocks of the upper plate of the Whipple
Mountains detachment fault (Paleozoic)

Sedimentary rocks of the lower plate of the Whipple
Mountains detachment fault (Paleozoic)

Granite and gneissic granite, including some metamor-
phic rocks (Tertiary to Precambrian)

Metamorphic rocks undifferentiated (Mesozoic to
Paleozoic)

Metamorphic rocks of the upper plate of the Whipple
Mountains detachment fault (Mesozoic to
Precambrian)

Metamorphic rocks of the lower plate of the Whipple
Mountains detachment fault (Mesozoic to
Precambrian)

 

34°

._ Forepau

 

0,118
-< Contact

_I__..__
: Fault—Dotted where concealed. Bar and ball on
downthrown side; arrows show relative movement

—A—A- A—A Thrust or detachment fault—Dashed where concealed.
Queried where location is poorly controlled

law”
“.60

- — ' — - Prominent aeromagnetic lineament

 

_ - ' , ' ._ a. . , -_ -, 3 : 3 ; .. _ Edge of Mojave-Sonoran Belt—Dashed where very
_, . 3 ~ . g . . 3 3 . approximate

Western edge of eastern Mojave “aseismic” area

 

75

® © Bouguer gravity contours—Contour interval 5 miligals.
All values are negative. H indicates gravity highs. L in-
dicates gravity lows

116° 115° 114° 113°

I ,, .1 I p . I I; I 3 \ T ; _ . it - . I ’ , , ,. “ p 3. 35°f 1 K T
\\ ‘._ "I \ _ v" r 3 T t‘.: - 3 ~ , ..~ ‘ a ‘ I -. 1‘ V 3 l) I I (r , ’33 t. 0 A

34°

 

 

 

|
33°
SOURCES OF GRAVITY DATA CONTOURS JOINED
BY W. J. CARR IN AREAS OF OVERLAP

A. Bouguer gravity map of California, Needles sheet, complied
by R. H. Chapman and J. D. Rirttman, 1976: California Divi
sion of Mines and Geology

B. Healey, D. L., and Currey, F. E. 1980, Complete Bouguer
gravity anomaly map of theVidal area, California and
Arizona: U.S. Geological Survry Open—File Report 80-619

C.Regiona| Bouguer gravity map Sundesert Nuclear Plant,
California, compiled by S. H.Biehler: Early Site Review
Report, Amend. 1 1, Fig. 2.5 K—1,San Diego Gas and Elec—
tric Co., July 1976

D.West, R. E. and Summer, J. 8., 1973, Bouguer gravity
anomaly map of Arizona: Laboratory of Geophysics,
Department of Geosciences, University of Arizona, Tuc-
son, Arizona

NOTES: Most of the data in California are terrain corrected; most of the data
in Arizona are not terrain corrected
Station coverage varies greatly; hence contours are much general-

 

 

 

 

33°
116° a x
. M ' , :1 ’ . ‘ x. . 1 Z V , , ized particularly in areas A, D, and the southeastern part of C
4 115° ” ‘ \ _ ' ' 'i / ,. 4 I :3.. ' All areas except D have been reduced from a largerscale: area D has
Base by US. Geological Survey, 1:500 000 140 I 1133? been enlarged 2X
32:133. IRE; Ziiil‘slffiifigga lo SCALE 1°°° 00" ' -
: . . ‘ I__C‘) 10 20 30 40 Geology compiled by W. J. Carr from various sources: Arizona~Wilson and others
. . ‘1 510 MILES :igggl; Rawhide Mountains area—Shackeliord (1900). California—Needles sheet, Bishop
i——-——-—i I; Salton Sea sheet Jennin ligfiil‘ I ’ ’ '
10 , gs , pusreconnaissance and into I t
r—r r—r i-——? 10 20 30 4o 50 KILOMETERS -\ W- J- Ca" [we 8 Ion by
t r I CALIF\-\
CONTOUR INTERVAL 500 FEET ‘7
‘ARIZONAI

NATIONAL GEODETIC VERTICAL DATUM OF 1929

1990 MAGNETIC DECLINATIUN VARIES FROM 13°00 EASTERLY FOR THE SOUTHEASTERN CORNER T0
13°30 EASTERLY FOR THE NORTHWESTERN CORNER. MEAN ANNUAL CHANGE IS 0°04' WESTERLY 'g

MAP LOCATION

GENERALIZED REGIONAL GEOLOGIC AND STRUCTURAL UN
1T MAP AND BOUGUER GRA
OF PART OF SOUTHEASTERN CALIFORNIA AND WESTERN ARIZONA VITY MAP

 

   
 
 

 

 

7S
, ” \ P4
DEPARTMENT OF THE INTERIOR /~z‘c Tm 0F ”W0 2 V- ”30
us GEOLOGICAL SURVEY § J I“ PROFESSIONAL PAPER 1430
35115 P y , UN 2 4 1991 y PLATE 3
' ' 13° 3”)” ‘g/ ORRELATION OF MAP UNITS
IIIII \V’
} QUATERNARY
TERTIARY
1
MESOZOIC
PALEOZOIC
PRECAMBRAIN

 

0v Volcanic rocks (Quaternary)

0T8 Alluvium (Quaternary and Tertiary)—lncludes Colorado
River Deposits. Bouse Formation, and fanglomerate of
Osborne Wash

Tu Volcanic and sedimentary rocks (Tertiary)

IIII

 

TM" Rhyodacite (Tertiary and Mesozoic)

Sedimentary rocks of the Livingston Hills Formation
type (Tertiary and Mesozoic)

Volcanic and sedimentary rocks, locally metamor-
phosed (Mesozoic)

Sedimentary and volcanic rocks, locally metamor-
phosed (Mesozoic and Paleozoic)

 

Sedimentary rocks, locally metamorphosed (Paleozoic)

Sedimentary rocks of the upper plate of the Whipple
Mountains detachment fault (Paleozoic)

Sedimentary rocks of the lower plate of the Whipple
Mountains detachment fault (Paleozoic)

Granite and gneissic granite, including some metamor-
phic rocks (Tertiary to Precambrian)

Metamorphic rocks undifferentiated (Mesozoic to
Paleozoic)

  

Metamorphic rocks of the upper plate of the Whipple
Mountains detachment fault (Mesozoic to
Precambrian)

Metamorphic rocks of the lower plate of the Whipple
Mountains detachment fault (Mesozoic to
Precambrian)

34°

 

Contact
——I—§—Fault—Dotted where concealed. Bar and ball on
downthrown side; arrows Show relative movement

A A—A Thrust or detachment fault—Dashed where concealed.
Queried where location is poorly controlled

' — ' — ‘ Prominent aeromagnetic lineament

 

Edge of Mojave-Sonoran Belt—Dashed where very
approximate

Western edge of eastern Mojave “aseismic” area

 

@ Magnetic contours—Showing total intensity magnetic field
725 of the Earth in gammas relative to arbitrary datum.
Hachures indicate closed areas of lower magnetic inten —

sity. Contour interval 25 gammas

Palo Ve'rde
Izaar

I7 ,»’
Acolita
2 7 l-

 

 

 

 

3 a
116° ' ,. . . .\
Base by US. Geological Survey, 1:500 000 114° 113303
Needles, 1956—62, Phoenix, 1954—69, SCALE 1:500 000
Prescott, 1954452, Salton Sea, 1959_57 1'0 0 10 20 30 In California contours are interpolated from resrdual map prepared by Gordon D, Bath
; . | . | . . . : 4‘0 5'0 MILES US Geological Survey from OpenAFile Report 75—52 by US. Geological Survey. In
10 O 10 Arizona contours are 2x enlargement from resrdual aeromagnetic map of Arizona ISauck
H H H 20 3O 4O 5O KILOM ETERS and Summer, IBTII, Arizona contours are resrdual + 400 gammas, Contours joined
I——-—' I—————I I CALIF . by W. J. Carr
CONTOUR INTERVAL 500 FEET
ARIZONA

NATIONAL GEODETIC VERTICAL DATUM OF 1929

I990 MAGNETIC DECLINATION VARIES FROM 13°OU' EASTERLY FOR THE SOUTHEASTERN CORNER TO
13°30’ EASTERLY FOR THE NORTHWESTERN CORNER. MEAN ANNUAL CHANGE IS 0°04' WESTERLY r‘

MAP LOCATION

GENERALIZED REGIONAL GEOLOGIC AND STRUCTURAL UNIT MAP AND RESIDUAL AEROMAGNETIC MAP
OF PART OF SOUTHEASTERN CALIFORNIA AND WESTERN ARIZONA

 

DEPARTMENT OF THE INTERIOR

U.S. GEOLOGICAL SURVEY

34°
00’

115°00’

Base by US Geological Survey, 1:500 000
Needles, 1956—62, Phoenix 1954—69,
Prescott, 1954452, Salton Sea, 1959—87

fill/197”?

' gton Mine /\"

8H 0

./
‘ «a
../ asy-

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2

./

I . \ \ I\.

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Ruins. \

> §/"“’” 24?“ ”"f

Ill/h 1' 17 pl

lJunct'On In\ I
plan arantine tti )

Vid I Junction
920
Tbo

.....

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_.r'

,,,,,,,,,,

vvvvvv

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I

114°45'

114°30’

SCALE 1:125 000
2 O 2 4 6 8 MILES
’ ' I

2 O 2 4 6 8 KILOMETERS
I——I I-—I P A ,

TRUE NORTH

CONTOUR INTERVAL 200 FEET
APPROX'MATE MEAN WITH SUPPLEMENTARY CONTOURS AT 100 FOOT INTERVALS
NATIONAL GEODETIC VERTICAL DATUM OF 1929

TECTONIC MAP, VIDAL-PARKER REGION, CALIFORNIA AND ARIZONA

114°15’

 

MAP LOCATION

34°

59 ,
CA 6US¢§ PIAIN; /

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é; IWJZ

."

114°00’

Geology by W.J. Iarr, DD. Dickey, and
WD. fluinlivan, “74—1977

OE
75'
P4

V. I 9’30

PROFESSIONAL PAPER 1430
PLATE 4

QUATERNARY
AND TERTIARY

TERTIARY

MESOZOIC

MESOZOIC TO
PRECAMBRIAN

 

DESCRIPTION OF MAP UNITS

 

 

QTa Alluvium and Colorado River deposits (Quaternary and

 

 

 

Tertiary)

Bouse Formation, Fanglomerate of Osborne Wash, and
associated volcanic rocks (Tertiary)

Volcanic and sedimentary rocks undifferentiated
(Tertiary)

Granitic rocks (Mesozoic)

Gneissic granitic rocks (Mesozoic)

Metamorphic rocks of the upper plate of the Whipple
Mountains detachment fault (Mesozoic to
Precambrian)

Area of abundant intrusive rocks in the lower plate of
the Whipple Mountains detachment fault

_ (Mesozoic to Precambrian)

Metamorphic rocks of the lower plate of the Whipple

Mountains detachment fault (Mesozoic to

Precambrian)

 

Contact

:13— FauIt—Showing dip. Probable significant lateral displace—
30 ment shown by arrows Bar and ball on downthrown
35 side Dotted where concealed, queried where doubtful

ALL Thrust fault—Showing dip. Sawteeth on upper plate

T Whipple Mountains detachment fault—Showing dipr
Dotted where concealed, queried where doubtful

—:Io— Syncline—Showing approximate trace of axial plane
‘—I-—— Anticline—Showing approximate trace of axial plane

50 Strike and dip of beds or flow layering

—'— Inclined
—l— Vertical
4— Attitude of foliation

NOTE: Owing to loss ofthe original compilation during report
processing, registry of geology with respect to topography
and culture is not precise, and this map contains un-
resolved errors in detail.

 

GE
75

P6

flu. I920

PROFESSIONAL PAPER 1430

PLATE 5
I13“
35"
MOho

  

 

 

‘ %

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

DEPARTMENT OF THE INTERIOR
U.S. GEOLOGICAL SURVEY

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

116“
I!

 

 

 

 

 

   

 

 

35

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

 

IMPERIAL
VALLEY .H

1140 ‘‘‘‘‘
50 MILES
I

40

20
I
50 KILOMETERS

I
I
30

CONTOUR INTERVAL 1000 FEET

GENERALIZED TOPOGRAPHY OF PART OF SOUTHEASTERN CALIFORNIA AND WESTERN ARIZONA

O~—O

 

TRUE NORTH

APPROXIMATE MEAN
DECLINATION, 1972