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Precambrian, Eocambrian, and Cambrian rocks of the Basin and Range Province of Eastern California

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Precambrian, Eocambrian, and Cambrian rocks of the Basin and Range Province of Eastern California

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Content PRECAMBRIAN, EOCAMBRIAN, AND CAMBRIAN ROCKS OF
(I
THE BASIN AND RANGE PROVINCE OP
EASTERN CALIFORNIA
by
Harry M. Quinn
A Thesis Presented to the
FACULTY OF THE GRADUATE SCHOOL
UNIVERSITY OF SOUTHERN CALIFORNIA
In Partial Fulfillment of the
Requirements for the Degree
MASTER OF SCIENCE
(Geology)
September, 1968
UMI Number: EP58567
All rights reserved
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UMI EP58567
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U N IV E R S IT Y O F S O U T H E R N C A LIF O R N IA
T H E G R A D U A TE SCHO O L
U N IV E R S IT Y PARK
LOS A N G E LE S , C A L IF O R N IA 9 0 0 0 7
1 ms tnesis, written oy
........ M R M . . M . . Q U I M ...............
under the direction of h.Xs..Thesis Committee,
and approved by all its members, has been pre
sented to and accepted by the Dean of The
Graduate School, in partial fulfillment of the
requirements for the degree of
Master. o..f...S.Q.iexiee....(Geol.g.gy.)
D a te Au3USt_l_968
IIS C0MMITTEE
C h i man
TABLE OP CONTENTS
PAGE
ILLUSTRATIONS ....................................
ABSTRACT............................... 1
INTRODUCTION .................................... 3
Location . • • . ........... . ............ 3
Geography and blimate ...... ............ 5
Vegetation . . ............................. 5
Method of Investigation ..................... 6
Presentation ............. 7
Acknowledgments ................ 7
THE CAMBRIAN BOUNDARY ........................... 8
WHITE AND INYO MOUNTAINS . ................... 11
Introduction............... 11
Stratigraphy and paleontology ............... 18
Precambrian Rocks . ..................... 18
9
Wyman Formation • • . • ............ 18
Paleozoic Rocks ......................... 19
Eocambrian System ................ 19
Reed Dolomite....................... 19
Deep Springs Formation ............. 20
Eocambrian and Cambrian System ........ 26
Campito Formation ................... 26
r
Cambrian System......................... 28
Poleta Formation .......... 28
iii
PAGE
Harkless Formation ................. 36
Saline Valley Formation ............. 38
Mule Springs Formation ............. 39
Monola Formation ............ 40
SOUTHERN PANAMINT RANGE ......................... 41
Introduction ................. ....... 41
Stratigraphy and paleontology ............... 46
PreCambrian Rocks ....................... 46
Crystalline Basement •••••••• 46
Pahrump Series ••••••••••• 46
Paleozoic Rocks ................... 47
Eocambrian System.................. 47
Noonday Dolomite ................... 47
Johnnie Formation *.... ........ 47
Sterling Quartzite ........ .... 48
Eocambrian and Cambrian System ..... 50
Wood Canyon Formation ............... 50
Cambrian System ......................... 52
Zabriskie Quartzite . ............. 52
Carrara Formation . ............... 53
NOPAH AND RESTING SPRINGS RANGE................. 57
Introduction.............. 57
Stratigraphy and paleontology . . . ........ 59
Precambrian Rocks.......... 59
Crystalline Basement . ............. 59
iv
PAGE
Pahrump Series.............. 60
Paleozoic Rocks ......................... 60
Eocambrian System ....................... 60
Noonday Dolomite ................... 60
Johnnie Formation ................... 60
Sterling Quartzite ................. 61
Eocambrian and Cambrian System ........ 61
Wood Canyon Formation ............. 61
Cambrian System......................... 62
Zabriskie Quartzite ................. 62
Carrara Formation .......... • • • • 63
PROVIDENCE MOUNTAINS ........................... 67
Introduction . . . . ....................... 67
Stratigraphy and paleontology • ••••••• 69
Precambrian Rocks . . . . . ............ 69
Crystalline Basement . . . .......... 69
Paleozoic Rocks........... ............. 69
Eocambrian System .... ............ 69
Prospect Mountain Quartzite ........ 69
Cambrian System •••••• ............. 76
Carrara Formation . ................. 76
MARBLE MOUNTAINS............................... 81
Introduction ••••• ..................... 81
Stratigraphy and paleontology............... 85
Precambrian Rocks ..................... . 85
PAGE
Crystalline Basement ............... 85
Paleozoic Rocks................ 88
Eocambrian System ....................... 88
Prospect Mountain Quartzite .......... 88
Cambrian System ......................... 89
Carrara Formation................ . . 89
PROBABLE CORRELATIONS.......................... . 98
Introduction ........ 98
Correlations............................... 99
Crystalline Basement . . . .............. 99
Pahrump Series ......................... 99
Noonday Dolomite ••••• 100
Johnnie Formation . . . 103
Sterling Quartzite . ................ 105
Wood Canyon Formation .............. 107
Zabriskie Quartzite ..................... 110
Carrara Formation ....................... Ill
CONCLUSION...................................... 114
REFERENCES...................................... 118
APPENDIX........................................ 128
LIST OF ILLUSTRATIONS
FIGURE PAGE
1. Interbedded quartzitic sandstones and
limy shales in the lower member of the
Deep Springs Formation, near the Molly
Gibson Mine......................... 23
2. Ripple marks in fine-grained quartzitic
sandstones in the middle member of the
Deep Springs Formation, near the Molly
Gibson Mine . • . . ............ . • . 25
3. Limestone and shale interbeds in the
upper member of the Poleta Formation,
along the west side of Saline Valley
just northeast of area 3 ............... 31
4. Olose-up of a limestone interbed within
the upper member of the Poleta Formation
showing algal-like structures on the
weathered surface, along the west side
of Saline Valley just northeast of area 3 32
5. Tracks and trails in the upper member
of the Poleta Formation, along the west
side of Saline Valley just northeast of
area 3 33
6. Close-up of tracks and trails in the
upper member of the Poleta Formation . . 34
7. Upper member of the Poleta Formation
showing the uppermost limestone and
underlying quartzitic sandstone, along
the west side of Saline Valley just
northeast of area 3 ............. 35
8. Ripple marks in a thin-bedded, micaceous
shale of the lower Harkless Formation,
along the east side of Cedar Flat .... 37
9. Milky quartz veins and veinlets cutting
through phyllites in the Johnnie Forma
tion, near the head of Trail Canyon . . . 49
vi
vii
FIGURE PAGE
10. Contact between the Sterling Quartzite
and the Wood Canyon Formation, along
the north wall of Trail Canyon • • • • • 51
11. View north from Trail Canyon showing the
Wood Canyon Formation, Zabriskie Quartz
ite, Carrara Formation, and Bonanza
King Formation ........ ........ 55
12. West flank of the Resting Springs Range
just east of Shoshone, California, show
ing the Wood Canyon Formation, Zabriskie
Quartzite, Carrara Formation, and
Bonanza King Formation ................. 64
13. Outcrops of Prospect Mountain Quartzite,
Carrara Formation, and Bonanza King
Formation along the west side of
Providence Mountain ..... 70
14. Conglomerate bed at the base of Member B
of the Prospect Mountain Quartzite in the
northern Providence Mountains, near
South Hayden Wash....................... 73
15* Grit and pebble lense in Member B of the
Prospect Mountain Quartzite, near South
Hayden Wash ......................... 75
16. Girvanellid-bearing limestone in the
Chambless Member of the Carrara Forma
tion, near Cornfield Springs ...... 73
17. Ripple marked, fine-grained, micaceous
quartzitic sandstone in the Cadiz Member
of the Carrara Formation, near South
Hayden Wash ••••.••••. ........ 80
18. Paleozoic sedimentary sequence in the
Marble Mountains northeast of Chambless,
California, showing the Prospect
Mountain Quartzite, Carrara Formation,
and Bonanza King Formation ....... 86
19. Unconformity between the Precambrian
gneiss and the Prospect Mountain Quartz
ite, southern end of the Marble Mountains
just northeast of Cadiz, California . . . 87
viii
FIGURE PAGE
20. Interbedded shale and quartzitic sand
stone in the Latham Member of the
Carrara Formation, northeast of Cadiz,
California....................... 90
21. Algal limestone of the Chambless Member
(•Ccc) resting on shales of the Latham
Member (-Cel) of the Carrara Formation,
northeast of Cadiz, California ......... 92
22. Girvanella sp. in the Chambless Member
of the Carrara Formation, northeast of
Cadiz, California • ................ .. . 93
23. Characteristic nodular weathering of the
upper part of the Chambless Member of
the Carrara Formation, northeast of
Cadiz, California....................... 94
24. Paleozoic sedimentary sequence in the
Marble Mountains just, northeast of Cadiz,
California, showing the Precambrian
gneiss, Prospect Mountain Quartzite, and
Carrara Formation ..................... .. 96
25. Cross-bedding on weathered surface of Sub
member B, Cadiz Member of the Carrara
Formation, northeast of Cadiz, Cali
fornia ............................... 97
ix
PLATE PAGE
I. Location Ma p ............................ 4
II. Westgard Pass Areas, White Mountains . . 12
III. White Mountains Area 1 ................. 14
IV. White Mountains Area 2 . . ............. 15
V. White Mountains Area 3 . . . . ......... 17
VI. Trail Canyon Area ........... • • • • • 44
VII. Location of Trail Canyon A r e a ......... 45
VIII. Nopah-Resting Springs Ranges ........... 58
IX. Providence Mountains Areas of Study . . 68
X. South Hayden Wash Area................. 71
XI. Marble Mountain Areas of Study......... 82
XII. South Marble Mountain Area............. 84
XIII. Correlation Chart ..................... 114
XIV. White Mountain Area Lower Cambrian
fauna 1 129
XV. White Mountain Area Lower Cambrian
fauna 2 ........................... 131
ABSTRACT
In eastern California there is a sequence of non-
fossiliferous rocks exhibiting a stratigraphic continuity
upward into rocks of Early Cambrian age. The sequence,
which has previously been assigned to a Late Precambrian
age, is herein assigned to the Eocambrian System of Early
Paleozoic age. This assignment permits the distinction
of the nonfossiliferous sequence from Precambrian meta
sediments, unconformably subjacent, and from the fossili-
ferous Lower Cambrian rocks gradationally superimposed.
Within eastern California, Late Precambrian
through Cambrian structural features and facies patterns
have resulted in conflicting correlations of the rock
units of these ages. As an effort toward resolving this
problem the writer examined Precambrian through Cambrian
outcrops at the White and Inyo Mountains, the southern
Panamint Range, the Wopah and Resting Springs Ranges, the
Providence Mountains, and the Marble Mountains. On the
basis of field relationships, laboratory and paleontologi
cal study, and a critical review of the literature, the
following formational correlations are indicated:
The Pahrump Series is correlated northward with
the Wyman Formation.
The Woonday Dolomite is correlated northward with
the Reed Dolomite.
The Johnnie Formation is correlated northward with
the Deep Springs formation.
The Sterling Quartzite is correlated northward with
the Andrews Mountain Member of the Campito Forma
tion.
The Wood Canyon Formation is correlated northward
with the Montenegro Member of Campito Formation,
the Poleta Formation, and the lower Harkless
Formation and easterly and southerly with portions
of the Prospect Mountain Quartzite.
The Zabriskie Quartzite is correlated northward
with the middle and upper Harkless Formation and
southerly and easterly with the upper Prospect
Mountain Quartzite.
1
2
The Carrara Formation is correlated northward with
the uppermost Harkless, Saline Valley, Mule
Springs and Monola Formations,
INTRODUCTION
Location
Five regions containing Precambrian and Cambrian
outcrops are examined as a means of obtaining a better
\ ( ? s Q ~
knowledge of the stratigraphy and paleontology of this
strata. This knowledge is needed in order to evaluate
some of the existing correlations between units of these
strata. These five regions are in eastern California and
closely parallel to the California-Nevada border. The
northernmost region (PI. I, No. 1) is in the White and
Inyo Mountains. These mountains are located along the
east side of Owens Valley near Big Pine, California.
Death Valley National Monument contains the next region
of study. This region (PI. I, No. 2) is situated in the
southern Panamint Range, along the west side of Death
Valley. The third region (PI. I, No. 3) includes portions
of the Nopah and Resting Springs Ranges and lies near the
California-Nevada border, just east of Shoshone, Cali
fornia. Just east of Kelso, California, is the fourth
region of study (PI. I, No. 4). This region is located
along the west flank of the Providence Mountains. The
southernmost region studied (PI. I, No. 5) is in the
Marble Mountains near Chambless, California.
3
Bishop
LOCATION MAP
1 W h ite -ln v o
\ Mountains
Pine
Death
Valley
National
Monument
Hwy
6 & 395
Area \
Shown
Enlarged
Nopah-
v R* stin q \
\ Springs Ranges
Hwy '
91 & 466
Mojave
Hwy 466
B arsto w
4 Providence Mountains
Hwy
395
Needles
Hwy. 66
5 Marble M ountains
Los Angeles
’ T^jj-r-rrn-rm
Joshua Tree National
Riverside
Monument
■Hwy. 60
ARIZONA
Pacific
Scale In M iles
Ocean
- r
CALI FORNI A
MEXICO
Plate
5
Geography and Climate
These five regions of study are all within the
Basin and Range Geomorphic Province of eastern California
(Oakeshott, 1964, pp. 24-25). The Basin and Range
province contains a series of nearly north-south trending
mountain blocks and intermontane valleys. Elevations
within the portions of the province studied vary from
more than 200 feet below sea level in Death Valley to over
14,000 feet above sea level in the White Mountains.
Precipitation varies from less than 2 inches a
year at the lower elevations to over 10 inches a year at
the higher elevations. Due to the low rates of precipita
tion and high summer temperatures, most of the Basin and
Range province has an arid to semi-arid climate.
Vegetation
Desert areas contain numerous playas and sand
dunes. Vegetation in these areas consists mainly of salt
brush, grasses, cacti, and creosote bushes with some
mesquite and willow bushes growing in the moist areas and
near springs.
Areas of intermediate elevation receive more
precipitation than most of the lower areas and support a
more abundant diverse flora. These areas are commonly
covered by grasses, sagebrush, junipers, and pinon pines.
6
Higher elevations receive even greater amounts of
precipitation and where elevations are not above timber
line, scattered groves of bristlecone pines are present.
Method of Investigation
The geology in the five study regions was examined
and sections were measured in each region. Field mapping
was conducted at four of the regions on enlarged topo
graphic maps; scale four inches to the mile.
Carbonate samples were separated into dolomites
and limestones by a selective staining process (Friedman,
1959)• Some carbonate samples were digested in acetic
acid and/or cut and polished. The acid residues and
polished surfaces were examined for microfossils, but none
was found. The polished surfaces of many samples revealed
the presence of ooliths which were not detected in the
field.
Shale samples were broken down by the kerosene
method and/or cut and polished. Most of the samples
examined were too silicified to break down but not silici-
fied enough to polish. The few samples which did break
down or could be polished were examined under a binocular
microscope, but, again, no microfossils were found. Where
possible, megafossils were collected and studied, but
their aid in paleontologic control and in correlating the
regions studied was not as useful as had been hoped.
7
Presentation
The five regions examined are presented as indivi
dual sections and the proposed correlations between rocks
in these regions are presented in a separate section fol
lowing them. Metasedimentary and crystalline rocks, which
are in sedimentary contact with overlying strata, are
herein referred to the Precambrian System. Non
metamorphosed or slightly metamorphosed sedimentary rocks
occurring below the base of the Olenellus zone and which
are in sedimentary contact with underlying metasediments
or crystalline rocks are placed in the Eocambrian System
by the writer. All rocks occurring above the base of the
Olenellus zone are herein referred to the Cambrian System.
Acknowledgments
The writer wishes to express his appreciation to
the members of his committee, Dr. William H. Easton, Dr.
Orville L. Bandy, and Dr. Gregory A. Davis, of the
University of Southern California, for their guidance and
critical reading of the manuscript. The writer is in
debted to Mr. William Bradford, Mr. Steve Wolf, and Mr.
Russell Quinn for the assistance they rendered in the
field. Indebtedness is also due Texaco, Inc. for as
sistance with drafting and reproductions, Miss Margo
McDougall and Mr. Philip Patton for their reading of the
8
manuscript, and to the writer1s wife for her constant
encouragement throughout the problem.
THE CAMBRIAN BOUNDARY
In areas where a sequence of nonfossiliferous rocks
exhibits stratigraphic continuity upward into rocks con
taining fossils of Lower Cambrian age, as in portions of
the Cordilleran miogeosyncline, there has been much dis
cussion on the positioning of the Lower Cambrian boundary.
Some investigators draw the base of the Cambrian in ac
cordance with the appearance of certain assemblages of
skeletal fossils, others employ lithologic criteria,
whereas some propose that a so-called historico-geological,
or tectonic method be used (Sk^eseth, 1963, p* 58; Rozanov,
1967, p. 432).
Brjzfgger (1900, from Skjeseth, 1963, p. 17) pro
posed the name f , Eo cambrian" for a sequence of non
fossiliferous rocks in Norway which demonstrate a gradual
transition upward into fossil-bearing Lower Cambrian
rocks. His term Eocambrian has still not gained wide ac
ceptance and some geologists refer to the Eocambrian
strata near the type section in Norway as the Sparagmite
series and consider it to be Precambrian in age (Vogt,
1924; Hernes, 1967). Skjeseth (1963, p. 36) refers to the
Eocambrian as a series within the Lower Cambrian System,
while Moore (1965, p. xxxii) considers the Eocambrian to
9
be a system within the Paleozoic Era.
Near the type area in Norway, the Eocambrian
section is composed mainly of quartzites, shales, sparag-
mites (felspathic quartzite), and tillites (Holtedahl,
1922; Skjeseth, 1963; B^rlykke, 1964). To the north,
near Spitsbergen, a stratigraphically equivalent sequence
of strata consists principally of quartzitic sandstones,
shales, carbonates, and tillites (Fleming and Edmon,
1941; Harland, Wallis, and Gayer, 1966).
Eocambrian rocks of eastern California are litho-
logically similar to those in Scandinavia and consist
mainly of quartzitic sandstones, shales, and carbonates.
They do, however, lack the sparagmites and tillites
present in the Scandinavian sequences. In both eastern
California and Scandinavia the Eocambrian strata grade
gradually upward into Lower Cambrian strata. The
Eocambrian strata of both areas contain tracks, trails,
possible algal remains, and Scolithus ? (Fleming and Ed-
mons, 1941; Skjeseth, 1963; B^rlykke, 1964).
The foregoing similarities have led the writer to
propose the use of the term Eocambrian for some non
metamorphosed or slightly metamorphosed sedimentary rocks
present in eastern California. These rocks unconformably
overlie metasedimentary or crystalline rocks and are
gradational into overlying Lower Cambrian rocks. The
writer also proposes that in the Cordilleran miogeo-
10
synclinal region skeletal fossil assemblages be used in
determining the Eocambrian-Cambrian boundary and that
tectonic and/or lithologic criteria be used as a means of
establishing the Precambrian-Paleozoic boundary. Such
methods appear to work well in establishing the
Precambrian-Paleozoic and Eocambrian-Cambrian boundaries
in the Precambrian through Cambrian rocks of eastern Cali
fornia and are used in this paper to establish these
boundaries.
Continuous sequences of nonfossiliferous rocks
which exhibit stratigraphic continuity upward into rocks
containing Lower Cambrian fossils are known elsewhere
around the world. One of the most publicized of these
sequences is in the Ediacara Hills area of South Australia
(Glaessner, 1958 and 1961; Glaessner and Daily, 1959). In
this area a large number of well preserved, soft bodied
fossil organisms have been found in a quartzitic sand
stone, about 500 feet below the lowest horizon containing
Cambrian fossils (Glaessner, 1961, p. 7). Lesser known
continuous sequences, which also contain soft bodied
organisms similar to those in the Ediacara Hills area, are
present in Southwest Africa and in England (Glaessner,
1961, p. 4-5). The writerfs proposed method for deter
mining the Precambrian-Eocambrian and Eocambrian-Cambrian
boundaries would appear to apply as well to the Ediacara
Hills area of South Australia as it does to the Cordil-
11
leran miogeosynclinal region of eastern California.
WHITE AND INYO MOUNTAINS
Introduction
Precambrian and Cambrian strata in the White and
Inyo Mountains are the northernmost outcrops of these
rocks to be found in eastern California. These mountains
contain approximately 13,000 feet of Eocambrian and
Cambrian strata and over 9,000 feet of Precambrian meta
sediments.
The White and Inyo Mountains are a south trending
range located in the Blanco Mountain, Waucoba Mountain,
and Independence quadrangles along the east side of Owens
Valley. Although essentially continuous, the range has
been separated at the pass east of Big Pine, California,
into the White Mountains to the north and the Inyo
Mountains to the south.
The main areas of study are in the vicinity of
Westgard Pass. This pass, located along the highway lead
ing from Big Pine to Deep Springs, California, is about
15 miles northeast of Big Pine (PI. I). Three areas were
mapped (PI. II) and, in all, 6,500 feet of section were
measured. Area 1 (PI. Ill), in the vicinity of Molly
Gibson Canyon, contains the lower portion of the section
measured. Area 2 (PI. IV) is located along the east side
of Cedar Flat and is where the upper portion of the_______
12
WESTGARD PASS
AREAS
AREA
P i . ne
Overlay for
T. 7 S. , R 35 E.
Blanco Mountain Quad.
Scale: h 6 2 5 0 0
Plate
eu Road
LEGEND FOR WHITE MOUNTAIN MAPS
Quaternary
13
o
: ytj. River and Terrace deposits
cambrian
Eh Harkle 2 3 Fo mation
Upper Po I0 ta Fornr,at ion, L1 mestone
ePc Upper Poleta Formation, ShaJe and Sandstone
OdB Upper poleta Formation, Shale
GpA Lower Poleta Formation
^ampito Formation, Montenegro Member
r,o cambrian
ec
Campito Formation, Andrews Min. Member
€ dE Upper Deep Springs Formation, Dolomite
CcU Upper Deep Springs Formation, Shale and
S and 3 to no
6 dm Middle Deep Springs Formation
GdB Lower* Deep Springs Formation, Submember B
GdA J Lower Deep Springs Formation, Submember A
Gr Reed Dolomite
G r £ r
Gr
Cca
GdA
Mollie Gibson
/M in e ^__ Sc’
GdA 6 r
Gr GdA
Qal
Cca
Gr
Gd m
GdD
•So'
Gd m GdD
Gca
GdE
\ Cca
/
Gca
U'
/D
Gca
c White Mtns,
Gca
Area I
Scale 1: I 56 2 D
P la te III
r ec
6cm
GpA
Qal
Qal
Qal
CpA
P l a t e IV
measured section was taken. Area 3 (PI* V) lies along
the west side of Deep Springs Valley and was examined for
additional stratigraphic and paleontologic information
about the lower portions of the Harkless Formation,
The areas of study are accessible by paved road
from Big Pine, and further access may be gained from dirt
roads and jeep trails. In order to supplement studies of
the Westgard Pass areas, reconnaissance trips were taken
into the areas of Wyman Canyon, Reed Flat, Black Mountain,
Papoose Flat, Harkless Flat, and Mule Springs to examine
formations not present in the study areas.
The Precambrian through Cambrian rocks of the
White and Inyo Mountains have previously been divided into
nine formations. The upper five were originally placed in
the Silver Peak Group by Turner (1902, pp. 264-265) with
the type locality near Silver Peak, Nevada. Walcott
(1908, pp. 167-230) followed Turner!s nomenclature in his
descriptions of Cambrian strata of the Inyo Mountains.
The boundaries of the Silver Peak Group were redefined and
three of the four remaining formations were named in a
report by Kirk (in Knopf, 1918, pp. 24-31). Maxson (1934,
pp. 310-311) included all olenellid-bearing strata as
part of the Silver Peak Group and added two formations
which were later merged into the one remaining formation.
The usage of Silver Peak Group has since been dropped in
favor of the present subdivisions proposed by Nelson
GpA/ * '
ecm-i
White Mtns.
Area 3
Scale 1 : 7273
Plate V
Qal
GpB
GpC
GpC
GpD
GpD
Gh
Gp B
GpD
r> C/' '
Qal t
GpC
Gh
• / G p C / GpB Qal ss
Gh
GpC /G p D
GpC
GpD / C h
GpD
GpC
GpD
GpC
GpC GpD
GpD
GpB GpD
GpD
Gh
18 !
!
(1962, pp. 139-144). Formational names presently accepted
by the U. S. Geological Survey, as well as descriptions of
i
their lithology and portions of their paleontology are
presented in the following pages.
Stratigraphy and Paleontology
PRECAMBRIAN ROCKS
Wyman Formation
The oldest sequence of rocks exposed in the White
Mountains is the Wyman Formation. The Wyman Formation
consists principally of thin-bedded, brown to black argil
lites, phyllites, and quartzites with some carbonate
interbeds. It was first named by Maxson (1934, pp. 310-
311) for exposures in and around Wyman Canyon. Maxson
originally described and named two formations differen
tiated by an unconformity. He placed all rocks below the
unconformity in the Roberts Formation and those above the
unconformity in the Wyman Formation. During a more
recent study of the area, Kelson (1962, p. 140) found no
evidence for such an unconformity and, since no major
lithologic changes occurred at this horizon, he placed all
of these metasedimentary rocks into what is now called the
Wyman Formation.
The Wyman Formation is not present in the areas
studied, and was only examined in reconnaissance. It is
19
assigned a maximum thickness of 9,000 feet with no base
having yet been found (Nelson, 1962, p. 140). The Wyman
Formation is overlain unconformably by the Reed Dolomite
(Maxson, 1934, p. 310 and 1935> P* 314; Nelson, 1962, p.
140).
PALEOZOIC ROCKS
EOCAMBRIAN SYSTEM
Reed Dolomite
The Reed Dolomite was first named by Kirk (in
Knopf, 1918, p. 24) for exposures at Reed Flat. Having a
thickness of approximately 2,900 feet (Maxson, 1934, p.
310) it rests unconformably on the Wyman Formation. This
unconformity is considered possibly to mark the
Precambrian-Cambrian boundary (Nelson and Perry, 1955* P*
1658). The upper contact is gradational, with the limy
dolomite of the upper Reed Formation grading into the
dolomitic limestone of the lower Deep Springs Formation.
This contact was arbitrarily chosen by the writer to be
at the horizon where carbonates yielded strong ef-
fervesence when tested with dilute hydrochloric acid.
At the type locality the Reed Dolomite is almost
entirely dolomite; the basal portion is usually oolitic
(Nelson, 1962, p. 140). The central part of the forma
tion becomes sandy and forms a northwest-tapering tongue
that attains a thickness of over 700 feet southeast of the
type locality. At Reed Plat this unit varies from zero to
a few feet in thickness (Nelson, 1962, p. 140).
Only the upper portion of the Reed Dolomite was
examined in detail by the writer; the remainder was
studied by reconnaissance. The upper portion consists of
350 feet of white to cream colored, massive to thin-
bedded dolomite with the upper 50 feet being predominantly
thin-bedded. This upper dolomite contains numerous red to
red-brown patches and some unusual square and round to
elliptical structures. No definite fossil remains were
found in the Reed Dolomite, but some of the round to
elliptical structures suggest a possible organic origin
of some kind. These structures range in size from 2 to
6 mm across and appear ovoid in shape. They are composed
of a translucent, coarse crystalline dolomite and are
held in a cream colored, fine-grained dolomite. Question
able metazoan remains have been reported from the upper
portion of the Reed Dolomite (Taylor, 1966, p. 54), but
nothing resembling their description was found in the
present investigation.
Deep Springs Formation
The Deep Springs Formation was named by Kirk (in
Knopf, 1918, p. 24) for exposures on the west side of Deep
Springs Valley near Molly Gibson Canyon. It consists
21
principally of dolomitic limestones, quartzitic sand
stones, and dolomites with some shales and siltstones.
All units within the Deep Springs Formation appear
conformable with one another, and the formation is con
formable with the underlying Reed Dolomite, The contact
with overlying Campito Formation was reported to be un-
conformable (Maxson, 1935* P- 314) > but no evidence for
an unconformity was found in the area (Area 1) studied by
the writer, although some local evidence of erosion along
the contact between these two formations exists in out
crops to the east of this area. Nelson (1962, p. 141)
considers the contacts between the Deep Springs Formation
and Campito Formation to be conformable.
The Deep Springs Formation consists basically of
five lithologic divisions, three carbonate sequences
separated by two quartzitic sandstone sequences, and has
been divided into three members by Nelson (1962, p. 141).
The lower member is principally a dolomitic limestone
with some dolomite, quartzitic sandstone, shale, and
sandy limestone. This member has been subdivided into two
submembers by the writer. The lower submember, submember
A, consists of 400 feet of dolomitic limestone, quartzitic
sandstone, and shale. The lowermost 300 feet is mainly a
thin- to medium-bedded, fine-grained, dolomitic limestone
which weathers gray-blue and contains some tan to brown
weathering sandy lenses. The upper 100 feet of A is a
22
sequence of limy shales, fine- to medium-grained, mica
ceous, quartzitic sandstones, and sandy dolomitic lime
stones. The upper sandy carbonate portion weathers tan-
gray to brown.
Submember B has a thickness of 230 feet and is com
posed mainly of dolomitic limestone and sandy limestone
with minor amounts of shale and quartzitic sandstone. The
basal 60 feet is a fine-grained, light blue-gray, dolomitic
limestone which weathers pale blue-gray with white flecks.
This unit is quite resistant and is used as the dividing
point between submembers A and B because of its easily
recognized color and cliff forming habit.
The next 100 feet is predominantly sandy, dolomitic
limestone with thin interbeds of limy quartzitic sand
stones and shales. This sandy, dolomitic limestone is set
apart from the lower portion by a ten foot bed of fine
grained, cross-bedded, quartzitic sandstone containing
numerous thin shaly interbeds (Pig. 1). The lower 30 feet
of the overlying portion is oolitic and consists of medium
gray-brown to brown sandy dolomite oolites held in a gray
dolomitic limestone. This oolitic, dolomitic limestone
contains pyrite throughout and euhedral magnetite in the
upper part. The entire unit, except for a few quartzitic
sandstones and some shales, weathers mottled gray and
yellow-brown.
Overlying this dolomitic unit is a 40-foot sequence
23
Figure 1.— Tnterbedded quartzitic
sandstones and limy shales in the
lower member of the Deep Springs
Formation, near the Molly Gibson
Mine.
24 j
of interbedded dolomitic limestone, shale, and quartzitic j
!
sandstone. The upper 15 feet is a fine- to medium-grained,j
cross-bedded micaceous, quartzitic sandstone. Immediately j
i
below this quartzitic sandstone is a 3 foot bed of mottled j
gray and yellowish-brown weathering limestone which con- |
i
tains euhedral magnetite and minor amounts of pyrite. j
The top 30 feet of submember B is gray to tan,
coarse-grained, limy dolomite which weathers tan-gray with
local brown-gray patches and has a sandy appearance,
Quartzitic sandstones comprise the principal part
of the middle member of Nelson. The member has a thick
ness of 470 feet with the upper portion consisting mainly
of carbonates. The lower 275 feet is principally a
medium- to coarse-grained, micaceous, quartzitic sandstone
and limy sandstone. Most of the quartzitic sandstones are
cross-bedded with many of the fine-grained, micaceous,
quartzitic sandstone beds exhibiting ripple marks along
partings (Fig. 2). The unit weathers gray-brown to dark
brown with the limy areas weathering yellow- to red-brown.
The upper 195 feet is a dolomitic limestone and
limy dolomite sequence, locally containing sandy lenses
and some oolitic lenses. The sequence weathers pale blue-
gray with the sandy areas yellow-brown and the oolitic
areas mottled blue-gray and yellow-brown.
The upper member consists of 450 feet of quartzitic
sandstone, micaceous shale, and dolomite. The lower 110
25
Figure 2.— Ripple marks in fine
grained quartzitic sandstones in
the middle member of the Deep
Springs Formation, near the Molly
Gibson Mine.
feet is medium-grained, micaceous, quartzitic sandstone
which is commonly cross-bedded and contains thin lenses
of shale.
The next 120 feet is principally micaceous shales
i with some lenses of fine- to medium-grained, micaceous
sandstones. Many of the shales show ripple markings and
some exhibit tracks and trails along partings. Cloud and
Nelson (1966, p. 767) report the presence of Pteridinium
sp. from this horizon. The upper 10 feet of this sequence
is a limy shale which weathers tan to tan-green.
The upper 220 feet of this member consists of a
medium-grained dolomite with some lenses of dolomitic
limestone and oolitic limy dolomite. It weathers a pale
blue-gray with occasional yellow-brown areas and some
mottled blue-gray and yellow-brown areas where it is
oolitic.
EOCAMBRIAN AND CAMBRIAN SYSTEMS
Campito Formation
The Campito Formation was originally named by Kirk
(in Knopf, 1918, p. 27) but its boundaries have since been
redefined by Nelson (1962, p. 141). It is 3,500 feet
thick and consists principally of dark gray-brown to
black, fine- to medium-grained, quartzitic sandstones with
interbedded gray-green to green-brown shales and silt-
stones. The shales and siltstones progressively increase
upward and become the predominant lithology in the upper
most 600 to 800 feet* This lithology change is used by |
Nelson (1962, p* 141) to split the Campito Formation into |
two members* The lower quartzitic sandstone portion is j
called the Andrews Mountain Member and the upper shaly |
portion, the Montenegro Member. j
1
The Campito Formation rests conformably on the Deep
Springs Formation and is gradational into the overlying
I
Poleta Formation* It contains the lowest occurrence of
trilobites, as well as the first archaeocyathids to be
found in the Paleozoic sediments of eastern California*
The Andrews Mountain Member consists of cross
bedded, fine- to medium-grained, quartzitic sandstone with
numerous thin shale and siltstone interbeds. Shales and
siltstones of the upper part of the Andrews Mountain
Member contain the first definite metazoan remains to be
found in the White and Inyo Mountain areas. Present in
this upper portion are the trilobite Fallotaspis sp., some
Scolithus tubes, and some tracks and trails.
The Montenegro Member is principally shales and
siltstones with numerous thin interbeds of fine- to
medium-grained, micaceous, quartzitic sandstones and a few
interbedded archaeocyathid-bearing limestones near the
top. This upper member shows a greater diversity in fauna
than the lower member. In addition to the fauna present
in the Andrews Mountain Member, the Montenegro Member
28 |
contains the trilobites Nevadia sp. and Holmia sp. as well j
as the lowest occurrence of carbonates containing archaeo
cyathids. Trilobite faunas are largely confined to the
siltstones and shales with only a few fragments being j
found in the quartzitic sandstones and limestones.
i
CAMBRIAN SYSTEM j
|
Poleta Formation
The Poleta Formation was named by Nelson (1962,
p. 141) for exposures along the west side of Payson Can
yon. It consists of a 1,000 to 1,200-foot succession of
limestones, shales, and quartzitic sandstones. The Poleta
Formation rests conformably upon the Montenegro Member of
the Campito Formation and is in turn overlain conformably
by the Harkless Formation.
The Poleta Formation has been divided into two
members by Nelson (1962, p. 141). The lower member is a
550- to 600-foot thick archaeocyathid-bearing limestone
which is resistant to weathering and is a prominent ridge
formerly along the east side of Cedar Flat. This lime
stone weathers cream to buff color at the top and base and
is blue-gray to light blue-gray in the center. Archaeo
cyathids (PI. XIV, Fig. 7) are common throughout this
member and are locally found in patches. Two forms
reportedly present in this lower limestone member are
Ajacic.yathus nevadensis (Okulitch) and Ethmophyllum________
29!
!
whitney (Meek) (Pesci, et al•, 1955, p. 196; McKee and |
Moiola, 1962, p. 534). A few trilobite fragments were |
!
found in the basal portions of this member and some pos- !
i
sible cystoid plates were seen in the extreme upper part.
The upper member is a 600- to 650-foot sequence of j
|
quartzitic sandstone, micaceous shale, and limestone. The
lower 350 to 400 feet of this member consists of green to
tan shales and siltstones with interbedded quartzitic
sandstones and archaeocyathid-bearing limestones. It
contains three trilobite zones with the lower one
characterized by Nevadella cf, N. gracile (Walcott) (PI.
XV, Pig. 1). Nevadella sp. is the only trilobite found in
this zone and it occurs there with two classes of
echinoderms (Durham, 1967, p. 98)* Although two classes
of echinoderms, the Helicoplacoidea and the Eocrinoidea
are said to be present, only examples of the Helicopla
coidea were found by the writer. These, three in all,
belong to the genus Helicoplacus sp. (PI. XV, Pig. 2).
Trilobite fragments and echihoderm plates are very
abundant on some bedding planes and in some areas form a
' ’fossil hash.”
About 300 feet above the Nevadella zone is a tan to
gray, thin, platy, calcareous shale. This shale contains
numerous trilobite fragments and is located between two
blue-gray limestones which contain a few randomly
scattered archaeocyathid remains. This zone is character-
3° |
ized by the presence of Fremontia sp, (PI, XIV, Fig. 3), !
i
Bonnla (?) sp. (PI. XIV, Pig. 4), and Onchocephalus (?) sp.j
(PI. XIV, Pig. 5).
I
!
Zone three is about 40 feet stratigraphically above j
: the Fremontia-Bonnia zone and is characterized by the j
t
presence of Fremontia sp. This zone is a 20- to 30-foot
section of gray-green to tan shale in which only this one
trilobite genus was found.
I
Overlying this shale is 100 to 150 feet of dark I
brown weathering quartzitic sandstone with a few thin
interbeds of siltstone, shale, and limestone (Fig, 3). The
interbedded shales and siltstones contain a few trilobite
fragments, and the limestones exhibit some algal-like
structures on the weathered surface (Fig. 4). The
quartzitic sandstones contain Scolithus tubes and locally
abundant tracks and trails (Figs. 5 and 6).
The uppermost 150 to 200 feet is a resistant
weathering limestone containing a few archaeocyathid
remains (Fig. 7). This member looks very much like
Member A, as it also weathers buff to tan at the top and
base, where it is silty and has a blue-gray weathering
central area. Although resembling Member A, it is dis
tinguishable because it is thinner and lacks the abundant
archaeocyathid remains common to A.
31
Figure 3.— Limestone and shale interbeds
in the upper member of the Poleta Forma
tion, along the west side of Saline Valley
just northeast of area 3.
32
Figure 4.— Close-up of a limestone inter-
bed within the upper member of the Poleta
Formation showing algal-like structures
on the weathered surface, along the west
side of Saline Valley just northeast of
area 3.
33
Figure 5.— Tracks and trails in the upper
member of the Poleta Formation, along the
west side of Saline Valley just north
east of area 3.
34
Figure 6.— Close-up of tracks and trails
in the upper member of the Poleta Forma
tion; note crossing of trails near the
point of the pick.
35
Figure 7.— Upper member of the Poleta
Formation showing the uppermost lime
stone and underlying quartzitic sand
stone, along the west side of Saline
Valley just northeast of area 3.
I
Harkless Formation
The Harkless Formation was named by Nelson (1962,
| p. 142) for exposures in the area of Harkless Flat. At
its type locality it is mainly shales and siltstones with
some interbeds of thin-bedded, fine- to medium-grained
quartzitic sandstones. The quartzitic sandstones increase
eastward and become the predominant lithology in the
vicinity of Waucoba Springs (Nelson, 1962, p. 142; Ross,
1965, pp. 11-12). The Harkless Formation rests conform
ably on the underlying Poleta Formation and is in turn
overlain conformably by the Saline Valley Formation
(Nelson, 1962, p. 142).
The quartzitic sandstones contain abundant
Scolithus tubes, and the shales and siltstones exhibit
ripple marks (Fig. 8) and some tracks and trails (Ross,
1965, pp. 11-12). The Harkless Formation has a maximum
thickness of 2,000 feet (Nelson, 1962, p. 142) with only
the lower 450 to 500 feet present in the areas studied.
The portion studied consists principally of shales and
siltstones with some thin lenses of fine- to medium-
grained, micaceous, quartzitic sandstones and a few thin
limestone lenses. The limestones are normally oolitic,
pisolitic, and archaeocyathid-bearing. Some of the
pisolitic ones exhibit structures suggestive of an algal
origin (PI. XIV, Fig. 6).
37
Figure 8.— Ripple marks in a thin-bedded,
micaceous shale of the lower Harkless
Formation, along the east side of Cedar
Flat.
38
Within area 3 (PI. V) are some 1- to 2-foot thick
beds of archaeocyathid-bearing limestone which weather
|
mottled dirty green and tan. These limestone lenses con
tain a number of archaeocyathids, many of which are
greater than 20 mm in diameter. McKee and Moiola (1962,
p. 535) report the presence of Archaeocyathus sp. and
Oambrocyathus sp. from limestone lenses in the lower part
of the Harkless Formation in Esmeralda County, Nevada.
In addition to archaeocyathids, two trilobite
localities were found in the lower part of the Harkless
Formation, within area 3 (PI. V) and both of these pro
duced only specimens of Paedeumias nevadensis Walcott.
Saline Valley Formation
The Saline Valley Formation is a highly variable
and lenticular sequence of quartzitic sandstones, shales,
and sandy limestones with a combined thickness of 800 to
850 feet (Nelson, 1962, p. 142; Ross, 1965> pp. 12-14).
It was named by Nelson (1962, p. 142) for exposures in the
northwestern part of Saline Valley near Waucoba Springs.
The Saline Valley Formation is in conformable contact with
both the underlying Harkless Formation and the overlying
Mule Springs Formation and contains a fauna which is
indicative of an early Cambrian age (Nelson, 1962, p. 142;
Ross, 1965> p. 12).
The Saline Valley Formation does not crop out in the
39
areas studied (PI. II) and was only examined on a recon
naissance trip into the northern Inyo Mountains where a
few fragments of Ogygopsis sp. were found in a micaceous
shale near the road leading into Papoose Flat. Nelson
(1963, p. 245) reports the presence of Ogygopsis sp. in
this formation, along with Olenellus sp. and Bonnia sp.
In addition to these trilobites, McKee and Moiola (1962,
p. 535) report Ptychoparia sp., Syspacephalus sp.,
Onchocephalus sp., and Salterella sp. from similar strata
in Nevada.
Mule Springs Formation
The Mule Springs Formation was named by Nelson
(1962, p. 142) for exposures near Mule Springs, ;)ust south
east of Big Pine, California. The formation is mainly a
girvanellid-bearing limestone with minor shaly interbeds
and has a thickness of 1,000 feet (Nelson, 1962, p. 142;
Ross, 1965> PP* 14-15). It is not present in the areas
studied and was examined only on reconnaissance trips
into the Papoose Flat area and Mule Springs area. The
Mule Springs Formation contains the uppermost olenellid-
bearing strata and is conformable with the underlying
Saline Valley Formation and the overlying Monola Forma
tion (Nelson, 1962, p. 142; Ross, 1965, pp. 14-15).
Monola Formation
The Monola Formation received its name from Nelson
(1963, pp. 29-33) and consists of a sequence of inter
bedded siltstones, shales, and limestones. It has a
thickness of around 1,200 feet and is conformable with the
underlying Mule Springs Formation and the overlying
Bonanza King Formation (Nelson, 1963, pp. 30-31; Ross,
1965, PP. 16-17). This formation is assigned a Middle
Cambrian age on the basis of its contained fauna (Nelson,
1963, pp. 31-32; Ross, 1965, pp. 16-17). The Monola
Formation is not present in this study area and also was
examined only on a reconnaissance trip into the area of
Papoose Flat.
At the type locality, the Monola Formation has been
subdivided into three members by Nelson (1963, pp. 31-32).
The lowest member consists of a 600-foot succession of
shales, siltstones, limy shales, and limestones. This
member contains the trilobites Alokistocare sp.,
Oryotocephalus sp., and Syspacephalus sp. (Nelson, 1963,
p. 32). The middle member is a 115-foot section of thin-
bedded limestones with some intercalated siltstones and
shales. The limestones within this member contain
Girvanella sp. (Nelson, 1963, p. 31). The uppermost
member consists of 425 feet of interbedded limestones,
siltstones, and shales and contains the trilobites
41 '
Alokistocare sp., Ogygopsis klotzl (Rominger), and
Sonoraspls nelson! Stoyanow (Nelson, 1963, p. 31).
In the northern part of the Inyo Mountains, the
Monola Formation has been divided into four members by
Ross (1965, p. 16) with his lowermost member a brown to
red-brown weathering shale and gray weathering siltstone
sequence having a maximum thickness of 350 feet. Over-
lying this is a 320-foot sequence consisting mainly of
red-brown weathering siltstone with numerous thin lime
stone interbeds. Above this sequence is a third member
which has a thickness of 330 feet and is a shale and
siltstone sequence similar to the lowermost member. The
upper 250 feet is a gray to blue-gray limestone with
shaly interbeds and is overlain by the Bonanza King Dolo
mite .
SOUTHERN PANAMINT RANGE
Introduction
Precambrian and Cambrian strata of the southern
Panamint Range comprise the westernmost continuous
sequence to be found in the central part of eastern Cali
fornia. Outcrops of these strata are mainly confined to
the eastern slope of the range with only isolated out
crops of the lower portion of the sequence present along
the western side. The range is essentially a north-south
trending range, which separates Panamint Valley to the j
!
west from Death Valley to the east. The Panamint Range is |
i
located within the Emigrant Canyon, Furnace Creek, and j
Telescope Peak quadrangles. Elevations within the range
vary from a few hundred feet above sea level to over
11,000 feet. |
|
The area closely examined by the writer is along
the north side of Trail Canyon (PI. VI). This canyon is
located on the east flank of the range, about 15 miles
southwest of the Furnace Creek Inn (PI. VII). It is
accessible by the Trail Canyon Jeep Road which intersects
Bennett's Well Road Just west of the Devils Golf Course.
Previous geologic work in the southern Panamint
Range has been concerned principally with the economics
and structure of the area rather than with the stratigraphy
or paleontology. Reconnaissance studies of this area were
conducted by Gilbert (1875) and Spurr (1908), but detailed
stratigraphic studies came sometime later. Portions of
this range have been mapped by Murphy (1932), Hopper
(194-7)* and Johnson (1957), and regional mapping of the
range has been done by Noble and Wright (1954), Jennings
(1958), Bates (1965) and Hunt and Mabey (1966).
Outcrop thicknesses of Precambrian and Cambrian
metasedimentary and sedimentary rocks of the southern
Panamint Range vary considerably. The main cause for this
variation appears to be faulting, although some strati-
Qal
G b
ec
€ z
G w
" i
€ s |
4 >
LEGEND FOR TRAIL CANYON NAP
Quaternary
River and Terrace Deposits
Cambrian
Bonanza King Formation
Carrara Formation
Zabriskie Quartzite
Wood Canyon Formation
Eocambrian
Sterling Quartzite
Johnnie Formation
Plate Va
44
Gb
54
52'
Gw
Qa
Gw
So# X \
50°'
Gs
47
Gj
" /
Gj
L
Trail Canyon
Area
Scale 1:15 62 5
Plate VI
J
Furnace
C reek
\ Inn
TRAIL CANYON
AREA
AREA
OF
STUDY
van
. a i . J
Canyon
- Natural
_/ Bridge
Bad >
Water •
Eagle
Borax
Works
Dantes
Po int
Bennet ts
Paved Road
Graded Road
Jeep Road
3hosnone
Scale in Miles
alena
Canyon
To
Shoshone
Plate VII
graphic thinning is known to occur in the vicinity of
Aquereberry Point (Hunt and Mabey, 1966, p. 25). A
lithologic and partial paleontologic description of these
formations is presented in the following pages.
Stratigraphy and Paleontology
PRECAMBRIAN ROCKS
Crystalline Basement
Precambrian crystalline basement rocks are not
present in the area studied. They crop out in Galena
Canyon, a few miles south of Trail Canyon, and consist
mainly of gneisses and schists (Hunt and Mabey, 1966, p.
11) .
Pahrump Series
The Pahrump Series was named by Hewett (1940, pp.
239-240) for exposures in the vicinity of Pahrump Valley.
The name is applied to a sequence of metasedimentary and
sedimentary rocks which in the type area rest unconformably
on the crystalline basement and are in turn unconformably
overlain by rocks of Paleozoic Age. Rocks of this series
are not present in the area of study but are present in
canyons south of Trail Canyon. Where present, they rest
unconformably on basement and are in fault contact with
the overlying Noonday Dolomite (Hunt and Mabey, 1966, pp.
47
12-14). ,
PALEOZOIC ROOKS
EOCAMBRIAN SYSTEM
Noonday Dolomite
The Noonday Dolomite was named by Hazzard (1937*
pp. 300-301) for exposures near the Noonday Mine in the
Nopah Range, California. In the Panamint Range it con
sists of a lower cream colored dolomite with an upper
portion of gray dolomite (Hunt and Mabey, 1966, p. 16).
The Noonday Dolomite has a thickness in excess of 1,000
feet and contains possible Scolithus tubes (Hunt and Mabey,
1966, p. 16). It is present at the head of Trail Canyon
but does not crop out in the area studied. The Noonday
Dolomite is gradational with the overlying Johnnie Forma
tion and is in fault contact with the underlying Pahrump
Series (Hunt and Mabey, 1966, p. 16).
Johnnie Formation
The Johnnie Formation was named by Nolan (1929,
pp. 461-463) for exposures near the town of Johnnie,
Nevada. In the Panamint Range, strata equivalent to this
sequence were originally referred to as the Hanaupah
Formation (Murphy, 1932, p. 349), but recent authors have
placed these strata in the Johnnie Formation (Hunt and
~4£Tj
Mabey, 1966, p. 17). j
The Johnnie Formation, in the Panamint Range, has
a maximum thickness in excess of 4,000 feet (Hunt and j
Mabey, 1966, pp. 18-19). It is gradational with the
underlying Noonday Dolomite (Hunt and Mabey, 1966, p. 18) j
and appears gradational with the overlying Sterling |
Quartzite. j
Where studied, the Johnnie Formation is an olive-
green phyllite and phyllitic shale with some interbeds of
sandy limestones and quartzitic sandstones, cut by
numerous thin milky quartz veins and veinlets (Fig. 9).
The lowest portion exposed in the area studied is a buff-
colored, thin-bedded, sandy limestone which grades up
ward into a limy shale, then into a shale-phyllite series,
and finally into a sequence of interbedded quartzitic
sandstones and shales at the top.
Sterling Quartzite
The Sterling Quartzite received its name from
Nolan (1929, p. 464) for exposures near the Spring
Mountains in Nevada. It consists basically of upper and
lower units of medium- to coarse-grained, quartzitic
sandstones and interbedded shales which are separated by
a central portion of shale. A lower quartzitic sandstone
is locally conglomeratic near the base, with the con
glomerate composed mainly of white quartz pebbles held in
49
Figure 9*— Milky quartz veins and veinlets
cutting through phyllites in the Johnnie
Formation, near the head of Trail Canyon,
coarse- to very coarse-grained quartzitic sandstone. Most j
of the quartzitic sandstones are cross-bedded and weather j
I
red-brown to brown while the shaly interbeds display some
ripple markings and weather gray-green to purple. The
Sterling Quartzite has a maximum thickness of 2,000 feet i
(Hunt and Mabey, 1966, p, 21), It appears to be con- j
formable with the underlying Johnnie Formation, although
a pebble conglomerate near its base might indicate the
existence of a disconformity at this horizon. The Sterl
ing Quartzite grades conformably into the overlying Wood
Canyon Formation (Fig. 10).
EOCAMBRIAN AND CAMBRIAN SYSTEMS
Wood Canyon Formation
The Wood Canyon Formation was named by Nolan (1929,
p. 463) for exposures in the Spring Mountains of Nevada.
In the Panamint Range, the Wood Canyon Formation consists
of fine- to medium-grained, thin-bedded, quartzitic sand
stones and micaceous shales with some carbonates present
in the lower and upper portions. The formation has a
maximum thickness in excess of 2,500 feet (Hunt and Mabey,
1966, p. 23). It is conformable with the underlying
Sterling Quartzite as well as the overlying Zabriskie
Quartzite.
No fossils were found during this investigation,
however the presence of Scolithus tubes and possible_______
51
Figure 10.— Contact between the Sterling
Quartzite (-6s) and the Wood Canyon Forma
tion (*Sw), along the north wall of Trail
Canyon.
algal structures in the lower portion of the Wood Canyon
Formation and trilobites in the upper part are reported
by Hunt and Mabey (1966, p. 22). This faunal zone, in the
upper portion, is characterized by the presence of
Nevadella gracile (Walcott) and marks the lowest occur
rence of trilobites yet found in the southern Panamint
Range (Hunt and Mabey, 1966, p. 22). In addition to
Nevadella gracile (Walcott), the upper portion contains
other fragmentary trilobites, some brachiopods, and some
oolitic, archaeocyathid-bearing, and/or pelmatazoan-
bearing carbonates (Hunt and Mabey, 1966, p. 22).
CAMBRIAN SYSTEM
Zabriskie Quartzite
Hazzard (1937, p. 309) originally designated the
Zabriskie Quartzite as member 4-H of the Wood Canyon
Formation. The Zabriskie Quartzite has since been raised
to formational status (Wheeler, 1948, pp. 24-25). In the
Panamint Range it is gray to tan quartzite with some
interbeds of micaceous shale and quartzitic sandstone near
the top and base. The Zabriskie Quartzite has a thickness
in excess of 200 feet (Hunt and Mabey, 1966, p. 25) but is
only 100 feet thick in the Trail Canyon area. It contains
some possible Scolithus tubes, rests conformably on the
Wood Canyon Formation, and is in turn overlain conformably
by the Carrara Formation.
53
Carrara Formation
The Carrara Formation was named by Cornwall and
Kleinhampl (1961) for exposures near Bare Mountain,
Nevada. As originally described, it includes all rocks
present between the Sterling Quartzite and the Bonanza
King Dolomite. It has since been modified, and Burchfiel
(1964, p. 47) applies the name Carrara Formation to all
rocks forming a transitional sequence between the early
Cambrian coarse elastics and the Middle Cambrian
carbonates. The Carrara Formation thus defined includes
the upper portion of the Wood Canyon of Nolan (1929, p.
463) and all of the Cadiz Formation of Hazzard (1937, pp.
314-315).
The Carrara Formation, in the southern Panamint
Range, is a succession of shales, limestones, and quartz
itic sandstones. It has a maximum thickness exceeding
1,200 feet (Hunt and Mabey, 1966, p. 26) with the lower
portion containing olenellid trilobites and the upper
portion containing Middle Cambrian trilobites (Bates,
1965, p. 14; Hunt and Mabey, 1966, p. 25). The Carrara
Formation appears to be overlain conformably by the
Bonanza King Dolomite. All members within this formation
appear to be conformable with one another.
The Carrara Formation was examined along the east
54
wall of a tributary to Trail Canyon (Pig, 11) where a 600-
foot section was measured. The remaining upper portion
was unmeasured due to inaccessibility.
In adopting the usage of the name Carrara Formation,
the writer has herein lowered the status of three of
Hazzard1s formations to members and has divided the
measured portion of the Carrara Formation into the Latham
Member, Chambless Member and Cadiz Member. The Latham
Member is a 130-foot sequence of shale, quartzitic sand
stone, and limy shale. The lower 30 feet is a thin-bedded,
fine- to medium-grained, quartzitic sandstone with some
thin limestone and shale interbeds. This unit weathers
tan to gray-green and becomes progressively siltier to
ward the top. The next 85 feet consists of thin-bedded
gray-green to olive-green shale with some thin quartzitic
sandstone and limestone interbeds. The number of lime
stone beds increase toward the top until the remaining 15
feet of this member consists of thin-bedded, silty lime
stone. This upper 15 feet contains some trilobite remains
and weathers thin, platy, and light tan in color.
Above the Latham Member is a 200-foot section of
girvanellid-bearing limestone which is designated the
Chambless Member. This member consists of massive, blue-
gray weathering limestone with some shaly interbeds near
the top and base. The only fossil found in this member was
Girvanella sp.
Figure 11.— View north from Trail
Canyon showing the Wood Canyon
Formation (-Cw), Zabriskie Quartz
ite (£z), Carrara Formation (-Cc),
and Bonanza King Formation (-6b).
The uppermost member, the Cadiz Member, was not
measured in its entirety due to inaccessibility to the
upper portion. The lower portion was examined and was
divided into two submembers which are arbitrarily called
A and B. Submember A consists of 200 feet of tan to gray-
green shales with some interbedded limestones and quartz
itic sandstones.
Submember B is 70 feet thick and consists
principally of thin-bedded, fine- to medium-grained,
quartzitic sandstone. It contains some thin shaly beds
near the base and some sandy limestone beds near the top.
Above Submember B is a gray to blue-gray cliff-
forming limestone, overlain by a slope-forming gray-green
shaly looking unit, and finally another cliff-forming
gray-blue carbonate sequence. The total thickness of this
upper unmeasured portion is estimated between 500 and 600
feet.
The only fossils found in the Carrara Formation
were some possible Scolithus tubes, some unidentifiable
olenellid fragments, and Girvanella sp. Bates (1965> pp.
14, 15, and Table I) and Hunt and Mabey (1966, pp. 25-26)
describe the presence of the following fauna from the
lower portion of the Carrara Formation:
Algae
G-irvanella sp.
57 I
i
Brachiopoda j
Dictyonina sp.
Lingulella sp.
Nisusla sp.
Paterina prospectensis Walcott I
Trilobita |
Bristolla sp. I
Fremontia sp.
Olenellus sp.
Onchocephalus sp.
Paedeumias clarki Resser
P. nevadensis (Walcott)
Peachella sp.
NOPAH AND RESTING SPRINGS RANGES
Introduction
The Nopah and Resting Springs Ranges are nearly
north-south trending, parallel ranges separated by Chicago
Valley. They are located east of the town of Shoshone,
California, within the Furnace Creek and Avawatz Mountains
quadrangles (Plate VIII). They vary in elevation from
2,000 to over 5,000 feet. A paved highway leading east
from the town of Shoshone passes through the ranges and
additional access into the area is provided by dirt roads.
Precambrian and Cambrian rocks are represented
here by over 17,000 feet of sedimentary strata (Hazzard,
1937, pp. 299-316). Some of the first geologic work on
the areawas a brief summary by Spurr (1903, pp. 195-200)
and a regional report by Noble (1934). Geologic know
ledge of the area has been increased as a result of the
detailed stratigraphic work of Hazzard (1937, pp. 273-339)
Furnace y
vC re e k x
X jn n / - / /
$ Johnnie
Death ,
Valley I
J unction
Shoshone
/
H w y.
127
10 15
Scale in Miles
Nopah-Resting Springs
Ranges
Camp Irw in Baker
H wy.
99 & 466
Plate VIII
59
and the partial mapping of the area by Mason (194-8) and
Wilhelms (1963).
Detailed stratigraphic work by the writer was in
the vicinity of Hazzard!s measured section B-Bf (1937,
pp. 274 and 294), where a section of strata was measured
from the upper Wood Canyon Formation to the upper Carrara
Formation. Thickness of the portion measured was in very
close agreement with that reported by Hazzard (1937, pp.
274, 278, and 294). In addition to this measured section,
fossils were collected near Hazzard*s (1937, p. 274)
fossil localities R-8 and R-10, and from an area about 3
miles north of these localities.
Stratigraphy and Paleontology
PRECAMBRIAN ROCKS
Crystalline Basement
The Precambrian crystalline basement consists
principally of granitic gneiss and mica schist. The
granitic gneiss is usually coarse-grained and contains
large pink feldspar crystals (Hazzard, 1937, p. 299).
Crystalline basement is overlain unconformably by strata
of the Pahrump Series and/or Noonday Dolomite (Hazzard,
1937, p. 279).
60 |
Pahrump Series |
The Pahrump Series (Hewett, 1940, pp. 239-240) in j
I
the Nopah Range is a sequence of metasedimentary and j
sedimentary limestones, shales, and conglomeratic sand- j
stones (Hazzard, 1937, p. 299). This series attains a j
thickness of approximately 7,000 feet and is unconformable
with the underlying crystalline basement (Hazzard, 1937,
P. 279).
i
PALEOZOIC ROCKS
EOCAMBRIAN SYSTEM
Noonday Dolomite
The Noonday Dolomite (Hazzard, 1937, pp. 300-301)
is light gray to tan dolomite which contains some algal-
like structures and has a thickness of 1,300 feet
(Hazzard, 1937, p. 279). It is in conformable contact
with the overlying Johnnie Formation and rests uncon
formably upon either the Precambrian crystalline basement
or strata of the Pahrump Series (Hazzard, 1937, p. 279).
Johnnie Formation
In the Nopah Range the Johnnie Formation (Nolan,
1929, pp. 461-463) consists of a 2,500-foot sequence of
quartzitic sandstones, micaceous shales, and silty and/or
arenaceous carbonates (Hazzard, 1937, pp. 303-306). The
6ll
Johnnie Formation rests conformably on the Noonday Dolo- !
i
mite and is questionably disconformable with the overlying j
Sterling Quartzite (Hazzard, 1937, pp. 305-306). I
i
i
i
Sterling Quartzite
In the Nopah Range the Sterling Quartzite (Nolan,
I
1929, p. 464) attains a thickness of about 2,600 feet
(Hazzard, 1937, P* 307). The formation consists of a
thick lower unit of conglomeratic, coarse-grained,
quartzitic sandstone, a thin central unit of micaceous
shales, and a thick upper unit of medium- to coarse
grained, quartzitic sandstone (Hazzard, 1937, pp. 306-307).
The existence of the pebble conglomerate at the base of
the Sterling Quartzite possibly indicates the presence of
a disconformable contact between it and the underlying
Johnnie Formation (Hazzard, 1937, p. 279). The Sterling
Quartzite is overlain conformably by the Wood Canyon
Formation.
EOCAMBRIAN AND CAMBRIAN SYSTEMS
Wood Canyon Formation
The Wood Canyon Formation (Nolan, 1929, p. 463)
crops out in both the Nopah and Resting Springs ranges.
It is the uppermost formation assigned to the Lower
Cambrian. In the Nopah and Resting Springs Range regions,
the Wood Canyon Formation attains a thickness of over______
! 3,000 feet (Hazzard, 1937, pp. 307, 311). The upper 800
j
j feet, members 4-H through 4-0, which Hazzard (1937, p.
278) called the Wood Canyon Formation, and all of the
Cadiz Formation (Hazzard, 1937, pp. 314-315) are now
placed in the Zabriskie Quartzite and the Carrara Forma
tion (Hunt and Mabey, 1966, pp. 24-27). The Wood Canyon
Formation is conformable with the underlying Sterling
Quartzite (Hazzard, 1937, p. 278).
The upper 100 feet of the Wood Canyon Formation is
present in the area examined. This strata consists of
gray to brown-gray, micaceous shales with interbeds of
fine- to medium-grained, quartzitic sandstone. The
quartzitic sandstones increase both in number and in thick
ness near the top. No fossils were found in this shaly
sequence, but Mesonacis fremonti Walcott (now Fremontia
fremonti rWalcott']), Wanneria (?) gracile Walcott (now
Nevadella gracile (Walcott)), and Obolella vermilionensis
Walcott are reported from a stratigraphically lower shale
sequence (Hazzard, 1937, p. 278).
CAMBRIAN SYSTEM
Zabriskie Quartzite
The Zabriskie Quartzite (Hazzard, 1937, p. 309) was
examined along the west side of the Resting Springs Range,
just north of the Resting Springs Ranch. It consists of
| 120 feet of massive, medium-grained, locally cross-bedded, j
i
gray to tan quartzite with some minor shale and coarse-
! |
j grained, quartzitic sandstone lenses near the top and
bottom. No recognizable fossils were found in this forma- |
tion. The Zabriskie Quartzite is underlain conformably by |
the Wood Canyon Formation. j
I
I
Carrara Formation i
j
The Carrara Formation crops out along the west flankt
|
of the Resting Springs Range (Fig. 12). In the Resting
Springs Range area, the Carrara Formation encompasses
units 4-1 through 4-0 of the Wood Canyon Formation of
Hazzard (1937, p. 278) and all of the Cadiz Formation of
Hazzard (1937, p. 278). The formation has a thickness in
j excess of 1,300 feet and is conformable with the under
lying Zabriskie Quartzite and the overlying Bonanza King
Formation (Hazzard, 1937, pp. 277-278).
The portion of the Carrara Formation measured is
divided into three members which, in stratigraphic order,
are herein called the Latham Member, the Chambless Member,
and the Cadiz Member (see Carrara Formation, p. 51). The
Latham Member consists principally of sandy, micaceous
shales with some siltstones and quartzitic sandstones.
The Latham Member has been divided into three submembers
which are arbitrarily A, B, and C. Submember A is a 200-
foot succession of sandy, micaceous shale and siltstone
64
Figure 12.— West flank of the Rest
ing Springs Range just east of Sho
shone, California, showing the Wood
Canyon Formation (-Gw), Zabriskie
Quartzite (-Gz), Carrara Formation
(-Gc), and Bonanza King Formation
(-Sb).
I 65 !
!with a central portion of silty, thin-bedded, fine- to
medium-grained quartzitic sandstone. The quartzitic sand
stones are locally cross-bedded and the shales and fine- !
i
grained sandstones exhibit ripple marks along partings. i
i ;
There are some thin limy lenses in the upper portion which !
become increasingly common near the top. The upper shaly-
limy portion contains numerous olenellid remains. The
identifiable form found was Paedeumias sp. The shales
weather a gray-green to olive-green, the quartzitic sand
stones a tan to dark brown, and the limy lenses a tan to
yellow-brown.
Above this shaly succession is 100 feet of thin-
bedded, arenaceous and/or silty limestone which is
designated as submember B. This limestone contains some
thin interbeds of limy shales and limy sandstones. Some
of the limestones contain Girvanella sp. and the shaly
portions contain olenellid fragments; no identifiable
trilobites were found in this submember. The limestones
weather a buff to tan color with local tan and yellow-
brown mottled areas. The limy shales and limy sandstones
weather gray-green to gray-brown.
Submember C is a 110-foot sequence of shales and
siltstones with some locally thin sandy and limy interbeds.
This submember contains locally abundant olenellid remains
and some questionable algal structures. Trilobites occur
ring in the lower part of this member are Bristolia (?)
66
sp., Fremontia (?) sp., Paedeumias clarki Resser, and
Paedeumias nevadensis (?) Walcott. This submember weathers
gray-green to olive-green with some local gray-brown areas.
j
Overlying the Latham Member is the Chambless Mem- |
i
ber. The Chambless Member consists of 100 feet of algal
limestone with some thin interbeds of limy sandstones and
limy, micaceous shales and siltstones. The limestones
|
contain Girvanella sp. and are locally oolitic. They
weather mottled gray and blue-gray with occasional yellow-
brown to orange-brown patches while the sandy and shaly
interbeds weather gray-green to gray-brown.
The uppermost member, Cadiz Member, consists mainly
of shales, carbonates, and fine-grained, micaceous sand
stones. The lower 220 feet of this member was examined
and found to consist principally of shale with some thin
carbonate and sandy interbeds.
Hazzard (1937, p. 278) reported the presence of
trilobite fragments from the lower portion of the member.
Except for some possible tracks and trails, no fossils
were found in this member at the area examined. The
shales weather a variegated light gray-green to dark
violet with the carbonate and sandy interbeds weathering
tan to brown.
This lower shaly portion is overlain by a cliff-
forming mottled gray to blue-gray and yellow-brown
weathering sandy limestone. This limestone was the upper-
most bed of Cambrian strata examined by the writer in the
Resting Springs Range.
|
PROVIDENCE MOUNTAINS
Introduction
The Providence Mountains are essentially a north-
south trending range located 5 miles east of Kelso, Cali
fornia (PI. IX) within the Kelso and Flynn quadrangles.
They range in elevation from 4,000 to over 7,000 feet.
Two areas within the range were investigated. These areas
are accessible by a dirt road which leads east from the
main road, just south of Kelso, California. This dirt
road forks about 1 mile east of town with the right fork
going to the area of Cornfield Spring and the left one to
the vicinity of South Hayden Wash. The road to South
Hayden Wash is locally bad but was passable to convention
al vehicles in the fall of 1966, when the area was last
visited. The road to Cornfield Spring, however, is
recommended for use by four-wheel drive vehicles only.
Lower Paleozoic strata crop out at both of these areas and
a section was measured near South Hayden Wash (PI. X).
Most of the geologic work on this area has been
conducted by J. C. Hazzard and published by him in a
number of different articles (Hazzard, 1933> 1937 > 1938,
1941, and 1954). In addition to his work, the northern
portion has been described by Hewett (1956)._______________
C i ma
Kelso
O -AREAS OF STUDY
10
Seale in M ile s
Amboy
C h am b less
Cadiz
69
Two formations, the Prospect Mountain Quartzite and ;
the Carrara Formation (Pig. 13) comprise the strata of
Early Paleozoic Age. The following paragraphs present a j
i
lithologic and paleontologic description of the strata |
i
examined during this study in the Providence Mountains. |
Stratigraphy and Paleontology
PRECAMBRIAN ROCKS
Crystalline Basement
Crystalline basement rocks in the Providence
Mountains are fine- to medium-grained, granitic gneiss.
The gneiss varies in color from a dark gray to a gray-
green and is overlain unconformably by the Prospect
Mountain Quartzite.
PALEOZOIC ROCKS
EOCAMBRIAN SYSTEM
Prospect Mountain Quartzite
The Prospect Mountain Quartzite was named by
Hague (1883, p. 254) for exposures at Prospect Mountain,
near the town of Eureka, Nevada. In the vicinity of
South Hayden Wash (PI. X), the Prospect Mountain Quartzite
consists of 960 feet of quartzite and quartzitic sand
stone with minor shale, siltstone, and conglomerate.
€t
■N x ,' .x.
Figure 13.— Outcrops of Prospect Mountain Quartzite (-Gp),
Carrara Formation (-Gc), and Bonanza King Formation (-Gb)
along the west side of Providence Mountain, near Corn
field Springs.
/ pG g
G c A'
<_/ \
So. Hayden Wash
Ar ea
Scale 1=15625
Plate X
72
The Prospect Mountain Quartzite rests unconformably
upon the Precambrian crystalline basement and is overlain
conformably by the Carrara Formation. Units within this
formation appear to be conformable with one another, al
though a sharp lithologic break between members A and B
!might indicate the existence of a disconformity at this
i
horizon.
The writer herein subdivides the Prospect Mountain
Quartzite into five members, which are arbitrarily called
A, B, C, D, and E. The lowest member, Member A, is a
quartzite and quartzitic sandstone and shale sequence. The
bottom 50 feet is a fine-grained, light gray to tan
quartzite which becomes coarser grained near the top and
base. The upper 100 feet consists of a sequence of fine-
to very coarse-grained, cross-bedded, quartzitic sand
stones with interbedded shales and siltstones.
Member B is a sequence of quartzitic sandstones,
shales, and conglomerates. This sequence is 20 feet
thick, and the lower 4 feet and upper 2 feet consist of a
quartz pebble conglomerate. The clasts range in size from
1/4 to 3/4 of an inch in length and consist principally
of milky quartz pebbles with occasional reddish or brown
jasperoid pebbles (Fig. 14). Between the upper and lower
conglomerate beds is a series of interbedded coarse- to
very coarse-grained, cross-bedded, quartzitic sandstones
and micaceous shales with some occasional thin con-
73
Figure 14.— Conglomerate bed at
the base of member B of the
Prospect Mountain Quartzite in
the northern Providence Mount
ains, near South Hayden Wash.
I glomerate stringers (Pig. 15)*
j
Above this is a 550-foot sequence of interbedded
medium- to very coarse-grained, cross-bedded, quartzitic
sandstones and shales which is designated Member C. The
interbedded shales exhibit ripple marks and some possible j
tracks and/or trails, but no definite organic remains were !
found. j
Member D consists of 140 feet of greenish-gray |
I
j
siltstones and gray-brown to green-brown, thin, platy,
quartzitic sandstones. These sandstones show some cross
bedding and some of the siltstone exhibit ripple marks.
This member weathers brownish-green and produces a break
in slope between more resistant cliff-forming quartzitic
sandstones.
The topmost member, Member E, is a 100-foot section
of brownish-weathering, tan to gray quartzite and
quartzitic sandstone. The basal and upper portions of
this member are medium-grained, locally cross-bedded,
quartzitic sandstone. These medium-grained quartzitic
sandstones are separated by a central portion of fine
grained orthoquartzite which is almost devoid of any
depositional features. Member E is locally mineralized
by hematite veins and the quartzite adjacent to these
mineralized zones is usually crushed and altered. These
mineralized zones have been prospected for iron ore in the
vicinities of South Hayden Yfash and Cornfield Springs.
75
Figure 15.--Grit and pebble lense
in member B of the Prospect
Mountain Quartzite, near South
Hayden Wash.
76]
CAMBRIAN SYSTEM I
! I
i j
Carrara Formation
i
|
The Carrara Formation (Cornwall and Kleinhampl,
1961) of the Providence Mountains was originally described |
by Hazzard (1954-, PP* 30-31) as three formations, the j
iLatham Shale, the Chambless Limestone, and the Cadiz
Formation. The writer has adopted the usage of the name
Carrara Formation in place of Hazzardfs original three
formational names and has herein lowered the status of
these three formations to that of members. In the
vicinity of South Hayden Wash, the Carrara Formation
consists of an 850-foot succession of micaceous, quartz
itic sandstones, shales, siltstones, and carbonates. It
s
appears to rest conformably upon the Prospect Mountain j
|
Quartzite and is in turn overlain conformably by the
Bonanza King Dolomite. All members within the formation
appear conformable with one another.
The Latham Member consists of 70 feet of quartzitic
sandstone and shale. The basal 50 feet is principally a
thin-bedded, fine- to medium-grained, quartzitic sand
stone which becomes increasingly shaly toward the top.
This upper shaly portion contains common brachiopod
remains and numerous trilobite fragments. The brachiopods
found are all of the same species, Paterina prospectensis
Walcott. In addition to this one species of brachiopod,
two identifiable trilobites, Bristolia cf. B. bristolensis I
(Walcott) and Fremontia (?) sp. were found in this portion
of the Latham Member. j
i
The upper 20 feet of the Latham Member is pre- !
dominantly thin-bedded, gray-green, micaceous shale. j
l
This portion contains the same fauna found in the lower
part as well as the trilobite Paedeumias nevadensis Wal
cott .
Overlying the Latham Member is the Chambless
Member. This member is a 160-foot sequence of girvanellid-
bearing limestone (Pig. 16) with some minor thin shaly
interbeds. Hazzard (1954, PP* 30-31) reported the presence
of brachiopods and trilobites from the shaly interbeds,
although Girvanella sp. was the only fossil found in the
member at the area examined by the writer.
Next is a 620-foot succession of shales, fine
grained, micaceous, quartzitic sandstones, and thin
carbonate lenses herein designated the Cadiz Member. This
member has been divided into four submembers which are
arbitrarily called A, B, C, and D.
Above the Chambless Member is a 280-foot sequence
of shale with some thin interbeds of quartzitic sandstone
and some thin carbonate lenses. The carbonate lenses are
sandy, usually less than 3 feet thick, and are locally
oolitic. The carbonates weather buff to tan and exhibit
some cross-bedding structures on the weathered surface.
78
Figure 16.— Girvanellid-bearing
limestone in the Chambless Member
of the Carrara Formation, near
Cornfield Springs.
79 j
t
The quartzitic sandstones are fine- to medium-grained, j
!
micaceous, and thin-bedded. They are locally cross- i
bedded and weather tan to yellow-brown in color. The I
shales are micaceous, weather tan to gray-green, and ex- I
hibit some ripple marks along bedding. Lower Cambrian
fossils are reported from the lower portion of this shale j
(Hazzard, 1954, pp. 30-31) but only tracks, trails, and I
!
some possible Scollthus tubes were noted. |
I
Submember B is a 15-foot bed of sandy limestone
which weathers a tan to brown color. The limestone is j
{
sandy, locally oolitic and exhibits cross-bedding |
(
structures on the weathered surface. i
i
Submember C consists of an 185-foot succession of j
i
siltstones, shales, and fine-grained quartzitic sand- j
stones with some minor carbonate interbeds. All the I
clastic rocks are thin-bedded and micaceous with most
exhibiting ripple marks, tracks and/or trails along
bedding (Pig. 17). This unit weathers tan-green to gray-
violet. A Middle Cambrian fauna is reported from this
member (Hazzard, 1954, pp. 30-31)> although no fossils
were found. This member contains an oolitic carbonate bed
about 50 feet below its top, which is 4 feet thick and
weathers tan to gray-brown.
The uppermost submember, Submember D, is principally
a gray to gray-blue weathering, thin-bedded limestone with
numerous gray-green to olive-green weathering limy shale
80
Figure 17.— Ripple marked, fine-grained,
micaceous, quartzitic sandstone in the
Cadiz Member of the Carrara Formation,
near South Hayden Wash.
interbeds, Hazzard (1954-, PP* 30-31) reported the
presence of a Middle Cambrian fauna from this submember
consisting of Alokistocare sp,, Zacanthoides sp.,
Clavaspidella sp., and Glossopleura sp. This submember
grades upward into massive gray colored limy dolomites of
the Bonanza King Formation.
MARBLE MOUNTAINS
Introduction
The Marble Mountains contain the southernmost out
crops of the Precambrian through Cambrian strata present
in eastern California. These outcrops are confined to the
southern portion of the range; the northern part of the
range consists mainly of Tertiary volcanics. The Marble
Mountains range in elevation from 1,000 feet to over
3,800 feet. Two areas in the southern portion were
examined; one of these is located just north of Cadiz,
California (PI. XI and XII) and the other is about a mile
northeast of Chambless, California (PI. XI). The southern
portion of the range is crossed by Highway 66, and addi
tional access to the area may be gained via numerous dirt
roads.
The geology of this region was first described by
Darton (1907) and has since been studied stratigraphically
by Clark (1921) and by Hazzard (1933). In addition to
C i ma
: A-
Kelso
O -AREAS OF STUDY
10
Seale in Miles
Amboy
Cham bless
Cadiz
e cc
€cB
€c A
6cc
eci
e p r
peg
83
LEGEND FOR MARBIE MOUNTAIN MAP
Cambrian
Carrara Formation,Cadiz Member, Sutamember C
Carrara Formation,Cadiz Member,Submember B
Carrara Formation,Cadiz Member,Submember A
Carrara Formation, Chambless Member
Carrara Formation, Latham Member
Eocambrian
Prospect Mountain Quartzite
Precambrian
Crystalline Basement
Plate Xla
Gee G c A ;GcC
30V \ \ u
40'/
G p r
Qal
G pr G pr
/Gcc
O
So. Marble Mtn.
Area
Scale 1:15625
Plate XII
| this stratigraphic work, paleontologic studies of the !
|region have been conducted by Resser (1928), Crickmay (in |
Hazzard, 1933), Mason (1935) and Riccio (194-9 and 1952),
i
Geologic field mapping has also been carried out in this |
region by Kilian (1964), Two formations, the Prospect j
Mountain Quartzite and the Carrara Formation, comprise the j
Eocambrian through Cambrian strata present here (Fig. 18). j
!
These formations are conformable with one another and rest j
I
unconformably on the Precambrian crystalline basement j
t
(Fig. 19).
I
Stratigraphy and Paleontology
PRECAMBRIAN ROCKS
Crystalline Basement
The crystalline basement consists of dark gray to
pink-gray granitic gneiss which is characterized by the
presence of pinkish feldspar porphyroblasts. The feldspar
porphyroblasts attain a size of nearly one inch in length,
and where abundant, impart a pinkish cast to the rock.
The granitic gneiss is locally cut by two- to four-foot
thick diabase dikes which weather dark green-brown to
black. The crystalline basement is overlain unconformably
by the Prospect Mountain Quartzite.
86
Figure 18.— Paleozoic sedimentary
sequence in the Marble Mountains
northeast of Chambless, California,
showing the Prospect Mountain
Quartzite (-0pr), Carrara Formation
(■0c), and Bonanza King Formation
( ■ 0 b).
87
Figure 19.— Unconformity between
the Precambrian gneiss (p€g) and
the Prospect Mountain Quartzite
(5pr), southern end of the
Marble Mountains just northeast
of Cadiz, California.
PALEOZOIC ROCKS
88
EOCAMBRIAN SYSTEM
Prospect Mountain Quartzite
The Prospect Mountain Quartzite (Hague, 1883, p.
254) consists of 500 feet of quartzitic sandstone with a
basal conglomeratic portion and an upper-central thin
shaly area. It rests unconformably upon the Precambrian
crystalline basement and is overlain conformably by the
Carrara Formation. No definite organic remains have been
found in this formation, but some of the structures
present may possibly represent Scolithus tubes.
The Prospect Mountain Quartzite is principally a
light-brown to dark-brown weathering, medium-grained,
quartzitic sandstone with the upper 50 to 60 feet slightly
coarser grained and lighter brown in color. The basal 10
to 15 feet is conglomeratic with the clasts ranging in
size from 1/2 to 1 inch across which are held in a poorly
sorted, locally cross-bedded, coarse-grained feldspathic,
quartzitic sandstone. The clasts consist principally of
milky quartz pebbles but there are occasional red jasperoid
pebbles present. In addition to the conglomeratic basal
portion, there is a sequence of thin shaly units present
about 90 feet down from the top. This shaly interval is
present in the area north of Chambless but is absent in
the area near Cadiz._______________________________ ; _________
CAMBRIAN SYSTEM
89
Carrara Formation
The Carrara Formation (Cornwall and Kleinhampl,
1961) is a 530-foot succession of micaceous shales,
quartzitic sandstones, and sandy looking carbonates. It
contains an olenellid fauna in the lower portion and a
Middle Cambrian fauna in the upper part (Hazzard, 1933,
pp. 72-74). The Carrara Formation rests conformably upon
the Prospect Mountain Quartzite and is overlain conformably
by the Bonanza King Formation. All members within this
formation appear to be conformable with each other.
The Carrara Formation is again subdivided into
three members (see Carrara Formation, p. 72); the Latham
Member, the Chambless Member, and the Cadiz Member. The
Latham Member is a 35-foot sequence of micaceous shale
with some thin interbeds of limy shale, quartzitic sand
stone, and limestone.- Interbedded quartzitic sandstones
are common in the lower portion (Fig. 20), and limestone
lenses are abundant in the upper part. The shales weather
a gray-green to olive-green, with local rust colored sandy
lenses and buff to red-brown colored limy lenses. It
contains an abundant Early Cambrian fauna with the follow
ing forms having been found by the writer and/or reported
present by Crickmay (in Hazzard, 1933, pp. 72-73) and
Riccio (1962, p. 28):
90
Figure 20.— Interbedded shale and
quartzitic sandstone in the
Latham Membei* of the Carrara
Formation, northeast of Cadiz,
California.
91
Brachiopoda
Paterlna prospectensls Walcott
Trilobita
Bristolia sp.
Fremontia fremontl (Walcott)
Fremontla sp.
Laudonla bisplnata Harrington
Paedeumias clarki Resser
Paedeumlas nevadensis Walcott
Peachella sp.
Above this shale member is a 70-foot sequence of
blue-gray to gray weathering girvanellid-bearing limestone
which is designated the Chambless Member. The lower 40
feet is principally a massive Girvanella limestone (Fig.
21 and 22) with a few thin green shaly interbeds near the
base. Trilobite fragments are present in the interbedded
shales but Girvanella sp. was the only Identifiable fossil
found in the lower portion of this member.
The upper part of the Chambless Member consists of
30 feet of alternating blue-gray grivanellid-bearing,
silty limestone and tan to gray-green limy shale. Because
of the weathering characteristic of the algal structures
within it, this upper portion of the members weathers with
a nodular appearance (Fig. 23). The shales contain both
brachiopods and trilobites, and those found include the
following:
Algae
Girvanella sp.
Brachiopoda
Dichtyonlna sp.
Paterlna (?) sp.
92
Figure 21.— Algal limestone of
the Chambless Member (-Gcc) rest
ing on shales of the Latham
Member (*0cl) of the Carrara
Formation, northeast of Cadiz,
California.
93
Figure 22.— Girvanella sp. in the
Chambless Member of the Carrara
Formation, northeast of Cadiz,
California.
94
Figure 23.— Characteristic nodular
weathering of the upper part of
the Chambless Member of the Carrara
Formation, northeast of Cadiz,
California.
Trilobita
Fremontia sp.
Paedeumias nevadensis Walcott
Paedeumias sp.
Above the algal limestones is the Cadiz Member.
This member is a 425-foot sequence of shales, carbonates,
and quartzitic sandstones. The sequence has been divided
into four submembers, informally called A, B, C, and D.
Submember A is 140-foot succession of micaceous shales and
thin-bedded micaceous quartzitic sandstones with a few
thin limestone lenses (Pig. 24). This submember weathers
gray-brown to green-brown and contains flute casts, ripple
marks, and tracks and/or trails along partings. In addi
tion, there are some possible Scolithus tubes present in
some of the quartzitic sandstones.
Above this shaly sequence is a 20-foot thick
carbonate, which is designated Submember B. This
carbonate is slightly dolomitic, arenaceous in spots, and
oolitic. It weathers a yellow-brown color with a dis
tinctive cross-bedded pattern present on the weathered
surface (Pig. 25). The lower portion of this limestone
contains some trilobite fragments but no identifiable forms
were found.
Submember C is a 200-foot succession of micaceous
shales and fine- to medium-grained, thin-bedded, micaceous,
quartzitic sandstones with some occasional silty and/or
sandy carbonate lenses. The shales in this submember
exhibit a great variation in color ranging from light gray-
£e/S
■ 7
V ■ ’ nf .
L : —
* ^ • • • . v ^v-* ~ ;
'* -*■ ■ : > _ .£ • • ‘ ac-y' i. * v A-„.. J
**W ' ., m m & Z - - •
Figure 24.— Paleozoic sedimentary sequence in the Marble Mountains
Just northeast of Cadiz, California, showing the Precambrian
gneiss (pCg), Prospect Mountain Quartzite (-Cpr), and Carrara
Formation (-Cel, -Ccc, -GcA, and-CcB).
vo
Ch
97
Figure 25.— Cross-bedding on
weathered surface of submember
B, Cadiz Member of the Carrara
Formation, northeast of Cadiz,
California.
98
green to olive-green to maroon. The quartzitic sandstones
are not as variegated in color and range from yellow-brown
to maroon. Both the shales and quartzitic sandstones
contain flute casts, ripple marks, and tracks and/or trails
along the bedding planes.
The carbonate lenses vary in thickness from a few
inches to over 3 feet and weather buff to yellow-brown.
Some lenses are oolitic, and these usually weather with a
mottled appearance.
The uppermost submember, Submember D, consists of
65 feet of thin-bedded dirty gray limestone with some thin
interbeds of limy shale. This submember contains a Middle
Cambrian fauna consisting of Alokistocare sp., Glosso-
pleura sp., and Sonoraspis sp. (Hazzard and Crickmay,
1933, PP. 65 and 73; Stoyonaw and Susuki, 1955* P* 468).
Submember D is overlain conformably by the Bonanza King
Formation.
PROBABLE CORRELATIONS
Introduction
Many possible correlations between the strata of
Precambrian and Cambrian age have been postulated.
Wheeler (1948) published a correlation of late Precambrian
and Cambrian strata in southern Nevada and in some
portions of eastern California. Additional correlation of
99
portions of Precambrian and Cambrian strata in eastern
California have been published by Hazzard (1937), Hewett
(1956), Blanc (1958), Dorsey (i960), McKee and Moiola
(1962), Nelson (1962 and 1963), and Stewart (1966). The
previously mentioned published correlations were examined,
and in light of the information gathered during this
study, the following correlations are considered to be the
most sound.
Correlations
CRYSTALLINE BASEMENT
Crystalline basement rocks are present at all of
the regions examined, except for the White-Inyo Mountains
region, and consist of two principal types. At the Nopah-
Resting Spring Range and Marble Mountain regions the
crystalline basement is a granitic gneiss containing
pinkish feldspar porphyroblasts. The southern Panamint
Range and Providence Mountain regions are characterized by
a fine- to medium-grained granitic gneiss which tends to
be schistose in sheared areas. Barca (1965, P* 1) re
ports the presence of both types of crystalline basement
rocks in northern Old Dad Mountains.
PAHRUMP SERIES
Dorsey (i960, p. 28) suggests a possible correla
100
tion between portions of the Wyman Formation in the White-
Inyo Mountains with portions of the Pahrump Series in the
Death Valley area. The Pahrump Series in the Death Valley
area is herein correlated with the Wyman Formation in the
White-Inyo Mountains (PI. XIII). This correlation is
based on the similarity in lithology and the stratigraphic
positions. At the regions studied, strata of the Pahrump
Series and Wyman Formation are overlain unconformably by,
or are in fault contact with, thick dolomite sequences and
either rest unconformably on crystalline basement or have
no base exposed. The lithology of these two units, on a
regional basis, shows a slightly higher degree of meta
morphism than that of the overlying strata. It is because
of this difference in the degree of metamorphism and the
unconformable relationship with the overlying strata that
the Pahrump Series and Wyman Formation are herein con
sidered Precambrian in age.
Rocks similar to that of the Pahrump Series do not
extend very far south of the Nopah-Resting Springs Range
region and are absent in both the Providence and Marble
Mountains.
NOONDAY DOLOMITE
Correlation between the Noonday Dolomite in the
Death Valley area and the Reed Dolomite in the White-Inyo
Mountains has been suggested by Hazzard (1937, p. 301) and
101
Nelson (1962, p. 140). This same correlation has been pro
posed by McKee and Miola (1962, p. 533) for the Reed Dolo
mite in Esmeralda County, Nevada, and the Noonday Dolomite
in the Nopah Range. These correlations are inferred from
the similarities in lithology and stratigraphic position.
Stewart (1966, p. 66) relates the Noonday Dolomite' with
strata occurring in the Wyman Formation or possibly with
unexposed rocks below the Wyman Formation in the White-
Inyo Mountains. Stewart bases his proposed correlation
primarily of the absence of any Noonday Dolomite as a
massive dolomite facies in the Funeral Mountains, Cali
fornia. Based on the following reasoning, the Noonday
Dolomite is herein correlated with the Reed Dolomite (PI.
XIII).
The Noonday Dolomite is apparently absent in the
Funeral Mountains, but is present in the southern Panamint
Range 25 miles to the west. Here it attains a thickness
of over 800 feet and crops out along the range in a
general northwest-southwest directional trend (Hunt and
Mabey, 1966, p. 16 and PI. I). Extending this trend of
the Noonday Dolomite to the northwest would align it with
outcrops of Reed Dolomite in the White-Inyo Mountains and
could extend it across an area in which no outcrops of
strata in this age are known to be exposed.
The Noonday Dolomite appears to grade laterally
into a clastic facies to the north of the type locality
102
in the southern Nopah Range (Stewart, 1966, pp. 68 and 69).
It also appears to grade into a clastic facies to the
south and southwest of the type locality (Wright and
Troxel, 1966, pp. 846-856; 1967* pp. 943-945). Thus the
Noonday Dolomite may he present as a northwest-southeast
trending, tabular-shaped dolomite facies, represented to
the northwest by the Reed Dolomite, which grades laterally
into elastics along the flanks. In the Death Valley area
the trend of the Noonday Dolomite appears to parallel the
edge of a late Pre-cambrian positive area which Wright and
Troxel (196?, p. 940) call the Nopah Upland.
Away from the White-Inyo Mountains, the trend of
the Reed Dolomite appears to swing northeasterly across
the northern portion of the Last Change Range toward
Esmeralda County, Nevada. In the northern Last Chance
Range, Stewart (1965* pp. 63-67) reports the absence of
the Reed Dolomite as a dolomite facies but assigns a 1560
foot succession of limestones and quartzites, with some
minor siltstones and dolomites, to a combined Deep Springs
Formation and Reed Dolomite equivalent. This 1560 foot
thickness is the same as the thickness of the Deep Springs
Formation in the White-Inyo Mountains (Nelson, 1962, p.
140) and is less than the thickness of the Deep Springs
Formation in Esmeralda County, Nevada (McKee and Moiola,
1967» p. 533). It is probable that the apparent absence
of Reed Dolomite results from a lack of exposure rather
103
than a change of facies.
The Noonday Dolomite in the Death Valley area may
be correlative with the Reed Dolomite in the White-Inyo
Mountains and in Esmeralda County, Nevada. Likewise, it
is probable that these two formations together form on
arcuate trending, tabular-shaped dolomite facies which
grades laterally into elastics along the flanks and is
aligned along the edge of the late Precambrian positive
area, the Nopah Upland.
The dolomite facies of the Noonday Dolomite appears
to extend only a few miles to the south of the type
locality as it is absent in the Silurian Hills (Wright and
Troxel, 1966, pp. 846-851)* Barca (1966, p. 2), however,
reports the presence of a basal dolomite unit farther to
the south in the Old Dad Mountains which he considers to
be equivalent to the Noonday Dolomite. A similar dolomite
unit is also present in the Kelso Mountains (G. A. Davis,
personal communication, 1968). However, no strata cor
relative with the Noonday Dolomite occur in the Providence
or Marble Mountains regions.
JOHNNIE FORMATION
Nelson (1962, p. 140) suggests a possible correla
tion between the Deep Springs Formation in the White-Inyo
Mountains and the Johnnie Formation in the Death Valley
area. A correlation is proposed by McKee and Moiola
104
(1962, p. 532),between the Deep Springs Formation in
Esmeralda County, Nevada and the Johnnie Formation*
Stewart (1965, p* 70) Indicates a possible correlation be
tween the Johnnie Formation and portions of the Wyman
Formation in the White-Inyo Mountains. The Johnnie Forma
tion is herein correlated with the Deep Springs Formation
(PI. XIII).
Correlations of the Johnnie Formation in the Death
Valley area are commonly based on the occurrence of an
oolitic dolomite bed which is present in the upper portion
of the formation (Stewart, 1966, p. 70; Wright and Troxel,
1966, pp. 850 and 851). The Deep Springs Formation con
tains a number of oolitic, dolomitic limestone beds
throughout and has an uppermost dolomite which is locally
oolitic.
The Deep Springs Formation also occupies a similar
stratigraphic position to that of the Johnnie Formation;
both are overlain by a quartzitic sandstone sequence and
underlain by thick dolomite sequences. In addition,
Hazzard (1937» PP* 279 and 305-306) places a possible un
conformity between the Johnnie Formation and overlying
Sterling Quartzite in the Nopah-Resting Springs Range.
Maxson (1934, p. 310; 1935> P* 314) places a possible un
conformity between the Deep Springs Formation and the
overlying Campito Formation in the White Mountains.
These similarities between the Johnnie Formation and
105
the Deep Springs Formation, though not conclusive, indi
cate a basis for correlating between these two formations.
No strata correlative with the Johnnie Formation is recog
nized in the Providence or Marble Mountain regions.
STERLING QUARTZITE
A possible correlation between the Sterling
Quartzite in the Death Valley area, the Campito Formation
in the White-Inyo Mountains and the Prospect Mountain
Quartzite in Nevada and southeast of the Death Valley area
has been proposed by Wheeler (194-8, p. 19). McKee and
Moiola (1962, p. 534-) suggest a correlation of the
Campito Formation in Esmeralda County, Nevada and portions
of the Wood Canyon Formation in the Nopah Range. Stewart
(1965, P* 70) correlates the lower Sterling Quartzite with
the upper Wyman Formation and the upper Sterling Quartzite
with the Reed Dolomite. The Sterling Quartzite is herein
considered to be correlative with the Andrews Mountain
Member of the Campito Formation in the White-Inyo Mountains
(PI. XIII).
Stewart based his correlation on the occurrence,
at Bare Mountain, Nevada, of a dolomite member (his
member D) in the upper half of the Sterling Quartzite.
This dolomite is overlain by a quartzite member (his member
E) which is the uppermost member of the Sterling Quartzite.
Stewart correlates the dolomite member with the lower Reed
106
Dolomite and the overlying quartzite member with the Hines
Tongue Member of the Reed Dolomite in the White-Inyo
Mountains, However, the dolomite member described by
Stewart is not present in the Sterling Quartzite in the
southern Panamint Range (Hunt and Mabey, 1966, pp. 20-22),
which is as close, if not a few miles closer, to the out
crops of the Campito Formation in the White-Inyo Mountains
than is the Bare Mountain area. The writer equates the
Sterling Quartzite in southern Panamint Range with the
Andrews Mountain Member of the Campito Formation in the
White-Inyo Mountains and considers the dolomite member
present at Bare Mountain to be a facies of the central
shaly portion of the Sterling Quartzite in the southern
Panamint Range. This possible correlation between the
Sterling Quartzite and the Andrews Mountain Member of the
Campito Formation is implied by their similar strati-
graphic position and similarity in composition. The
Sterling Quartzite contains a basal conglomerate composed
primarily of milky quartz pebbles and occasional jasperoid
pebbles. Although no conglomerates were observed in the
Campito Formation, the overall composition of this forma
tion is reported by Blanc (1958, p. 14) to be 82-87 per
cent quartz and chert.
The absence of the Heinz Tongue Member in the Reed
Dolomite in Esmeralda County, Nevada (McKee and Moiola,
1962, p. 533) further supports this correlation. This
107
region is closer to the Bare Mountain, Nevada area than is
the White-Inyo Mountain area, yet lacks the quartzitic
member requisite to Stewartfs correlation.
No strata correlative with the Sterling Quartzite
are considered by the writer to be present in the
Providence or Marble Mountain regions.
WOOD CANYON FORMATION
McKee and Moiola (1962, p. 534) suggest a possible
correlation between the Wood Canyon Formation in the Nopah
Range and the Campito Formation, Poleta Formation, and
lower Harkless Formation in Esmeralda County, Nevada.
Stewart (1926, pp. 71-72) correlates the Wood Canyon
Formation with the Deep Springs Formation, Campito Forma
tion, Poleta Formation, and lower Harkless Formation in the
White-Inyo Mountains. He divides the Wood Canyon Formation
into three members and correlates the lower member with
the Deep Springs Formation, the middle member with most of
the Campito Formation, and the upper member with the
upper Campito Formation, Poleta Formation, and lower Hark
less Formation. Stewart has based his correlation on the
presence of Scolithus and archaeocyathid-bearing lime
stones which are present at both areas. The Wood Canyon
Formation in the Death Valley area is herein correlated
with the Montenegro Member of the Campito Formation, the
Poleta Formation, and the lower Harkless Formation is the
108
White-Inyo Mountains (PI. XIII).
Both of these correlated sequences contain
Scolithus, Hevadella cf. N. gracile (Walcott), and
arehaeocyathid-bearing limestones. Scolithus tubes are
common in the upper portion of the Wood Canyon Formation
(Hunt and Mabey, 1966, p. 23; Stewart, 1965, pp. 66-69)
and are also prevalent in the upper part of the. Poleta
Formation and scattered throughout the Harkless Formation
(Ross, 1965> pp. 11-12). Arehaeocyathid-bearing lime
stones occur in the upper portions of the Poleta Formation
and the lower part of the Harkless Formation as well as in
the lower member of the Poleta Formation and the upper
part of the Montenegro Member of the Campito Formation.
Stewart has correlated the arehaeocyathid-bearing lime
stones in the upper Wood Canyon Formation with those pre
sent in the lower member of the Poleta Formation. The
writer believes that these limestones in the upper Wood
Canyon Formation may better be correlated with the
arehaeocyathid-bearing limestones in the upper part of the
Poleta Formation and lower Harkless Formation, which in
both cases would mark their highest occurrence in the
sections. It is the opinion of the writer that when cor
relating these Lower Cambrian strata, the highest occur
rence of one fauna makes a better correlation horizon than
does the lowest occurrence of a fauna. For example, if a
correlation were made on the lowest occurrence of
109
Fremontla, the upper member of the Poleta Formation is the
White-Inyo Mountains would be equivalent with the Latham
Member of the Carrara Formation in the Marble Mountains,
or if based on the lowest occurrence of Paedeumias, the
lower Harkless Formation in the White-Inyo Mountains would
be correlated with the Latham Member of the Carrara Forma
tion in the Marble Mountains. However, if the correlation
was based on the uppermost occurrence of Fremontia and
Paedeumias, the Latham Member of the Carrara Formation in
the Marble Mountains correlates with the upper Harkless
Formation and Saline Valley Formation of the White-Inyo
Mountains.
The trilobite Nevadella and pelmatazoan debris are
present in the upper member of the Poleta Formation in the
White-Inyo Mountains and in the upper part of the Wood
Canyon Formation in the Death Valley area (Hazzard, 1937,
p. 278; Hunt and Mabey, 1966, pp. 22-23; Stewart, 1965, pp.
66-68; 1966, p. 71; Durham, 1967, pp. 97-98). Nevadella
occurs below the upper arehaeocyathid-bearing limestones
in the Poleta Formation and is in association with or above
these limestones in the Wood Canyon Formation. However,
it is considered probable that Nevadella moves upward in
the stratigraphic section in a southeasterly direction from
the White-Inyo Mountains, as does Fremontia and Paedumias.
In addition, the lower part of the Harkless Forma
tion in the White Mountains and in Esmeralda County,
110
Nevada, contains some oolitic and pisolitic carbonate beds
as does the uppermost part of the Wood Canyon Formation in
the southern Panamint Range (Hunt and Mabey, 1966, p. 23).
The Wood Canyon Formation is herein correlated to
the south with members A through D, this report, of the
Prospect Mountain Quartzite in the Providence Mountains
and with an undetermined thickness of the lower Prospect
Mountain Quartzite in the Marble Mountains (PI, XII). A
grit and conglomerate bed in the lower middle portion of
the Wood Canyon Formation is exposed in the Nopah Range
(Hazzard, 1937, p. 278) and in the southern Panamint
Range (Hunt and Mabey, 1966, p. 23). This grit and con
glomerate horizon is thought to be correlative with the
grit and conglomerate zone present immediately above the
base of the Prospect Mountain Quartzite in the Providence
Mountains and with the one present at the base of the
Prospect Mountain Quartzite in Marble Mountains.
ZABRISKIE QUARTZITE
A probable correlation between the Zabriskie
Quartzite in the Death Valley area and portions of the
Harkless in the White-Inyo Mountains has been suggested by
Stewart (1965* PP. 66-67; 1966, pp. 68-72). The Zabriskie
Quartzite is also correlated by McKee and Moiola (1962,
p. 535) with portions of the Harkless Formation in
Esmeralda County, Nevada. Bates (1965* PI. VIII) considers
Ill
the Zabriskie Quartzite to be correlative with the lower
part of the Saline Valley Formation in the White-Inyo
Mountains. The Zabriskie Quartzite is herein correlated
with the middle and upper part of the Harkless Formation
(PI. XIII).
The Zabriskie Quartzite and the Harkless Formation
occupy similar stratigraphic positions in that they are
the first thick quartzite unit to occur below the
girvanellid-bearing limestone, and have a similar litho-
logic composition. In addition, Scolithus tubes are common
in the Zabriskie Quartzite (Hazzard, 1937, p. 310; Hunt
and Mabey, 1966, p. 25) and they are also abundant in the
Harkless Formation (Nelson, 1962, p. 142; Ross, 1965, PP*
11-12) .
The Zabriskie Quartzite Is herein correlated to the
south with member E of the Prospect Mountain Quartzite in
the Providence Mountain and with an undetermined thickness
of the upper Prospect Mountain Quartzite in the Marble
Mountains (PI. XIII). This correlation is based upon
similarities in stratigraphic position and lithology.
CARRARA FORMATION
Correlation between the Carrara Formation of the
central part of eastern California and the Saline Valley
Formation, Mule Springs Formation, and Monola Formation in
the White-Inyo Mountains has been shown by Nelson (1963,
112
p. 30), Bates (1965, PI. VIII), Rose (1965, p. 16) and
Stewart (1965, pp. 66-67; 1966, p. 70). McKee and Molola
(1962, pp. 535-536) do not recognize the Saline Valley
Formation and Monola Formation in Esmeralda County,
Nevada. They have correlated the Carrara Formation with
the upper Harkless Formation, the Mule Springs Formation
and portions of the Emigrant Formation in their area.
The Carrara Formation is herein correlated with the upper
most Harkless Formation, Saline Valley Formation, Mule
Springs Formation, and Monola Formation in the White-Inyo
Mountains (PI. XIII).
The writer has adopted the usage of the name
Carrara Formation in place of Hazzard1s original three
formational names and has herein lowered the status of
these three formations to that of members. The Carrara
Formation is herein divided into three members, a lower
shaly sequence called the Latham Member, then a
girvanellid-bearing limestone sequence called the
Chambless Member, and an upper quartzitic sandstone, shale
and carbonate sequence called the Cadiz Member. All
three members are easily recognizable in the southern
Panamint Range, Providence Mountains, and Marble Mountains,
but are not recognized at Bare Mountain, Nevada, by Corn
wall and Kleinhampl (1961).
The Latham Member of the Carrara Formation is here
in equated with the uppermost Harkless Formation and all
113
of the Saline Valley Formation. At all five regions of
study (PI. I) these correlative units are overlain by
girvanellid-bearing limestones and underlain by quartzitic
sandstones. These correlated units also contain a
similar Lower Cambrian olenellid fauna.
The Chambless Member of the Carrara Formation is
herein correlated with the Mule Springs Formation. Both
are girvanellid-bearing limestones which contain a
Bristolia-Peachella trilobite fauna in the lower portion
(Bates, 1965, PI. VIII).
The Cadiz Member of the Carrara Formation is here
in correlated with the Monola Formation. These correlated
units are overlain by the thick carbonates of the
Bonanza King Formation and underlain by girvanellid-
bearing limestones. In addition, these two units contain
a Middle Cambrian fauna, characterized by the trilobites
Alokistocare and Glossopleura.
CONCLUSION
In southeastern California, Cambrian and Late Pre
cambrian structural features and facies patterns have
resulted in conflicting correlations of the rock units of
these ages*
As an effort toward resolving this problem, Pre
cambrian and Cambrian outcrops have been examined in the
White and Inyo Mountains, the southern Panamint Range, the
Nopah and Resting Springs Ranges, the Providence Mountains,
and the Marble Mountains. The writer has also critically
reviewed previously proposed correlations. On the basis
of field relationships, laboratory and paleontological
study, and a review of the literature, the following
formational correlations are indicated:
The Pahrump Series is correlated with the Wyman
Formation.
The Noonday Dolomite is correlated with the Reed
Dolomite.
The Johnnie Formation is correlated with the Deep
Springs Formation.
The Sterling Quartzite is correlated with the
Andrews Mountain Member of the Campito Formation.
The Wood Canyon Formation is correlated to the
north with the Montenegro Member of the Campito
Formation, the Poleta Formation, and the lower
Harkless Formation; to the east and south the
Wood Canyon Formation is correlated with portions
of the Prospect Mountain Quartzite.
The Zabriskie Quartzite is correlated northward
with the middle and upper Harkless Formation.
116
To the south and east the Zabriskie is correlated
with the upper portion of the Prospect Mountain
Quartzite.
The Carrara Formation is equated with the upper
most part of the Harkless Formation, the Saline
Valley Formation, the Mule Springs Formation and
the Monola Formation.
All nonmetamorphosed or slightly metamorphosed
strata occurring below the Olenellus zone and in sedi
mentary contact with underlying metasedimentary or
crystalline rocks have, in this report, been referred to
the Eocambrian System. The writer has also lowered the
formational status of the Latham Shale, Chambless Limestone
and Cadiz Formation of Hazzard (1933 and 1954) to members
within the Carrara Formation of Cornwall and Kleinhampl
(1961). These three members are not recognizable at the
type locality of the Carrara Formation (Cornwall and
Kleinhampl, 1961) but are present at the five regions
examined during this study. These three members are also
recognizable in parts of southwestern Nevada (Barnes and
Palmer, 1961).
The PreCambrian rocks of the Pahrump Series and the
Wyman Formation in southeastern California were deposited
in a large arcuate miogeosynclinal belt. Unconformities
between the Pahrump Series and the overlying Noonday Dolo
mite and between the Wyman Formation and overlying Reed
Dolomite show that this depositional trough was uplifted
and eroded during Late Precambrian time. Before or dur-
ing this uplift, many of the rocks filling the miogeo-_____
117'
syncline were tilted, truncated, metamorphosed and locally-
intruded by dikes and sills.
During Eocambrian time this early Cordilleran mio-
geosynclinal area began to subside and receive sediment
again. Deposition of the Noonday Dolomite and of the
Johnnie Formation conformably upon it suggests that -
deposition within the miogeosynclinal area was continuous
throughout most of the Early Eocambrian. The same rela
tionship is expressed by the Reed Dolomite and the con
formably superjacent Deep Springs Formation. A possible
disconformity between the Johnnie Formation and overlying
Sterling Quartzite and also between the Deep Springs
Formation and the overlying Campito Formation indicates
that uplift and erosion may have again taken place in
this portion of the Cordilleran miogeosyncline sometime
during the Late Eocambrian. Following this possible up
lift, subsidence and deposition reoccurred and appears to
have been continuous from Late Eocambrian time until
Middle Cambrian time. This continued subsidence and
deposition is apparent from the presence and conform-
ability of the Sterling' Quartzite, Wood Canyon Formation,
Zabriskie Quartzite, Carrara Formation and Bonanza King
Formation in the Death Valley region. This conformable
relationship is present also in correlative strata in the
White-Inyo Mountains and in the Providence and Marble
Mountains.
REFERENCES
REFERENCBS
Albers, J. P. and Stewart, J. H., 1962, Precambrian (?)
and Cambrian stratigraphy in Esmeralda County,
Nevada: U. S. Geol. Survey Prof. Paper 450-D, p.
24-27.
Anderson, G. H., 1937, Precambrian stratigraphy in the
northern Inyo Range (Abs.): Geol. Soc. America Proc.
1936, p. 61-62.
Ball, S. H., 1907, A geologic reconnaissance in south
western Nevada and eastern California; U. S. Geol.
Survey Bull. 308, p. 1-212.
Barca, R. A., 1966, Old Dad Mountain quadrangle, San
Bernardino County, California: Map Sheet 7, Calif.
Div. Mines and Geology.
Barnes, H. and Christiansen, R. L., 1967, Cambrian and
Precambrian rocks of the Groom District, Nevada,
southern Great Basin: U. S. Geol. Survey Bull. 1244-G,
P. 1-32.
Barnes, H. and Palmer, A. R., 1961, Revision of strati-
graphie nomenclature of Cambrian rocks, Nevada Test
Site, and vicinity, Nevada, in short papers in the
geologic and hydrologic sciences: U. S. Geol. Survey
Prof. Paper 424-C, p. C100-C103.
Bates, E. E., 1965, Stratigraphic analysis of the Cambrian
Carrara Formation, Death Valley region, California-
Nevada: Unpublished Masters Thesis, University of
California, Los Angeles.
Bishop, C. C., 1963, Geologic map of California, Needles
Sheet, Olaf P. Jenkins, editor: Calif. Div. Mines,
Scale 1:250,000.
Bj^alykke, Knut, 1964, The Eocambrian stratigraphy of the
B3jzfranes window and the thrusting of the Kvitubia
nappe: Norg. Geol. Unders., v. 234, p. 5-14.
Blanc, R. P., 1958* Geology of the Deep Springs Valley
area, White-Inyo Mountains, California: Unpublished
Masters Thesis, University of California, Los
Angeles.
Br^gger, W. C., 1900, Norges geologi, in Norge: det. 19,
aarhundrede. I, p. 1-32.
120
Burchfiel, B. 0., 1964, Precambrian and Paleozoic strati
graphy of Specter Range quadrangle, Bye County,
Nevada: American Assoc, Petroleum Geologists Bull.,
v. 48, no. 1, p. 40-56.
Clark, C. W., 1921, Lower and Middle Cambrian formations
of the Mojave Desert: University of California
Published Bull., Dept. Geol. Sci., v. 13, p. 1-7.
Cloud, P. E., Jr., and Nelson, C. A., 1966, Phanerozoic-
Cryptozoic and related transitions: New Evidence:
Sci., v. 154, no. 3750, p. 766-769.
Cornwall, H. R. and Kleinhampl, P. J., 1961, Geology of
the Bare Mountain quadrangle: U. S. Geological
Survey Map G.Q. 157.
Darton, N. H., 1907, Discovery of Cambrian rocks in
southeastern California: Jour. Geol., v. 15, p. 470.
Durham, J. W., 1967, Notes on the Helicoplaciodea and
early Echinoderms: Jour. Poleo., v. 41, no. 1, p.
97-102.
Durham, J. W. and Caster, K. E., 1963, Helicoplacoidea;
A new class of Echinoderms: Sci., v. 140, no. 3568,
p. 820-822.
Fleming, W. L. S. and Edmons, J. M., 1941, Hecla Hoek
Rocks of New Friesland (Spitsbergen): Geol. Mag., v.
78, p. 405-428.
Friedman, G. M., 1959, Identification of carbonate
minerals by staining methods: Jour. Sedimentary
Petrology, v. 29, p. 87-97.
Gilbert, G. K., 1875, Report on the geology of portions
of Nevada, Utah, California, and Arizona, examined
in the years 1871 and 1872: U. S. Geog. and Geol.
Surveys W. 100th Meridian (Wheeler), v. 3, p. 17-187.
Glaessner, M. F., 1958, The oldest fossil faunas of South
Australia: Geologische Rundschau, v. 47, p. 522-531.
Glaessner, M. F., 1961, Pre-Cambrian animals: Scientific
American Reprint, No. 837, p. 1-8.
Glaessner, M. F. and Daily, B., 1959, The geology and
Late Precambrian Fauna of Ediacara Fossil Reserve:
Rec. So. Aust. Mus., v. 8.
121
Hague, A., 1883* Abstract of report on the geology of the
Eureka District, Nevada: U. S. Geol, Survey, 3d Ann.
Report, p. 237-290.
Hague, A., 1892, Geology of the Eureka District, Nevada:
U. S. Geol. Survey Monograph 20.
Harland, W. B., Wallis, R. H., and Gayer, R. A., 1966, A
revision of the Lower Hecla Hoek Succession in
central north Spitsbergen and correlations elsewhere:
Geol. Mag., v. 103, no. 1, p. 70-97.
Hazzard, J. C., 1937, Paleozoic section in the Nopah and
Resting Springs Mountains, Inyo County, California:
Calif. Jour. Mines and Geol., Rept. 33, p. 273-339.
Hazzard, J. C., 1937, Cambrian “Girvanella1 1 from the
southern Great Basin region (Abs.): Geol. Soc.
America Proc. 1936, p. 354—355-
Hazzard, J. C., 1938, Paleozoic section in the Providence
Mountains, San Bernardino County, California (Abs.):
Geol. Soc. America, Proc. 1937, p. 240-241.
Hazzard, J. C., 1941, Faulting in the northern Providence
Mountains, San Bernardino County, Califomia (Abs.):
Geol. Soc. America Bull., v. 52, p. 1951*
Hazzard, J. C., 1954, Rocks and structure of the northern
Providence Mountains, San Bernardino County, Cali
fornia, (pt.) 10 in Chap. 4 of Jahns, R. H. editor,
Geology of southern California: Calif. Div. Mines
Bull. 170, p. 27-35.
Hazzard, J. C., and Crickmay, C. H., 1933, Notes on the
Cambrian rocks of the eastern Mojave Desert, Cali
fornia, with a paleontological report: University
of California Publ. Bull., Dept. Geol. Sci., V. 23,
no. 2, p. 57-80.
Hazzard, J. C. and Mason, J. F., 1936, Middle Cambrian
formations of the Providence and Marble Mountains,
California: Geol. Soc. America Bull., v. 47, no. 2,
p. 229-240.
Hernes, I., 1967, The Late Pre-Cambrian stratigraphic
sequence in the Scandinavian mountain chain: Geol.
Mag., v. 104, no. 6, p. 557-563.
122
Hewett, D. F., 1940, Hew formation names to be used in the
Kingston Range, Ivanpah quadrangle, California:
Washington Acad. Sci. Jour., v. 30, p. 239-240.
Hewett, D. F., 1956, Geology and mineral resources of
the Ivanpah quadrangle, California and Nevada: U. S.
Geol. Survey Prof. Paper 275, p. 1-172.
Holtedahl, 0., 1922, A tillite-like conglomerate in the
Eocambrian Sparagmites of southern Norway: American
Jour., Sci., v. 4, p. 165-173.
Hopper, R. H., 1947, Geologic section from the Sierra
Nevada to Death Valley, California: Geol. Soc.
America Bull., v. 58, p. 393-432.
Howell, B. F., 194-4, Correlation of the Cambrian forma
tions of North America: Geol. Soc. American Bull.,
v. 55, p. 993-1044.
Hunt, C. B. and Mabey, D. R., 1966, Stratigraphy and
structure, Death Valley, California: U. S. Geol.
Survey Prof. Paper 494-A, p. 11-28.
Hussey, R. C., 194-7, Historical geology, The geologic
history of North America: McGraw-Hill Book Co.,
Inc., New York, N. Y.
Jennings, C. W., 1958, Geologic map of California, Death
Valley sheet; Olaf P. Jenkins, editor: California
Div. Mines, Seale 1:250,000.
Jennings, C. W., 1961, Geologic map of California,
Kingman sheet, Olaf P. Jenkins, editor: California
Div. Mines, Seale 1:250,000.
Jennings, C. W., Burnett, J. L., and Troxel, B., 1962,
Geologic map of California, Trona sheet, Olaf P.
Jenkins, editor: California Div. Mines, Scale
1: 250, 000.
Johnson, B. K., 1957, Geology of a part of the Manly Peak
quadrangle, southern Panamint Range, California:
University of California Published Bull. Dept. Geol.
Sci., v. 30, no. 5, p. 353-424.
Johnson, J. H., 1966, A review of the Cambrian algae:
Quarterly Bull., Colorado School Mines, v. 61, no. 1,
162 p.
123
Killian, H. M., 1964, Geology of the Marble Mountains,
San Bernardino County, California: Unpublished
Masters Thesis, University of Southern California,
112 p.
Knopf, A., 1918, Inyo Range and the eastern slope of the
southern Sierra Nevada, California: U. S. Geol,
Survey Prof, Paper 110,
Kummel, 1961, History of the earth: W. H. Freeman and
Company, San Francisco and London,
Lochman, C., 1947, Analysis and revision of eleven
lower Cambrian trilobite genera: Jour, Paleo., v,
21, no. 1, p, 55-71.
Lockman-Balk, C. and Wilson, J. L., 1958, Cambrian bio
stratigraphy in North America: Jour. Paleo., v. 32,
no. 2, p. 312-315.
Longwell, C. R., 1'952, Lower limit of the Cambrian in the
Cordilleran region: Washington Acad. Sci. Jour., v.
42, p. 107-118.
Mason, J. F., 1935> Fauna of the Cambrian Cadiz Forma
tion, Marble Mountains, California: So. Calif. Acad.
Sci. Bull., v. 34, p. 97-119.
Mason, J. F., 1948, Geology of the Tecopa area, south
eastern California: Geol. Soc. America Bull., v. 59>
p. 333-352.
Mason, J. F., Longwell, C. R., and Hazzard, J. C., 1937 >
Sequence of Cambrian faunas in the southern Great
Basin (Abs.): Geol. Soc. America Proc. 1936, p.
366-367.
Maxson, J. H., 1934, Precambrian stratigraphy of the Inyo
Range: Pan. American Geol., v. 61, p. 310-311.
Maxson, J. H., 1935, Precambrian stratigraphy of the Inyo
Range: (Abs.): Geol. Soc. America Proc. 1934, p.
314.
McKee, E. H. and Moiola, R. J., 1962, Precambrian and
Cambrian rocks of south central Esmeralda County,
Nevada: American Jour. Sci., v. 210, p. 530-538.
Miller, W. J., 1952, An introduction to historical
geology with special reference to North America:
D. Van Nostrand Co., Inc.
124
Moore, R. C., editor, 1955* Treatise on invertebrate
paleontology, Part E, Archaeocyatha, Porifera:
Lawrence, Kansas, Univ. Kansas Press, 22 p.
Moore, R. 0., editor, 1959* Treatise on invertebrate
paleontology, Part 0, Arthropoda Is Lawrence, Kansas,
Univ. Kansas Press, 560 p.
Moore, R. C., editor, 1962, Treatise on invertebrate
paleontology, Part W, Miscellanea: Lawrence, Kansas,
Univ. Kansas Press, 259 P*
Moore, R. 0., editor, 1965* Treatise on invertebrate
paleontology, Part H, Brachiopoda: Lawrence, Kansas,
Univ. Kansas Press, v. 2, 927 p.
Moore, R. C., editor, 1966, Treatise on invertebrate
paleontology, Part U, Echinodermata: Lawrence,
Kansas, Univ. Kansas Press, v. 2, 695 p.
Murphy, P. M., 1932, Geology of a part of the Panamint
Range, California: Calif. State Mining Bur., Mining
in Calif., v. 28, p. 329-355.
Kelson, C., 1957, Waucoban stratigraphy, Inyo Mountains,
California (Abs.): Geol. Soc. America Bull., v. 68,
p. 1838.
Kelson, C. A., 1962, Age of the Johnnie Formation (Abs.):
Geol. Soc. America Spec. Paper 68, p. 45-46.
Kelson, C. A., 1962, Lower Cambrian— Precambrian succes
sion, White-Inyo Mountains, California: Geol. Soc.
America Bull., v. 73, p. 139-144.
Kelson, C. A., 1963, Stratigraphic range of Qgygopsis:
Jour. Paleo., v. 37, no. 1, p. 244-248.
Kelson, C. A., 1963, Preliminary geologic map of the
Blanco Mountain quadrangle, Inyo and Mono Counties,
California: U. S. Geol. Survey Min. Inv. Field
Studies Map MF-256, Scale 1:48,000.
Kelson, C. A., 1965, Monola Formation in Cohee and West,
changes in stratigraphic nomenclature by the U. S.
Geol. Survey, 1963: U. S. Geol. Survey Bull., no.
1194-A.
Kelson, C. A., 1966, Geologic map of the Waucoba Mountain
quadrangle, Inyo County, California: U. S. Geol.
Survey Map GQ-528, Scale 1:62,500.
125
Nelson, C. A. and Perry, L. J., 1955, Late Precambrian-
Early Cambrian strata, White-Inyo Mountains, Cali
fornia (Abs.): Geol. Soc. America Bull., v. 66, p.
1657-1658.
Nicol, D., 1966, Cope’s rule and Precambrian and Cambrian
invertebrates: Jour. Paleo., v. 40, no. 6, p.
1397-1399.
Noble, L. P., 1934, Rock formations of Death Valley,
California: Science, N. S., v. 80, no. 2069, p.
173-178.
Noble, L. F. .-and Wright, L. A., 1954, Geology of the
central and southern Death Valley region, California,
(pt.) 10 in Chap. 2 of Jahns, R. H., editor, Geology
of southern California: Calif. Div. Mines Bull. 170,
p. 143-160.
Nolan, T. B., 1929, Notes on the stratigraphy and
structure of the northwest portion of Spring
Mountains, Nevada: American Jour. Sci., 5th Ser.,
v. 17, no. 101, p. 461-472.
Palmer, A. R.^and Hazzard, J. C., 1956, Age and correla
tion of Cornfield Springs and Bonanza King Formations
in southeastern California and southern Nevada:
American Assoc. Petroleum Geol. Bull., v. 40, no. 10,
p. 2494-2499.
Pesci, R. C., Scholl, D. W., Scales, F. H. H., and Libby,
F. J., 1955» Archaeocyathid localities in the Waueoba
type section, California: The Compass, v. 32, no. 3,
p. 195-197.
Resser, C. E., 1928, Cambrian fossils from the Mojave
Desert: Smith, Misc. Coll., v. 81, no. 2, p. 1-14.
Riccio, J. F., 1949, Lower Cambrian fauna of the Marble
Mountains, California: The Compass, v. 26, no. 4,
P. 354-359.
Riccio, J. F., 1962, The Lower Cambrian Olenellidae of
the southern Marble Mountains, California: Bull.,
So. Calif. Acad. Sci., v. 51> part 2, p. 25-49.
Ross, D. C., 1965> Geology of the Independence quadrangle,
Inyo County, California: U. S. Geol. Survey Bull.
1181-0, p. 6-17.
126
Rozanov, A. Yu,, 1967, The Cambrian lower boundary
problem: Geol. Mag,, v. 104, no. 5, P* 415-434.
Sears, D. H., 1955, Geology of the central Panamint Range,
California: American Assoc. Petroleum Geol. Bull.,
v. 39, no. 1, p. 140.
Skjeseth, S., 1963, Contributions to the geology of the
Mj^sa Districts and the classical Sparagmite area in
southern Norway: Norg. Geol. Unders., v. 220, 126 p.
Spurr, J. E., 1903, Descriptive geology of Nevada south
of the fortieth parallel and adjacent portions of
California: U. S. Geol. Survey Bull. 208.
Stewart, J. H., 1965, Precambrian and Lower Cambrian
formations in the Last Chance Range area, Inyo County,
California: U. S. Geol. Survey Bull. 1224-A, p.
A60-A70.
Stewart, J. H., 1966, Correlation of Lower Cambrian and
some Precambrian strata in the southern Great Basin,
California and Nevada: U. S. Geol. Survey Prof.
Paper 550-C, p. 66-72.
Stewart, J. H. and Barnes, H., 1966, Precambrian and
Lower Cambrian formations in the Desert Range, Clark
County, Nevada; in Cohee, G. V. and West, W. S.,
Changes in stratigraphic nomenclature by the U. S.
Geological Survey, 1965s U. S. Geol. Survey Bull.
1244-A, p. A35-A42.
Stoyanow, A., 1958, Sonoraspis and Albertella in the
Inyo Mountains, California: Geol. Soc. America
Bull., v. 69, p. 347-352, 1 pi.
Stoyanow, A. and Susuki, T., 1955, Discovery of Sonoraspis
in southern California: Geol. Soc. America Bull.,
v. 66, p. 467-470.
Taylor, M. B., 1966, Precambrian Metazoan (?) fossils
from Inyo County, California (Abs.): Proc. of 1966
Annual Meeting for the Geol. Soc. America, Rocky Mtn.
Sec., p. 59-
Turner, H. W., 1909, Contribution to the geology of the
Silver Peak quadrangle, Nevada: Geol. Soc. America
Bull., v. 20, p. 223-264.
12?
Vogt, T., 1924, The relation between the Sparagmitian
System and marine Lower Cambrian at Lake Mjjzfsen: Norg.
Geol. Unders., v. 7, p. 281-384.
Walcott, C., 1891, The Cambrian group of rocks in North
America: Geol. Soc. America Bull., v. 81, p.
313-325.
Walcott, C., 1908, Cambrian sections of the Cordilleran
area: Smithsonian Misc. Coll., v. 53, no. 5, P*
167-230.
Wheeler, H. E., 1943, Lower and Middle Cambrian strati
graphy in the Great Basin area: Geol. Soc. America
Bull., v. 54, p. 1781-1822.
Wheeler, H. E., 1947, Base of the Cambrian system: Jour.
Geol., v. 55, no. 3, p. 153-159.
Wheeler, H. E., 1948, Late Precambrian-Cambrian strati
graphic cross section through southern Nevada:
Univ. Nev. Bull., v. 42, no. 3, Geol. and Min. Ser.,
no. 47, 58 p.
Wilhelms, D. E., 1963, Geology of part of the Nopah and
Resting Springs Ranges, Inyo County, California:
Unpublished Doctoral Dissertation, University of
California, Los Angeles, LD 791*9, U3W 649.
Wright, L. A. and Troxel, B. W., 1966, Strata of Late
Precambrian-Cambrian age, Death Valley region,
Califomia-Nevada: American Assoc. Petroleum Geol.
Bull., v. 50, no. 5, P* 846-857.
Wright, L. A. and Troxel, B. W., 1967, Limitations on
right-lateral, strike-slip displacement, Death
Valley and Furnace Creek fault zones, California:
Geol. Soc. America Bull., v. 78, no. 8, p. 933-950.
APPENDIX
Plates XIV through XV
Fossil Photographs
Figure
Figure
. Figure
Figure
Figure
Figure
Figure
129
White Mountain Area Lower Cambrian fauna
Plate XIV
•— Fallotaspis sp. (X 1/2) from the Montenegro
Member of the Campito Formation, NE4NE4 Sec,
22, T7S, R35E, Blanco Mountain quadrangle.
•— Nevadia sp, (X l/2) from the Montenegro
Member of the Campito Formation, NE4NE4 Sec.
22, T7S, R35E> Blanco Mountain quadrangle.
• — Fremontia sp. (X 2) from the upper member of
the Poleta Formation, NW4JPJ4 See. 4, T8S,
R35E, Blanco Mountain quadrangle.
•— Bonnia ? sp. (X 3) from the upper member of
the Poleta Formation, NW4NE4 Sec. 4, T8S, R35E,
Blanco Mountain quadrangle.
.— Onchocephalus ? sp. (X 3) from the upper
member of the Poleta Formation, NW4NE4 Sec. 4,
T8S, R35E, Blanco Mountain quadrangle.
• — Algal ? pisolitic limestone (X 1) from the
lower portion of the Harkless Formation,
EW4NE4 Sec. 35, T7S, R35E, Blanco Mountain
quadrangle.
• — Archaeocyathids (X 5) from the lower member
of the Poleta Formation, SW4NW4 Sec. 4, T8S,
R35E, Blanco Mountain quadrangle.
130
Fig. 7
P la te ;XIV
k
131
White Mountain Area Lower Cambrian fauna
Plate XV
Figure 1.— Nevadella cf. N. gracile (Walcott) (X 2) from
the upper member of the Poleta Formation,
NE4SE4 Sec. T8S, R35E> Blanco Mountain
quadrangle.
Figure 2.— Helicoplacus sp. (X 3) from the upper member
of the Poleta Formation, NE4SE4 Sec. 5, T8S,
R35E, Blanco Mountain quadrangle.
132
Fig, 1
t r j - % 'm
«■ I ! ' > /// / • ' , ‘ it
WHITE-INYO MOUNTAINS
(After Nelson, 1962
and Ross, 1965)
PANAMINT RANGE
(After Hunt
and
Mabey, 1966)
NOPAH-RESTING SPRINGS RANGE
(After Hazzard, 1937)
PROVIDENCE MOUNTAINS
MARBLE MOUNTAINS
(After Clark, 1921
and Hazzard, 1933)
S 42° E
X
S 58° E S 30 E
>-<
S 5 E
u a tu m : Base o f th e Bonanza King F o rm a tio n
CORRELATION PLATE
Explanatio n
Possible Unconformity
Legend For Correlation Chart
G ms
Gc m
Pahrump Series
Precambrian M e ta s e d im e n ta ry Rocks
Cambrian
Monola Formation
Mule Springs Formation
Saline Valley Formation
Harkless Formation
Poleta Formation
Campito Formation, Montenegro Member
Carrara Formation
Zabriskie Quartzite
Wood Canyon Formation
Eocambrian
Campito Formation, Andrews Mountain Member
Deep Springs Formation
Reed Dolomite
Sterling Quartzite
Johnnie Formation
Noonday Dolomite
Prospect Mountain Quartzite
F2
Shale
Conglomerate Limestone Silty
Limestone
Sandy
Dolomite
Siltstone
Quartsitic
Sandstone
Sandy
Limestone
Dolomite Silty
Dolomite
Scale
H o riz o n ta l, 1"= 6 m i.; V ertical, 1''=1 0 0 0'
1. Section from top of Reed Dolomite to base of Harkless
Formation measured by the writer in Westgard Pass area.
2. Section from lower Johnnie Formation to top of the Wood
Canyon Formation reconnaissance studied and the Zabriskie
Quartzite and lower Carrara Formation measured by the
writer in 3. Section from base of Zabriskie Quartzite to the top of
the Carrara Formation measured by the writer in the
southern Resting s nrlnrrs Ran re.
— ■*.----o o
4. Measured by the writer in the area of South Hayden Wash.
5. Section from crystalline basement to the top of the
Carrara Formation remeasured by the writer near the
area of Chambless.
W yman Form ation
Plate XIII

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Fourier grain-shape analysis of quartz sand from the eastern and central Santa Barbara littoral cell, Southern California

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Geology of the central part of the Clark Mountain Range, San Bernardino County, California

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Structural geology of a portion of the eastern Rand Mountains, Kern and San Bernardino counties, California

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Foraminiferal trends and paleo-oceanography in Late Pleistocene-recent cores, Tanner Basin, California

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Geology of the coastal portion of the San Luis Range, San Luis Obispo County, California

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Structural geology of the eastern Whipple Mountains, San Bernandino County, California

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Hydrogeology of La Habra Ground Water Basin, California

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Sedimentology of the Beck Spring Dolomite, eastern Mojave Desert, California

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Groundwater geology and hydrology of the Great Divide and Washakie Basins South Central Wyoming

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Temporal and spatial distribution of basin-range faulting in Nevada and Utah.

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An analysis of sedimentation rates and cyclicity in the laminated sediments of Santa Monica Basin, California Continental Borderland.

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Hydrogeologic investigation of Carpinteria ground water basin, Santa Barbara County, California

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Magnetostratigraphy of Peninsular Ranges Terrane Upper Cretaceous strata: Point Loma Formation, San Diego, California

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Heavy mineral correlation of Pleistocene acquifer materials of the Los Angeles basin, a feasibility investigation

Asset Metadata

Creator Quinn, Harry M (author)

Core Title Precambrian, Eocambrian, and Cambrian rocks of the Basin and Range Province of Eastern California

Degree Master of Science

Publisher University of Southern California (original), University of Southern California. Libraries (digital)

Tag Geology,OAI-PMH Harvest

Language English

Contributor Digitized by ProQuest (provenance)

Permanent Link (DOI) https://doi.org/10.25549/usctheses-c30-112200

Unique identifier UC11225366

Identifier usctheses-c30-112200 (legacy record id)

Legacy Identifier EP58567.pdf

Dmrecord 112200

Document Type Thesis

Rights Quinn, Harry M.

Type texts

Source University of Southern California (contributing entity), University of Southern California Dissertations and Theses (collection)

Access Conditions The author retains rights to his/her dissertation, thesis or other graduate work according to U.S. copyright law. Electronic access is being provided by the USC Libraries in agreement with the au...

Repository Name University of Southern California Digital Library

Repository Location USC Digital Library, University of Southern California, University Park Campus, Los Angeles, California 90089, USA