Mineral Resources of the Sacatar Meadows 

Wilderness Study Area, Tulare and 

Inyo Counties, California

U.S. GEOLOGICAL SURVEY BULLETIN 1705-D

Chapter D

Mineral Resources of the

Sacatar Meadows Wilderness Study Area,

Tulare and Inyo Counties, California

By MICHAEL F. DIGGLES, JAMES G. FRISKEN, 

and ANDREW GRISCOM 

U.S. Geological Survey

LUCIA KUIZON 

U.S. Bureau of Mines

U.S. GEOLOGICAL SURVEY BULLETIN 1705

MINERAL RESOURCES OF WILDERNESS STUDY AREAS: 

SOUTH-CENTRAL CALIFORNIA
DEPARTMENT OF THE INTERIOR 

DONALD PAUL MODEL, Secretary

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1988

For sale by the

Books and Open-File Reports Section

U.S. Geological Survey

Federal Center, Box 25425

Denver, CO 80225

Library of Congress Cataloging-in-Publication Data

Mineral resources of the Sacatar Meadows Wilderness Study 

Area, Tulare and Inyo Counties, California.

U.S. Geological Survey Bulletin 1705-D

Bibliography

Supt. of Docs. No.: I 19.3:1705-0

1. Mines and mineral resources California Sacatar

Meadows Wilderness. 2. Sacatar Meadows Wilderness

(Calif.) I. Diggles, M.F. II. Series.

QE75.B9 No. 1705-D 557.3s 87-600425 

[TN24.C2] [553'.09794'95]
STUDIES RELATED TO WILDERNESS

Bureau of Land Management Wilderness Study Area

The Federal Land Policy and Management Act (Public Law 94-579, October 21,1976) 

requires the U.S. Geological Survey and U.S. Bureau of Mines to conduct mineral surveys on 

certain areas to determine the mineral values, if any, that may be present. Results must be made 

available to the public and be submitted to the President and the Congress. This report presents the 

results of a mineral survey of part of the Sacatar Meadows (CA-010-027) Wilderness Study Area, 

Tulare and Inyo Counties, California.

CONTENTS

Summary Dl

Abstract 1

Character and setting 1 

Identified mineral resources 1 

Mineral resource potential 1 

Introduction 3

Location and physiography 3 

Procedures 3 

Previous studies 3 

Acknowledgments 5 

Appraisal of identified resources 5

Mining and mineral exploration history 5 

Identified resources 6 

Assessment of mineral resource potential 6 

Geology 6

Jurassic or older metamorphic rocks 6

Granitic rocks 7

Quaternary surficial deposits 7

Structure 7 

Geochemistry 7

Methods 7

Results and interpretation 7 

Geophysics 9

Aeromagnetic data 9

Gamma-ray survey 9

Remote sensing 10 

Mineral resource potential 10 

References cited 11 

Appendixes

Definition of levels of mineral resource potential and certainty of

assessment 17

Resource/reserve classification 18 

Geologic time chart 19

FIGURES

1. Index map showing location of the Sacatar Meadows Wilderness Study 

Area, Tulare and Inyo Counties, California D2

2. Mineral resource potential and generalized geology of the Sacatar Meadows 

Wilderness Study Area, Tulare and Inyo Counties, California 4

Contents V

MINERAL RESOURCES OF WILDERNESS STUDY AREAS: 

SOUTH-CENTRAL CALIFORNIA

Mineral Resources of the

Sacatar Meadows Wilderness Study Area,

Tulare and Inyo Counties, California

By Michael F. Diggles, James G. Frisken,anc/ Andrew Griscom 

U.S. Geological Survey

Lucia Kuizon

U.S. Bureau of Mines

SUMMARY 

Abstract

At the request of the U.S. Bureau of Land Management, approximately 11,447 acres of the Sacatar Meadows Wilderness 

Study Area (CA-010-027) were evaluated for mineral resources 

(known) and mineral resource potential (undiscovered). In this 

report, the area studied is referred to as the "wilderness study 

area" or simply "the study area"; any reference to the Sacatar 

Meadows Wilderness Study Area refers only to that part of the 

wilderness study area for which a mineral survey was requested 

by the U.S. Bureau of Land Management. Field work was 

conducted in 1984 through 1987 to assess the mineral resources 

(known) and resource potential (undiscovered) of the area. No 

mineral resources were identified.

There are five areas of low mineral resource potential in and 

near the Sacatar Meadows Wilderness Study Area. The ridge 

northwest of Big Pine Meadow, outside the study area, has low 

mineral resource potential for tungsten and molybdenum possibly in skarn. The hillside southeast of Scodie Meadow has low 

mineral resource potential for tungsten and molybdenum possibly in skarn. The valley east of Long Canyon, the small drainage 

northeast of Sacatar Meadow, and the area southeast of Big Pine 

Meadow have low mineral resource potential for tungsten 

possibly in skarn within granitoid rocks. The area has no 

geothermal energy, energy mineral, or oil and gas resource 

potential.

Character and Setting

The Sacatar Meadows Wilderness Study Area is approximately 11,447 acres in size and is 5 mi southwest of Coso 

Junction, Calif, (fig. 1). The terrane is generally steep and

rugged, with elevations ranging from about 6,200 ft at Chimney Meadow to about 8,800 ft at unnamed points along the 

crest of the S ierra Nevada in the northern part of the study area. 

Access into the study area is by private roads from the 

Ninemile Canyon Road (County Road J41) off U. S. Highway 

395.

Most of the area is underlain by plutonic rocks of the Sierra 

Nevada batholith. The oldest rocks in the area are Jurassic or 

older (see appendix for Geologic Time Chart) metamorphosed sedimentary rocks composed of quartz-mica schist 

and quartzite. These are intruded by the oldest intrusive rocks 

in the study area, which are Triassic and (or) Jurassic gabbros 

and diorites. A younger set of more mafic granitic rocks of 

Jurassic age that are granodioritic to tonalitic in composition 

dominate the study area. The youngest rocks in the study area 

are leucocratic, nonfoliated Cretaceous granites, alaskites, 

aplites, and pegmatites.

Identified Mineral Resources

There are no identified mineral resources in the Sacatar 

Meadows Wilderness Study Area. In 1984, U.S. Bureau of 

Mines personnel conducted a mineral appraisal of the study 

area. During this study, no mines or prospects were found and 

no mining claims or leases were current in or near the study 

area.

Mineral Resource Potential

Within and near the study area, five areas have low 

mineral resource potential (fig. 2) on the basis of analytical

Mineral Resources of the Sacatar Meadows Wilderness Study Area D1
118°00'

36°00'

35°45'

Monache 

Mtn

CALlC

Haiwee

Reservoir

AREA OF MAP

012345 MILES

APPROXIMATE BOUNDARY OF

SACATAR MEADOWS 

WILDERNESS STUDY AREA

tle

Pearsonville

Figure 1. Index map showing location of the Sacatar Meadows Wilderness Study Area, Tulare and Inyo Counties, California.

D2 Mineral Resources of Wilderness Study Areas South-Central California
results of geochemical sample collection; all five areas may be 

related to unmapped small pods of skarn. The five areas, the 

host rock, and associated commodity of each are as follows: 

(1) ridge northwest of Big Pine Meadow, outside the study 

area; metasedimentary rocks of the Kernville Series; tungsten 

and molybdenum, (2) hillside southeast of Scodie Meadow 

and nearby Deadfoot Canyon; granodiorite and quartz diorite; 

tungsten and molybdenum, (3) valley east of Long Canyon; 

quartz diorite; tungsten, (4) small drainage northeast of 

Sacatar Meadow; quartz diorite; tungsten, (5) area southeast 

of Big Pine Meadow; quartz diorite; tungsten.

The wilderness study area has no geothermal energy, 

energy mineral, or oil and gas resource potential.

INTRODUCTION

This mineral survey was requested by the U.S. Bureau of 

Land Management and is the result of a cooperative effort by 

the U.S. Geological Survey and the U.S. Bureau of Mines. An 

introduction to the wilderness review process, mineral survey 

methods, and agency responsibilities was provided by 

Beikman and others (1983). The U.S. Bureau of Mines 

evaluates identified resources at individual mines and known 

mineralized areas by collecting data on current and past 

mining activities and through field examination of mines, 

prospects, claims, and mineralized areas. Identified resources 

are classified according to the system described by U.S. 

Bureau of Mines and U.S. Geological Survey (1980). Studies 

by the U.S. Geological Survey are designed to provide a 

reasonable scientific basis for assessing the potential for 

undiscovered mineral resources by determining geologic 

units and structures, possible environments of mineral deposition, presence of geochemical and geophysical anomalies, 

and applicable ore-deposit models. Mineral assessment 

methodology and terminology as they apply to these surveys 

were discussed by Goudarzi (1984). See the appendixes for 

the definition of levels of mineral resource potential, certainty 

of assessment, and classification of identified resources.

Location and Physiography

The Sacatar Meadows Wilderness Study Area (CA-010- 

027) comprises 11,447 acres in the Sierra Nevada physiographic province. It is situated mostly in the southeast corner of 

Tulare County, about 5 mi southwest of Coso Junction. The 

east boundary generally follows the Tulare-Inyo County line 

along the crest of the Sierra Nevada. Elevations in the study 

area range from about 6,200 ft at Chimney Meadow to about 

8,800 ft along the crest of the Sierra Nevada in the northern 

part of the study area.

Climate in the southern Sierra Nevada is classified as 

highland type, where precipitation averages 20 to 40 in. per 

year on the western slope and 12 to 20 in. per year on the 

eastern slope and supports vegetation of the Sonoran and

Transition Zones (Storer and Usinger, 1963). Higher ground 

has the greatest precipitation and is covered by vegetation of 

the Transition Zone, principally Jeffrey pine, incense cedar, 

black oak, ceanothus, and, on the west side of Long Canyon, 

on the north side of Lament Peak, rare sugar pine. The middle 

elevations are in the Upper Sonoran Zone and support pinon 

and digger pine, live oak, ceanothus, manzanita, and chinquapin. On the dryer lower slopes, the vegetation is typically 

lower Sonoran sagebrush and mountain mahogany.

Procedures

The U.S. Geological Survey conducted detailed field investigations of the Sacatar Meadows Wilderness Study Area 

in the spring and summer of 1985 with follow-up work in the 

summers of 1986 and 1987. This work included geologic 

mapping at a scale of 1:24,000, field checks of existing 

geologic maps, geochemical sampling, and the examination 

of outcrops for the tungsten-bearing mineral scheelite using 

ultraviolet lamps. Adrian and others (1987) presented the data 

from the U.S. Geological Survey stream-sediment samplecollection program for this study. The U.S. Bureau of Mines 

examined the Sacatar Meadows Wilderness Study Area in 

October 1984 for this study. During this survey, areas likely 

to contain mineralized rock were examined, sampled where 

warranted, and routinely checked for radioactivity with a 

scintillometer. Office studies, completed prior to the field 

study, included a review of literature andU.S. Bureau of Land 

Management mining claim records. One placer and four rock 

samples were collected from the study area during the U.S. 

Bureau of Mines' field studies. The rock samples were 

analyzed by fire-assay/inductively coupled-plasma (ICP) for 

gold and silver and analyzed spectrographically for 40 elements including antimony, barium, cadmium, cobalt, chromium, copper, gold, iron, lead, lithium, magnesium, manganese, molybdenum, nickel, platinum, silver, tin, titanium, 

vanadium, and zinc. The placer sample was chemically 

analyzed for uranium and analyzed by a radiometric method 

for thorium.

Previous Studies

Kuizon (1985) presented the results of a mineral resource 

appraisal. Aeromagnetic data were collected for the U.S. 

Geological Survey in 1981 (U.S. Geological Survey, 1982). 

Smith (1964) and Matthews and Burnett (1966) compiled the 

regional geology of the Bakersfield and Fresno 1° by 2° sheets, 

respectively. The general geology of the area west of the 

Sierra Nevada crest was described by Miller (1931,1946) and 

Miller and Webb (1940). A detailed geologic map of the 

Owens Peak (CDCA-158) and Little Lake Canyon Wilderness S tudy Areas, east of this study area, was made by Diggles 

and others (1987) and the mineral resources, geochemistry, 

and mineral resource potential of those areas were described

Mineral Resources of the Sacatar Meadows Wilderness Study Area D3
118°05'

36POO'

3^55'

Ball 

Mountain

Qoa>

_________118°00'

Coaiy

APPROXIMATE BOUNDARY OF 

SACATAR MEADOWS 

WILDERNESS STUDY AREA 

(CA-010-027)

Ka

W, Mo

Figure 2. Mineral resource potential and generalized geology of the Sacatar Meadows Wilderness 

Study Area, Tulare and Inyo Counties, California. Geology from Diggles and others (1987).

D4 Mineral Resources of Wilderness Study Areas South-Central California
by Diggles and others (1985). The geology of the Owens Peak 

Wilderness Study Area (CA-010-026), south of this study 

area, was mapped by Diggles and Clemens (1986) and the 

mineral resources, geochemistry, and mineral resource potential of that area were described by Diggles and others (1986). 

Causey and Gaps (1985) conducted a mineral resource appraisal of the Owens Peak (CDCA-158), Owens Peak (CA010-026), and Little Lake Canyon Wilderness Study Areas. 

The geochemistry and mineral resource potential of the South 

Sierra Wilderness and the South Sierra Roadless Area was 

described by Diggles (1987). The geochemistry and mineral 

resource potential of the Rockhouse Basin Wilderness Study 

Area, 5 mi west of the study area, was described by Taylor and 

others (1984) and summarized by Taylor (1984).

Other resource-related studies of the area include a discussion of mines and prospects of Tulare County by Goodwin

EXPLANATION

Area with low mineral resource potential See 

appendix for definition of mineral resource 

potential (L) and certainty (B,C)

Commodities

Molybdenum 

Tungsten

Description of Map Units

Alluvium (Quaternary)

Older alluvium (Quaternary)

Granite of Ball Mountain (Cretaceous)

Alaskite, aplite, and pegmatite (Cretaceous)

Granite of Lamont Peak (Cretaceous)

Sacatar Quartz Diorite of Miller and Webb

(1940) (Jurassic) Locally includes

diorite (di) 

Summit Gabbro of Miller and Webb (1940)

(Jurassic and (or) Triassic) 

Kernville Series of Webb (1931) (Jurassic or

older) Locally includes marble (mb) and

barite (ba) 

Mafic dikes

Contact Hachured where gradational 

Fault Dashed where inferred; dotted where 

concealed; bar and ball on downthrown side 

Mine 

Dirt road

Figure 2. Continued.

Mo 

W

Qal

Qoa

Kbm

Ka

Kip

Js

JTis

MzPzk

md

-|IKltt

(1958). High Life Helicopters, Inc./QEB, Inc. (1980a, b), 

conducted an airborne gamma-ray and magnetometer survey 

of the region under contract to the U.S. Department of Interior. 

Hydrogeochemical and stream-sediment surveys were compiled for the Bakersfield and Fresno quadrangles by the Oak 

Ridge Gaseous Diffusion Plant (198 la, b). In 1983, the study 

area was studied as part of the U.S. Bureau of Land Management Geology, Energy, and Minerals (G.E.M.) inventory 

program (Great Basin GEM Joint Venture, 1983). Other 

mineral resources appraisal studies in the region include the 

Domeland Additions and Woodpecker Roadless Areas (Spear 

and McCulloch, 1981) and Domeland Wilderness 

(Leszcykowski and others, 1982) to the west, and the Golden 

Trout Wilderness (Zilka, 1982) to the north.

Acknowledgm ents

The authors greatly appreciate the cooperation of the local 

property owners and of Gary Walker and Robert Waiwood of 

the U.S. Bureau of Land Management's Bakersfield office. 

Logistical support was provided by Claire and John McDowell. D.A. Dellinger, L.D. Batatian, E.C. Roscoe, S.E. Jensen, 

Jr., J.D. Landells, Jackson Ruby, and Wiley Cranney assisted 

with the geologic mapping. M.C. Horn assisted the U.S. 

Bureau of Mines author with field examination.

APPRAISAL OF IDENTIFIED RESOURCES

By Lucia Kuizon 

U.S. Bureau of Mines

Mining and Mineral Exploration History

There were no mining claims or mineral leases located 

within the Sacatar Meadows Wilderness Study Area in 1984. 

No workings, such as prospect pits or trenches, were found 

within the study area.

Sand and gravel were mined in 1981 from a pit 0.5 mi 

north of the study area in Long Canyon (Silva and others, 

1983). Stream terrace deposits there are suitable for portland 

cement concrete aggregate; they do not extend into the study 

area in quantities sufficient to constitute a resource.

The White King mine, 1 mi west of the study area (fig. 2), 

is on a patented feldspar mining claim. Trenches at the mine 

expose pegmatite dikes of feldspar and quartz. Tucker and 

Sampson (1938) reported that several carloads of feldspar 

were shipped to Los Angeles in 1933. Current owners use the 

material for construction purposes on their ranch. The study 

area lies along the trend of the dikes, but no similar feldspar 

deposits were found within its boundaries.

Barite and tungsten occurrences were prospected 5 to 8 mi 

west of the study area in shear zones and skarn along the 

contact between plutonic rocks and metasedimentary carbonMineral Resources of the Sacatar Meadows Wilderness Study Area D5
ate rocks of the Kemville Series (Tucker and Sampson, 1938; 

Miller and Webb, 1940; Goodwin, 1958; Taylor and others, 1984). No carbonate rocks were found within the study 

area.

Identified Resources

No mineral resources were identified within the Sacatar 

Meadows Wilderness Study Area.

During a stream-sediment survey for the U.S. Department 

of Energy, 12 samples were collected near the study area (Oak 

Ridge Gaseous Diffusion Plant, 198 la, b). Reconnaissance 

by U.S. Bureau of Mines personnel using a hand-held 

scintillometer revealed one sample-collection site southeast 

of Big Pine Meadow within the study area having almost three 

times the background radioactivity. A placer sample 

collected there contains 7.8 parts per million (ppm) uranium 

and 30 ppm thorium (Kuizon, 1985, fig. 2, No. 5). Aboveaverage values for uranium and thorium in the area can be 

interpreted to indicate radioactive minerals commonly 

associated with pegmatite dikes and disseminated in the 

quartz diorite (Troxel, 1957). Granitic rocks of the Sierra 

Nevada batholith may also contain average to above average 

values of thorium (Olson and Overstreet, 1964).

Samples of a quartz vein in the granodiorite phase of the 

Sacatar Quartz Diorite, an aplite dike in schlieric quartz 

diorite, and quartzite from the Kernville Series were collected 

because they were suspected to be mineralized. They contain 

no anomalous mineral concentrations (Kuizon, 1985, fig 2, 

Nos. 2,4, and 1, respectively). Two faults noted by Diggles 

and others (1987) in Sacatar Canyon were examined, but 

showed no evidence of mineral concentrations.

Sand and gravel in sufficient quantities to be classified as 

resources were not found in the study area. Rock types found 

in the study area could meet local demand for dimension 

stone, road metal, riprap, crushed stone, and rubble stone for 

landscaping. However, similar material of equal or better 

quality is abundant closer to local markets.

ASSESSMENT OF MINERAL RESOURCE POTENTIAL

By Michael F. Diggles, James G. Frisken, and 

Andrew Griscom 

U.S. Geological Survey

Geology

The Sacatar Meadows Wilderness Study Area consists 

dominantly of granitic rocks of the Sierra Nevada batholith 

that represent at least three major periods of intrusive activity 

(Evernden and Kistler, 1970). The granitic rocks intrude 

Jurassic or older quartz-biotite-muscovite schist and quartzite. The oldest intrusive rocks in the area are Triassic and (or) 

Jurassic in age, rich in mafic minerals, dioritic to gabbroic in 

composition, and schistose to gneissic in structure. Most of 

the study area is underlain by a younger suite of granitic rocks 

of Jurassic age that is commonly more mafic in composition 

and more foliated in texture than the Cretaceous rocks. The 

youngest rocks in the study area are leucocratic, nonfoliated 

Cretaceous rocks of granite composition.

Collectively, mineral survey reports on the six nearby 

study areas (listed in Previous Studies section, above) describe several types of mineral deposits that could be present 

in the Sacatar Meadows Wilderness Study Area. Mineral occurrences near the study area, many with small-scale production, are virtually all associated with late-stage pegmatites or 

with contact zones between granitic rocks and intruded metamorphic rocks of the Kernville Series, which are now preserved mainly as roof pendants and xenoliths. These host 

rocks, though not dominant in aerial extent, are present in all 

six study areas. The associated mineral-deposit types consist 

of: (1) bedded barite lenses in the Kernville Series and 

possibly remobilized barite in veins, (2) lead, copper, zinc, 

and local gold and silver disseminated sulfide deposits in the 

Kernville Series and in dike rocks, (3) tungsten-molybdenum 

(scheelite) skarn deposits where plutonic rocks are in contact 

with older calcareous sedimentary rocks, or less commonly, 

scheelite in quartz veins, (4) uranium-thorium occurrences in 

disseminated uranium- and (or) thorium-bearing zircon, thorite, and allanite and also possibly monazite, uraninite, and 

secondary uranium minerals in quartz diorite and in shear 

zones in the intrusive rocks, and (5) feldspar and quartz from 

large pegmatite dikes.

Jurassic or Older Metamorphic Rocks

Metamorphic rocks in the area consist chiefly of quartzmica schist with lesser abundance of phyllite and quartzite. 

Skarn was mapped where plutonic rocks intruded calcareous 

metasedimentary rocks outside the study area, but geologic 

mapping does not indicate that such rocks or contact zones are 

present within the study area. Phyllite and quartzite, however, 

were observed in outcrop as pods too small to map at 1:24,000 

scale and as float within the study area (M.F. Diggles and E.G. 

Roscoe, unpub. data, 1987). Calcareous metasedimentary 

rocks are common in outcrops of phyllite and quartzite outside 

the study area. Geochemical evidence suggests that small 

pods of skarn may be present locally within the study area. 

The metamorphic rocks define a roof pendant, mapped as part 

of the Jurassic or older Kernville Series of Miller (1931), that 

crops out in the area of Big Pine Meadow (fig. 2). The 

metamorphic rocks in the region of the study area may be at 

the older end of the age range (Diggles and others, 1985) while 

those west of the region of the study area are at the young end 

of this age range or younger (Saleeby and Busby-Spera, 

1986).

D6 Mineral Resources of Wilderness Study Areas South-Central California
Granitic Rocks

The oldest of three suites of plutonic rocks in the study 

area consists of two rock units of Triassic and (or) Jurassic age 

that commonly are schistose to gneissic. The Summit Gabbro 

of Miller and Webb (1940) is dark gray to black, coarse 

grained, and characterized by euhedral phenocrysts of hornblende; exposures rarely exceed 0.7 mi2 in area. The Sacatar 

Quartz Diorite of Miller and Webb (1940) is a medium-darkgray, medium-grained, foliated rock exposed over most of the 

study area. Its composition is granodioritic, particularly east 

of the Sierra Nevada crest near the base of the range front; 

elsewhere it is quartz dioritic. Locally, the Sacatar Quartz 

Diorite is porphyritic. In places it is rich in mafic inclusions 

in varying degrees of assimilation possibly formed by mingling of small amounts of high-alumina basalt magma with 

quartz diorite magma early in its crystallization (Frost and 

Mahood, 1987).

The younger of the three suites of plutonic rocks consists 

of Cretaceous granite, alaskite, aplite, and pegmatite. In 

general, these rocks are more leucocratic than the older ones 

and are nonfoliated. Numerous small pods of medium- to 

coarse-grained alaskite and associated alkali-feldspar granite, 

aplite, and pegmatite bodies crop out along the crest of the 

Sierra Nevada in and near the study area and extend east into 

the adjacent Little Lake Canyon Wilderness Study Area.

Quaternary Surficial Deposits

Quaternary surficial deposits include Holocene poorly 

sorted gravel, sand, and silt in stream-channel and flood-plain 

deposits. Older Quaternary stream-channel deposits form 

terraces that are dissected by streams.

Structure

The metamorphic rocks in and near Big Pine Meadow 

have a strong foliation that trends generally northwest. These 

rocks underwent at least two periods of uplift associated with 

major intrusive events (Nokleberg and Kistler, 1980).

En echelon faults trend west-northwest across the range 

and control the formation of the major canyons east of the 

study area. These faults are best exposed as shear zones in 

Sacatar and Little Lake Canyons. They are cut at the eastern 

margin of the range by faults along the Sierra Nevada range 

frontal fault zone along which the range was uplifted. A fault 

trending north-south through Scodie Meadow is probably part 

of the range-front fault system.

cobbles), 21 samples of minus-80-mesh stream sediment, and 

20 samples of heavy-mineral concentrate from 22 sites in the 

Sacatar Meadows Wilderness Study Area. With the exception 

of one rock sample collected from outcrop, these samples 

represent eroded bedrock material from drainage basins that 

collectively constitute most of the surface of the study area. 

The minus-80-mesh stream-sediment reflects bedrock geochemistry and usually indicates the presence of mineralized 

areas in the drainage basin. The nonmagnetic fraction of 

panned concentrates is used because this medium concentrates many minerals associated with mineralized and altered 

rocks. Only samples of rocks thought to be mineralized or 

altered were collected for analysis from this study area.

In reconnaissance geochemical resource assessment programs, the semiquantitative spectrographic method is used for 

the initial studies. This method allows for both the rapid and 

economical analysis of large numbers of samples, but with 

many commodity elements detected at only fairly high lower 

limits of determination. To overcome the effects of this 

limitation, other elements associated with mineral occurrences, pathfinders, are studied. When anomalous concentrations of pathfinder elements are determined, selected samples 

are resubmitted for analysis by more sensitive techniques.

All samples were analysed for 31 elements, including 

antimony, barium, cadmium, cobalt, chromium, copper, gold, 

iron, lead, magnesium, manganese, molybdenum, nickel, 

silver, thorium, tin, titanium, tungsten, vanadium, and zinc, 

using a six-step semiquantitative emission spectrographic 

method described by Grimes and Marranzino (1968). In 

addition, the nonmagnetic panned concentrates were 

analyzed for tungsten by spectrophotometry (Welsch, 1983); 

the minus-80-mesh stream sediments and the three rock 

samples were analyzed for uranium and thorium by a neutronactivation method described by Millard and Keaten (1981). 

The rocks were analysed by ICP spectroscopy for five 

elements with limits of determinations as follows: arsenic, 5 

ppm; antimony, 2 ppm; zinc, 2 ppm; bismuth, 2 ppm, and 

cadmium, 0.1 ppm. Methods used were those described by 

Crock and others (1983) and a modification of those described 

by O'Leary and Viets (1986). Two of the rock samples were 

analyzed by atomic absorption for gold at a determination 

limit of 0.1 ppm and mercury at a determination limit of 0.02 

ppm by a modification of the methods described by 

Thompson and others (1968) and by methods described by 

Koirtyohann and Khalil (1976) respectively. Adrian and 

others (1987) presented tables of analytical data, descriptions 

of sample-collection, preparation, and analytical methods, 

and a map showing locations of sample-collection sites.

Geochemistry

Methods

In the spring of 1985, the U.S. Geological Survey collected three samples of rock (two of which are stream

Results and Interpretations

Because of the small data set and the nonlognormal distribution of some of the data, the geochemical threshold values 

for rocks and minus-80-mesh stream sediments were calculated at two to three times the average concentrations for

Mineral Resources of the Sacatar Meadows Wilderness Study Area D7
Sierra Nevada plutonic rocks (Dodge, 1972) or for granodiorites worldwide (Levinson, 1980; Rose and others, 1979). 

Threshold values (in parentheses) for the nonmagnetic concentrates are based on numerous studies of concentrates. For 

nonmagnetic panned concentrates, nine samples contained 

anomalous concentrations of tungsten (10 ppm or greater), six 

contained anomalous concentrations of molybdenum (detected at slightly below the determination limit of 10 ppm), 

and six contained anomalous concentrations of thorium (500 

ppm). For rocks and minus-80-mesh stream sediment, one 

sample contained an anomalous concentration of molybdenum (detected at slightly below the determination limit of 10 

ppm), seven contained anomalous concentrations of thorium 

(30 ppm), 11 contained anomalous concentrations of uranium 

(8 ppm), one contained an anomalous concentration of barium 

(2,000 ppm), and three contained anomalous concentrations 

of copper (70 ppm).

Geochemical interpretations presented in this paper are 

based in part on the above anomalous-threshold values and on 

geochemical data from the Little Lake Canyon Wilderness 

Study Area (Detra and others, 1985). Anomalous concentrations of indicator elements in samples from the Sacatar 

Meadows Wilderness Study Area are generally low in contrast to nearby study areas. Anomalies are also isolated rather 

than found in clusters or being widespread throughout the 

study area.

Most if not all of the mineral-deposit types (listed in 

Geology section, above) may be locally present in the Sacatar 

Meadows Wilderness Study Area. Under current market conditions, it is unlikely that deposits, if they exist in the study 

area, would be economic due to their likely small size. 

Pegmatites cannot be detected geochemically, but a few 

pieces of coarse-grained potassium feldspar, probably derived from pegmatites, were seen in a few of the drainages 

along Long Canyon and at a site west of Bales vertical-angle 

bench mark (VABM) (fig. 2), in the southeast corner of the 

study area. Although no marble or calcsilicate rocks were 

observed at the sample-collection sites, tungsten values in 

concentrates ranging from 5 to 650 ppm were obtained from 

10 of the 20 samples. These anomalies are probably due to the 

presence of small, unmapped skarn occurrences upstream 

from the sample-collection sites. Silicic metasedimentary 

rocks, like those known to be associated with skarn outside the 

study area were observed in drainages above two of the 

sample-collection sites. Except for a few molybdenum values 

of 10 ppm or slightly less, these are single-element anomalies. 

The skarn mineral occurrences in the nearby Owens Peak 

Wilderness Study Areas contain anomalous concentrations of 

tungsten, molybdenum, bismuth, copper, and lead.

The strongest evidence of mineralization in the study area 

comes from three panned-concentrate samples that have high 

tungsten concentrations and contain a few scheelite grains 

(found under shortwave ultraviolet radiation) and limonite 

pseudomorphs after pyrite. These sample-collection sites are

located in: (1) a small drainage that flows into Long Canyon, 

(2) a very small drainage flowing south to Sacatar Canyon, 

and (3) a small south-flowing drainage located 0.5 mi southeast of Big Pine Meadow. These sites have tungsten values of 

650, 45, and 250 ppm, respectively. These concentrations 

cannot be used alone to evaluate the importance of the individual sites because several variables can have an effect on the 

number of scheelite grains in the analyzed fraction. These 

variables consist of: (1) the choice of sample-collection site 

within the drainage basin, (2) theefficiency of the panning and 

sample preparation procedures, (3) the proximity of skarn 

outcrops, (4) the aerial extent of the exposed skarn, (5) the 

amount of scheelite present in the skarn, and (6) the homogeneity of the samples when split for analysis. Eight additional 

samples contain 5 to 15 ppm tungsten. Two are associated 

with detectable molybdenum (10 ppm) and one with limonite 

pseudomorphs after pyrite. The latter three samples are from: 

(1) a small drainage sampled from Scodie Meadow, (2) a very 

small drainage northwest of Big Pine Meadow, and (3) the 

small drainage west of Bales VABM. The latter site has 15 

ppm tungsten and 10 ppm molybdenum as well as epidote and 

chlorite grains in the concentrate and 3,000 ppm barium and 

70 ppm copper in a granitoid cobble. About 3 mi east of this 

site, samples collected from upper Deadfoot and upper 

Fivemile Canyons in the Little Lake Canyon Wilderness 

Study Area contain moderately anomalous concentrations of 

tungsten, molybdenum, lead, and copper, probably due to 

skarn mineralization, which may extend into the Sacatar 

Meadows Wilderness Study Area. Several of the stream 

sediments and nonmagnetic concentrates collected along the 

east side of the divide separating the two study areas contain 

higher concentrations of copper (100 ppm in sediments) and 

molybdenum (100 ppm in concentrates) than samples collected along the west side of the divide (this study area), in 

which two contained 70 ppm copper and and two contained 10 

ppm molybdenum.

All of the above described tungsten-molybdenum anomalies could be accounted for if scattered small pods of mineralized skarn containing minerals of the scheelite-powellite 

series were present in the study area. No such pods were 

observed, but their existence is indicated by observations of 

silicic metasedimentary rocks in the study area similar to 

those seen in outcrop with skarn outside the study area, and by 

the geochemical results.

During a stream-sediment survey conducted by the U.S. 

Department of Energy (Oak Ridge Gaseous Diffusion Plant, 

198 la, b), 12 samples were collected near the study area. Nine 

of those samples contain 1.76 to 5.88 ppm uranium, which 

falls within two standard deviations of the mean of 3.46 ppm 

for the Bakersfield quadrangle (Oak Ridge Gaseous Diffusion 

Plant, 1981a). One sample containing 10.59 ppm uranium 

was collected about 2 mi west of the study area and about 1 mi 

northeast of Chimney Peak. Thorium values for the 12 

samples range from 10 to 42 ppm; seven are above the average

D8 Mineral Resources of Wilderness Study Areas South-Central California
value of 10 ppm for intermediate igneous rocks (Oak Ridge 

Gaseous Diffusion Plant, 1981a;Levinson, 1980). During the 

U.S. Geological Survey study, 21 stream-sediment and three 

rock samples were analyzed for uranium and thorium, and 

scintillometer readings were taken at ground level in the 

stream channels at most of the sample-collection sites. Thorium concentrations in samples collected from 20 streamsediment sample-collection sites, including a granite stream 

cobble collected southwest the Bales VABM site, ranged 

from 14.6 to 80.9 ppm. At 15 of the 21 sites, uranium 

concentrations ranged from 6.29 to 15.8 ppm. These uranium 

and thorium concentrations are higher than those reported by 

the Department of Energy (Oakridge Gaseous Diffusion 

Plant, 198la) and U.S. Bureau of Mines (Kuizon, 1985), 

perhaps due to selection of sample-collection sites since the 

sites for this study were selected where heavy minerals were 

naturally concentrated. All of the samples were collected 

from areas of granitic rock, have above-average thorium 

concentrations (most have above-average uranium concentrations for intermediate granitic rocks), and contain euhedral 

crystals of metamict zircon and thorite in the heavy-mineral 

concentrates, These facts suggest that the radioactive minerals are probably derived from widespread disseminations in 

the plutonic rocks. If this is the case, the uranium-thorium 

minerals will not be present in large amounts unless concentrated in placers. Five nonmagnetic concentrate samples have 

thorium concentrations of 500 to 700 ppm and one has a value 

of 1,500 ppm. These values are not unusually high for 

concentrates from felsic intrusive rocks, on the basis of 

comparison with values found in samples from several other 

study areas in similar geologic settings, and do not suggest 

concentrations sufficient to constitute placer deposits. Olson 

and Overstreet (1964) concluded that the granitic rocks of the 

Sierra Nevada batholith may contain above-average concentrations of thorium; Troxel (1957) discussed the disseminated 

uranium-thorium minerals in pegmatite dikes and in quartz 

diorite.

The scintillometer, set at its lowest range setting, produced readings ranging from two to 23 counts per second. The 

variation could be due to varying potassium content of the 

sediment and nearby bedrock, topographic variations, or 

variation in the degree of natural concentration of heavy 

minerals at the sites. The highest uranium and thorium 

concentrations from samples as well as the highest scintillometer readings were obtained in the central two thirds of the 

study area. Outcrops within a 2-mi radius of a point 2 mi south 

of the head of Sacatar Canyon appear to have contributed the 

highest concentrations of radioactive minerals. Three rock 

samples collected outside the 2-mi radius ranged from 0.43 

ppm uranium in quartz veins to 2.95 ppm in granite.

In this study, low-detection-level gold analyses were not 

run on the concentrates; however, neither megascopic nor 

microscopic gold was observed. The three rocks that were 

analyzed contain no detected gold or mercury.

Geophysics

Aeromagnetic Data

An aeromagnetic survey of the Sacatar Meadows South 

Wilderness Study Area was flown in 1981 by a private 

contractor (U.S. Geological Survey, 1982). The aeromagnetic data were collected along parallel east-west flightlines 

spaced 0.5 mi apart and at an elevation of 9,000 ft. The 

contractor then gridded the data set using a grid spacing of 650 

ft and machine contoured the gridded data at a scale of 

1:62,500.

Variations in the Earth's magnetic field are generally 

caused by variations in the amounts of magnetic minerals in 

different rock units. Magnetite is the common magnetic 

mineral in this area. Magnetic minerals, where locally concentrated or absent, may cause a high or low magnetic anomaly that can be a guide to mineral occurrences or deposits. 

Boundaries between magnetic and relatively less magnetic 

rock units are located approximately at the steepest gradient 

on the flanks of the magnetic anomaly because at these 

magnetic latitudes the inch'nation of the Earth's magnetic field 

is relatively steep (61° below the horizontal).

Comparison of the contoured aeromagnetic map with the 

geologic and topographic maps indicates that most of the 

magnetic anomalies are caused by topographic relief in 

magnetic terrane composed of Mesozoic plutonic rocks, in 

particular the mesocratic to melanocratic ones. Relatively 

magnetic intrusive rocks include the Sacatar Quartz Diorite 

and the Summit Gabbro, whereas the other plutonic rocks and 

the older metamorphic rocks tend to be weakly magnetic or 

nonmagnetic. One area of Sacatar Quartz Diorite within the 

study area is an exception and appears to be only weakly 

magnetic because here the local hills do not produce magnetic 

highs in the manner of the more typical Sacatar Quartz Diorite 

elsewhere. This uniquely nonmagnetic area is located in the 

westernmost part of the study area north of Big Pine Meadow 

and west of the fault striking N. 5° W. along the east side of the 

Big Pine Meadow. Perhaps some weak alteration has partly 

destroyed the magnetite within this nonmagnetic area. The 

faults in the study area tend to be associated with magnetic 

lows in those places where magnetic rocks are juxtaposed, but 

this association is most probably an effect of the low topographic expression of the faults.

In general, the aeromagnetic data do not appear to provide 

any evidence for mineral resource potential in this area.

Gamma-ray Survey

Airborne gamma-ray spectrometer surveys were flown 

within this study area (High Life Helicopters, Inc., and Geodata International, Inc., 1979; High Life Helicopters, Inc./ 

QEBJnc., 1980aand 1980b). These helicopter surveys were

Mineral Resources of the Sacatar Meadows Wilderness Study Area D9
flown on east-west flightlines spaced 3.1 mi apart at an 

altitude of 400 ft above the ground. These data measure the 

effective uranium, thorium, and potassium content of the 

uppermost inch or so of soil or rock at the surface. Within the 

study area no uranium anomalies were observed.

Remote Sensing

Hydrothermal alteration is often accompanied by the formation of the minerals pyrite and (or) hematite, which, along 

with other iron-rich minerals, are oxidized during weathering 

in the near-surface environment to produce ferric oxide 

(hematite), hydrated ferric oxide (goethite, lepidocrocite), 

ferric sulfate (jarosite), or ferric carbonate (siderite) minerals 

(Blanchard, 1968). These secondary iron-bearing minerals, 

along with amorphous or poorly crystalline ferric oxide material like ferrihydrite, are collectively referred to as the limonite 

minerals and are recognized in the field by their red, yellow, 

or brown colors.

The limonite mineral group has unique spectral reflectance characteristics that can be detected on Landsat multispectral scanner (MSS) images using a color-ratio compositing technique described by Rowan and others (1974). This 

compositing was used to look for areas of limonite in the study 

area (D.H. Knepper, Jr., and F.A. Kruse, written commun., 

1986). Areas of hydrothermal alteration lacking the limonite 

minerals cannot be found using this technique, and areas of 

limonite not related to hydrothermal alteration cannot be 

distinguished from those that are. The presence of limonite 

minerals cannot be reliably mapped in areas with approximately 50 percent or greater vegetation density and in areas of 

deep to moderate shadows.

The spectral response of Landsat MSS data of the study 

area is dominated by vegetation. Consequently, the presence 

of anomalous concentrations of limonite possibly associated 

with hydrothermal alteration could not be evaluated (D.H. 

Knepper, Jr., and F.A. Kruse, written commun., 1986).

Mineral Resource Potential

In and near the Sacatar Meadows Wilderness Study Area, 

five areas that have mineral resource potential were delineated. The study area is situated in the Sierra Nevada physiographic province, which contains the largest concentration 

of tungsten deposits in the United States (Newberry, 1982). 

The mineral-deposit model that is most appropriate to apply in 

this study area is the tungsten-skarn felsic-plutonic-rock 

model (Einaudi and others, 1981; Cox, 1983; Cox and Singer, 

1986). Tungsten skam deposits form along contacts and in 

roof pendants of batholiths and in thermal aureoles of apical 

zones of stocks that intrude carbonate rocks. Of 28 tungstenskarn deposits, Cox (1986) notes a mean of 1.2 million tons 

with a one-standard-deviation range of from 0.06 to 24 million

tons. He notes a mean grade of 0.67 percent tungsten trioxide 

with a one-standard-deviation range of from 0.34 to 1.4 

percent tungsten trioxide.

The ridge northwest of Big Pine Meadow, located outside 

and adjacent to the study area to the east, has low mineral 

resource potential for tungsten and molybdenum with a certainty level of B. Geochemical analyses suggest that tungsten, 

molybdenum, uranium, and thorium are present in low-level 

concentrations on the ridge in areas underlain by metasedimentary rocks of the Kernville Series. Although geologic 

mapping does not indicate large bodies of calc-silicate 

hornfels along this ridge, skarn is present elsewhere in the 

Kernville Series and probably is present as small pods along 

the ridge.

The area from the valley to the ridge crest southeast of 

Scodie Meadow has low mineral resource potential for tungsten and molybdenum with a certainty level of C. This hillside 

is underlain by granodiorite and quartz diorite of the Sacatar 

Quartz Diorite. Silicic metasedimentary rocks were observed 

as small pods in outcrop in this drainage. Geochemical 

analyses indicate that tungsten, molybdenum, barium, and 

minor amounts of copper are present in low-level concentrations in the numerous small xenoliths of calcareous metasedimentary rock mapped in this unit (Diggles and others, 1986). 

Secondary alteration and skam minerals are present in 

samples from the area. There is an area of low mineral 

resource potential for tungsten in Deadfoot Canyon, in the 

adjacent Little Lake Canyon Wilderness Study Area east of 

this hillside (Diggles and others, 1985).

The valley east of Long Canyon and the small drainage 

northeast of Sacatar Meadow both have low mineral resource 

potential for tungsten with a certainty of C. Float of silicic 

metasedimentary rock was observed in the former valley. 

Geochemical analyses indicate that tungsten, thorium, and 

uranium are present in low-level concentrations in both of 

these areas, which are underlain by the Sacatar Quartz Diorite. 

One of the samples from each of these areas contains visible 

pyrite.

The area southeast of Big Pine Meadow has low mineral 

resource potential for tungsten with a certainty of C. Geochemical analyses indicate that tungsten, thorium, uranium, 

and minor molybdenum are present in low-level concentrations in this area, which is underlain by the Sacatar Quartz 

Diorite and adjoins an area underlain by a belt of alaskite. 

There is visible pyrite in one of the samples. A U.S. Bureau 

of Mines scintillometer reading in this area was three times the 

background level. A placer sample collected here, however, 

contains only low-level concentrations of uranium and thorium.

The Sacatar Meadows Wilderness Study Area has no geothermal energy potential (Higgins, 1981) and the geology is 

not conducive to petroleum or natural gas resource potential 

(Scott and Miller, 1982; Scott, 1983). The radioactive minerals are probably derived from widespread disseminations in 

the plutonic rocks. In the absence of placers of these minerals,

D10 Mineral Resources of Wilderness Study Areas South-Central California
there are no concentrations of energy minerals and therefore 

no energy mineral resource potential in the study area.

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Mineral Resources of the Sacatar Meadows Wilderness Study Area D13

APPENDIXES
DEFINITION OF LEVELS OF MINERAL RESOURCE POTENTIAL 

AND CERTAINTY OF ASSESSMENT

Definitions of Mineral Resource Potential

LOW mineral resource potential is assigned to areas where geologic, geochemical, and geophysical 

characteristics define a geologic environment in which the existence of resources is permissive. This 

broad category embraces areas with dispersed but insignificantly mineralized rock as well as areas with 

few or no indications of having been mineralized.

MODERATE mineral resource potential is assigned to areas where geologic, geochemical, and geophysical 

characteristics indicate a geologic environment favorable for resource occurrence, where interpretations 

of data indicate reasonable likelihood of resource accumulation, and (or) where an application of 

mineral-deposit models indicates favorable ground for the specified type(s) of deposits.

HIGH mineral resource potential is assigned to areas where geologic, geochemical, and geophysical 

characteristics indicate a geologic environment favorable for resource occurence, where interpretations of 

data indicate a high degree of likelihood for resource accumulation, where data supports mineral-deposit 

models indicating presence of resources, and where evidence indicates that mineral concentration has 

taken place. Assignment of high resource potential to an area requires some positive knowledge that 

mineral-forming processes have been active in at least part of the area.

UNKNOWN mineral resource potential is assigned to areas where information is inadequate to assign low, 

moderate, or high levels of resource potential.

NO mineral resource potential is a category reserved for a specific type of resource in a well-defined area.

Levels of Certainty

CJ

QC

D 

O 

C/5

U/A

UNKNOWN

POTENTIAL

H/B

HIGH POTENTIAL

M/B

MODERATE POTENTIAL

L/B

LOW

POTENTIAL

H'C

HIGH POTENTIAL

M/C 

MODERATE POTENTIAL

L/C

LOW

POTENTIAL

H/D

HIGH POTENTIAL

M/D

MODERATE POTENTIAL

L/D

LOW POTENTIAL

N/D

NO POTENTIAL

B C 

LEVEL OF CERTAINTY

A. Available information is not adequate for determination of the level of mineral resource potential.

B. Available information suggests the level of mineral resource potential.

C. Available information gives a good indication of the level of mineral resource potential

D. Available information clearly defines the level of mineral resource potential.

Abstracted with minor modifications from:

Taylor, R B., and Steven, T. A., 1983, Definition of mineral resource potential: Economic Geology,

v. 78, no. 6, p. 1268-1270. 

Taylor, R B., Stoneman, R. J , and Marsh, S P., 1984. An assessment of the mineral resource potential

of the San Isabel National Forest, south-central Colorado: U.S Geological Survey Bulletin 1638, p.

40^12. 

Goudar/.i, G H., compiler, 1984. Guide to preparation of mineral survey reports on public lands: U.S.

Geological Survey Open-File Report 84-0787, p. 7. 8.

D16 Mineral Resources of Wilderness Study Areas South-Central California
RESOURCE/RESERVE CLASSIFICATION

ECONOMIC

MARGINALLY 

ECONOMIC

SUBECONOMIC

IDENTIFIED RESOURCES

Demonstrated

Measured

Res<

 

Mar 

Res<

Indicated

srves

ginal 

srves

Demonstrated 

Subeconomic 

Resources

Inferred

Inferred 

Reserves

Inferred 

Marginal 

Reserves

Inferred 

Subeconomic 

Resources

UNDISCOVERED RESOURCES

Probability Range

Hypothetical Speculative

Major elements of mineral resource classification, excluding reserve base and inferred reserve base. Modified from U.S. Bureau of Mines 

and U.S. Geological Survey, 1980, Principles of a resource/reserve classification for minerals: U.S. Geological Survey Circular 831, p. 5.

Mineral Resources of the Sacatar Meadows Wilderness Study Area D17
GEOLOGIC TIME CHART 

Terms and boundary ages used by the U.S. Geological Survey in this report

EON

Phanerozoic

Proterozoic

Archean

ERA

Cenozoic

Mesozoic

Paleozoic

Late Proterozoic

Middle Proterozoic

Early Proterozoic

Late Archean

Middle Archean

Early Archean

PERIOD

Quaternary

Tertiary

Neogene 

Subperiod

Paleogene 

Subperiod

Cretaceous

Jurassic

Triassic

Permian

Carboniferous 

Periods

Pennsylvanian

Mississippian

Devonian

Silurian

Ordovician

Cambrian

pre-Archean2

EPOCH

Holocene

Pleistocene

Pliocene

Miocene

Oligocene

Eocene

Pateocene

Late 

Early

Late 

Middle 

Early

Late 

Middle 

Early

Late 

Early

Late 

Middle 

Early

Late 

Early

Late 

Middle 

Early

Late 

Middle 

Early

Late 

Middle 

Early

Late 

Middle 

Early

-

AGE ESTIMATES 

OF BOUNDARIES 

(in Ma)

- 0.010

- 1.7

- Ro

<"k A

- 24

oo 

- 55*j\j

 ftC

- 96

 17Q

one

f^r\J 

_ *>QH

OO\J 

_ 1Rf\

- 410

L_ A-JC *rO*/

- 500

O/ \J

^- onn aUU

- 1600

_ oenn

OvIUU

- 3400

'Rocks older than 570 Ma also called Precambrian, a time term without specific rank. 

Informal time term without specific rank.

D18 Mineral Resources of Wilderness Study Areas South-Central California
Mineral Resources of 

Wilderness Study Areas: 

South-Central California

This volume was published as chapters A D

U.S. GEOLOGICAL SURVEY BULLETIN 1705
DEPARTMENT OF THE INTERIOR 

DONALD PAUL MODEL, Secretary

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director
CONTENTS

[Letters designate the separately published chapters]

(A) Mineral Resources of the Owens Peak Wilderness Study Area, Tulare and Kern 

Counties, California, by Michael F. Diggles, James G. Frisken, Andrew Griscom, 

Herbert A. Pierce, and J. Douglas Causey.

(B) Mineral Resources of the Southern Inyo Wilderness Study Area, Inyo County, 

California, by James E. Conrad, James E. Kilburn, Richard J. Blakely, Charles 

Sabine, Eric E. Gather, Lucia Kuizon, and Michael C. Horn.

(C) Mineral Resources of the Pinnacles Wilderness Contiguous Wilderness Study Area, 

Monterey and San Benito Counties, California, by Steve Ludington, Karen Gray, and 

Lucia Kuizon.

(D) Mineral Resources of the Sacatar Meadows Wilderness Study Area, Tulare and Inyo 

Counties, California, by Michael F. Diggles, James G. Frisken, Andrew Griscom, 

and Lucia Kuizon.
GPO 585-045/78030