Full text of "Quartzite in California"

3 1175 00670 0960

OUARTZITE IN CALIFORNIA

BULLETIN 187

California Division of Mines and Geology
Ferry Building, San Francisco, l9t>o

QUARTZITE IN CALIFORNIA

By WILLIAM E. VER PLANCK

California Division of Mines and Geology

BULLETIN 187

California Division of Mines and Geology
Ferry Building, San Francisco, 1966

UNIVERSITY OF CALIFORNIA
DAVIS

■ 1975

STATE OF CALIFORNIA

Edmund G. Brown, Governor

THE RESOURCES AGENCY

Hugo Fisher, Adminisfrafor

DEPARTMENT OF CONSERVATION

DeWitt Nelson, Director

DIVISION OF MINES AND GEOLOGY

Ian Campbell, Slate Geologist

BULLETIN 187
Price $2.75

CONTENTS

Page

Introduction _— __ 7

Quartzite industry in California — — - 7

Previous work 7

Scope - -- 7

Acknowledgments _ — - - 8

Geologic Occurrence — - — - - — 8

Petrography 8

Geologic associations -- 8

Commercial sources of high-purity quartzite — — 8

Some quartzite deposits and operations 8

Eureka Quartzite near Lone Pine 8

Previous work 9

Method of work 9

Descriptive geology 9

Stratigraphy 9

Structure 12

The Eureka Quartzite in detail 12

Operations — - 16

Lakeview quarries — — - 1 6

Swansea quarry __.. 1 7

Dolomite 17

Talc 17

Quartzites of the Oro Grande series near Victorville 17

Previous work and acknowledgments 18

Descriptive geology 1 8

Quartzite quarries .— 1 8

Atlas 1 8

Emsco - 19

Riverside Cement Company — 19

Southwestern — 19

Some undeveloped deposits 20

Klondike 20

Quartzite Mountain Northwest 20

Quartzite Mountain Southwest ..- 20

Quartzite Mountain (upper unit) 20

Quartzite Mountain (lower unit) — 20

Coxcomb Ridge 21

Zabriskie Quartzite near Shoshone 21

Previous work 21

Descriptive geology — 22

The Zabriskie Quartzite in detail 22

Dublin Hills -- 22

McLain Peak , - 25

Resting Spring Range - — 26

Quartz rock deposits of Gabilan Range_ 26

Descri ptive geology 26

Fremont Peak deposit 26

Quartzite in the Hodge Volcanic Series _ 27

Descriptive geology 27

Golconda quarry 27

Kennedy quarry 27

Deposit in section 29 — - 27

[3]

CONTENTS— Continued

Page

Some impure quartzites _ 28

Quortzites of the Kernville Series... _ 28

Prospect Mountain Quartzite 29

Soragosso Quartzite 29

Stirling Quartzite -. 30

Vitreous quartzite of Eagle Mountains, Riverside County 30

Quarrying and processing 31

Metfiods 31

Performance data 32

Utilization 32

In general 32

Silica brick 32

Trends in the Steel industry 32

Silica brick industry in California . 33

Method of production - 33

The mineralogy of silica firebrick by J. Morrow Elias 36

Specifications 40

Portland cement 40

The manufacture of porfland cement 40

California plants that use silica 40

Specifications 41

Ferrosilicon and silicon 41

The industry in California 41

Method of production 41

Specifications 42

References 43

Tabulated list of quartzite formations 47

[4]

ABSTRACT

Quartzite, a compact, granular rock composed of interlocking quartz grains, is
common and widespread. Large, uniform deposits of high-purity quartzite containing
95 to 100 percent Si02 are relatively scarce in California and are located far from
consuming centers. Production in California is several tens of thousands of tons a year.

The Ordovician Eureka Quartzite near Lone Pine, Inyo County, furnishes the only quartz-
ite produced in California that is currently known to be suitable for making super duty
silica brick. It occurs in a conformable sequence of predominantly dolomite beds that strike
parallel to the mountain front. Of a total thickness of 400 feet, only the upper 150 feet
consists of high-purity quartzite. Units of the late Paleozoic Oro Grande Series near Vic-
torville, San Bernardino County, have furnished several million tons of high-purity quartz-
ite, mostly for the portland cement industry. Quartzite, limestone, dolomite, and schist
of the Oro Grande Series have been complexly folded and faulted, then overlapped
and intruded by rocks of the Triassic (?) Sidewinder Volcanic Series. Both units are
intruded by granitic rocks. Near Shoshone, Inyo County, large deposits of the Zabriskie
Quartzite Member of the Lower Cambrian Wood Canyon Formation occur in the Dublin
Hills, on McLain Peak, and in the Resting Spring Range. The quartzite is of high purity
but has not been developed. Quartz rock is associated with carbonate rocks of the
Sur Series near Fremont Peak, Monterey County. The nearly complete replacement of
carbonate rock by silica has resulted in substantial bodies of material that resembles
quartzite. The deposits are not of the highest purity and are undeveloped. Deposits in
the Paleozoic (?) Hodge Volcanic Series, 10 to 15 miles southwest of Barstow, San
Bernardino County, furnished quartzite for silica brick during the 1920's. Lenticular
bodies of high-purity quartzite as much as 200 feet thick and 1000 feet long occur in
a sequence of steeply dipping muscovite schist and quartz-biotite schist. Quartzite-
bearing formations that probably are not pure enough to be potential sources of
high-purity quartzite include the Paleozoic (?) Kernville Series, the Lower Cambrian
Prospect Mountain Quartzite, the Paleozoic Saragossa Quartzite, the Lower Cambrian
Stirling Quartzite, and the vitreous quartzite series of the Eagle Mountains, Riverside
County.

Quartzite is brittle and breaks easily but is abrasive and difficult to drill. Standard
quarrying methods are employed.

Silica brick, produced by the careful burning of crushed quartzite mixed with one
to three percent of hydrated lime, are used mostly for the roofs of open hearth steel
furnaces. Because of technical changes in the steel industry, their use is declining. The
purest quartzite obtainable is used. Alumina and alkalies are critically deleterious
impurities. In super duty silica brick, the percent of alumina plus twice the percent of
alkalies must equal 0.5 or less. Most other oxides are less harmful. The quartzite also
must crush to form angular particles that pack tightly and that do not crack or dis-
integrate in the kiln. In the manufacture of portland cement, some form of silica makes
up part of the kiln feed if enough silica is not present in the principal raw materials.
Plants use the cheapest available silica material that meets their particular chemical
requirements. Relatively few plants use quartzite. Ferrosilicon and silicon were not
being produced in California in 1961, but have been produced in the past. They are
made in the electric furnace from tough quartzite or quartz that contains no minus
%-inch material and does not disintegrate in the kiln. A few tenths of a percent of
iron and alumina are tolerated; but only traces of arsenic, phosphorus, and sulfur
are allowed.

;5]

Gladding McBean and Company is now known as "Interpace" (International Pipe and
Ceramics Corporation). The firm name has been changed since Mr. Ver Planck prepared
this report.

QUARTZITE IN CALIFORNIA

Bv WILLIAM E. VER PLANCK *

INTRODUCTION

Quartzite In California

Quartzite is a compact, granular rock composed of
interlocking quartz grains. Quartzite is a common,
widespread rock that is abundant in most metamorphic
terranes. Because of its abundance there can never be
an absolute shortage. Its unit value is low, and speci-
fications for most uses are exacting. This report is
concerned mostly with high-purity quartzite contain-
ing 95 to 100 percent SiOo. Relatively few quartzite
formations in the United States consistently reach such
high purities. Even such material has no economic
value unless it can be cheaply mined and shipped to the
consumer.

No detailed statistics are available, but the produc-
tion of high-purity quartzite in California is on the
order of several tens of thousands of tons per year. Of
this amount probably 75 percent is consumed by the
Portland cement industry. The cement industry also
consumes a much larger tonnage of silica in forms
other than high-purity quartzite. Some of this material,
which includes impure quartzite, contains substan-
tially less than 95 percent Si02. Most, if not all, of
the remainder of the high-purity quartzite produced
in California is consumed in the manufacture of super
duty silica brick for use as a refractory material.
Quartzite for this purpose should contain not more
than 0.25 percent combined alumina and alkalies and
must also meet certain physical requirements, includ-
ing the proper particle size distribution of the crushed
material. Silicon and ferrosilicon also are made from
high-purity quartzite and quartz. Lump material with
only a few tenths of a percent of iron and alumina is
used. Quartzite from California has never been so used,
but, probably some of it would be suitable. Because
of its physical properties, quartzite is admirably suited
for use as aggregate and railroad ballast; but in Cali-
fornia these materials are made from other types of

* The main body of this paper was prepared b>- Air. Vcr Planck
prior to his untimely death in 1963. It has since been added
to by various members of the Division staff, to bring it more
nearly up to date.

rock, deposits of which are more conveniently located
than the quartzite deposits. Relatively minor amounts
of decorative building stone are prepared from certain
impure colored and stained quartzite in California.

In 1961, two operations in California were produc-
ing high-purity quartzite. One, near Lone Pine, Inyo
County was supplying the silica brick industry; the
other, near Victorville, San Bernardino County, pro-
duced quartzite for the portland cement industry. In
addition, quartz rock for the silica brick industry was
brought into the state from the vicinity of Grants
Pass, Oregon.

Previous Work

No comprehensive report on the quartzite resources
of California has been published previously. The
quarrying of deposits of quartzite associated with the
Oro Grande Series and the Hodge \^olcanic Series in
San Bernardino County has been described in the
county reports of the Division of Mines (Tucker and
Sampson 1930; 1943; Wright and others, 1953). Quartz-
ite and quartz are summarized together in a four-page
article in "Mineral Commodities of California", Divi-
sion of Mines Bulletin 176. Most quartzite formations
are discussed in geologic reports in which areal geol-
ogy and stratigraphy are given primary consideration,
but few of these reports contain the details necessary
for the economic evaluation of a particular formation
at a particular place. Perhaps the most thorough survey
was made by Gladding, McBean and Company during
1953. This survey was summarized by Richard F.
Brooks in a paper presented to the Mining Branch,
Southern California Section, A.I.M.E., on October 21,
1955.

Scope and Method of Work

This report describes the geologic occurrence, min-
ing, processing, and utilization of quartzite in Califor-
nia. The work began with a survey of the literature.
All of the geologic reports available to the writer were
e.xamined, and the descriptions of quartzite-bearing
formations were noted and tabulated by formation
and locality. Most of the quartzite-bearing formations

[7]

California Division of Mines and Geology

Bull. 187

that have been tabulated are small and impure and of
no present economic value. The literature sur\'ey in-
dicated that relatively few formations are extensive
and uniform enough to warrant further study. A rela-
tively small number of deposits that were thought to
be of possible economic value \\ere examined briefly
in the field.

Three deposits were examined in detail. A plane
table map, scale 1 inch equals 100 feet, was made of a
deposit of the Eureka Quartzite near Lone Pine, Inyo
County. Oliver E. Bowen, Jr., of the Division of
Mines and Geology staff and the author mapped the
quartzite-bearing Oro Grande Series near \"ictorville,
San Bernadino County, on a scale of 1:12,000. The
report of this work has been published separately, and
a summary of it is included here. Two large-scale
structure sections were made of the Zabriskie Quartz-
ite near Shoshone, Inyo County.

Acknowledgmenis

The writer wishes to thank Arthur G. Moore of
Gladding, iMcBean, and Company, Richard F. Brooks,
formerly of Gladding, McBean and Company, Oliver
E. Bowen Jr., Charles ^^^ Chcstcrman, and James R.
McNitt of the Di\'ision of Mines and Geology, and
Lauren A. Wright, formerly of the Division of .Mines
and Geology, for help and advice.

GEOLOGIC OCCURRENCE

Petrography

Quartzite is defined as a rock "consisting largely
of quartz fragments so thoroughly cemented or re-
crystallized that it breaks through the grains as readily
as around them." (Grout, 1932, pp 366-368). Some
quartzite is a metamorphosed sandstone, the grains of
which have been recrystallized as the result of heat
and pressure into an interlocking aggregate af anhedral
quartz crystals (see photo 3). The term also applies
to a sandstone solidly cemented by silica that has
grown in optical continuity around each fragment.
Grout's definition implies that quartzite must be de-
rived from sand with a high proportion of quartz
grains. The tendency, however, is to include other
forms of silica, such as chert or quartz silt, that have
been recrystallized through metamorphism. Another
type of quartz rock results from the replacement of
carbonate rock or other rock types by silica (see photo
12). If silicification has been complete, the quartz rock
is difficult to distinguish in hand specimen or even thin
section from a true quartzite derived from sandstone
and also has the same commercial uses.

In practice, the term quartzite is used loosely, and
some inetamorphic rocks that contain as little as 60
percent quartz have been called quartzite (Heinrich,
1956). Impurities include non-quartz grains, particu-
larly feldspar, that were present in the sand from

which the quartzite was derived, micas and other
minerals produced from clay during metamorphism,
and introduced minerals such as pyrite. With increas-
ing feldspar content, quartzite grades into feldspathic
quartzite and then into gneiss. Similarly, with an in-
creasing mica content, quartzite grades into micaceous
quartzite (photo 15) and schist. Quartz -rich rocks
also exhibit a \\-ide and unbroken range of induration.
There is a complete gradation from thoroughly re-
crystallized or cemented quartzite to sandstone, friable
sandstone, and unconsolidated sand.

Geologic Associations

Quartzite is found in metamorphic terranes in as-
sociation with schist, gneiss, marble, and other meta-
morphic rocks. Quartzite bodies range in size from
discontinuous layers less than an inch thick to forma-
tions several hundred feet thick that occur within
areas of hundreds of square miles. Some quartzite
bodies exhibit heterogeneous mineralogy; others are
remarkably uniform. The impurities in a few wide-
spread and uniform quartzite formations are in the
order of a few tenths of a percent.

Commercial Sources of High-purity Quartzite

Sources of high-purity quartzite in California are
few and poorly located with respect to transportation
facilities and markets. Although quartzite occurs in
most of the mountainous regions of the state, most of
it is feldspathic, micaceous, and in the form of thin
layers associated with schist. Formations consisting
largely or entirely of quartzite are most numerous in
the southeastern deserts and are of Paleozoic or Pre-
cambrian age. \'cry few of them are sufficiently pure
and uniform to be potential sources of high-purity
quartzite.

The Eureka Quartzite is quarried near Lone Pine,
Inyo County, for silica brick. Quartzite of the Oro
Grande Series from near \"ictorville, San Bernardino
County is used for portland cement and formerly for
silica brick. At one time, quartzite for silica brick was
obtained from small deposits associated ^\■ith the
Hodge \'olcanic Scries near Hodge, San Bernardino
Count)-. Deposits of quartz rock near Fremont Peak,
.Monterey County, and the Zabriskie Quartzite and
perhaps parts of the Stirling Quartzite in the Death
\'alley area ma\" be suitable for some commercial
purposes.

SOME QUARZITE

DEPOSITS AND OPERATIONS

Eureka Quartzite Near Lone Pine

Outcrops of the Eureka Quartzite near Lone Pine,
Inyo County, furnish the only quartzite produced in
California that is known to be suitable for making
super duty silica brick.

1966

QUARTZITE

The Eureka Quartzite, of middle Ordovician age, is
a remarkably uniform formation that is widespread in
central and western Nevada. The type locality is near
Eureka, Nev-ada. In California, it occurs in the Death
Valley area and as far west as Owens Valley.

The quartzite deposits under consideration crop out
on the steep southwest face of the Inyo Mountains,
roughly 6 to 11 air miles southeast of Lone Pine
and 100 to 800 feet above the floor of Owens Lake.
The outcrops extend discontinuously from the vicin-
ity of Swansea, where quartzite was obtained in 1955,
to at least a mile northwest of Alico Siding on the
now abandoned narrow gage Owens Valley line of the
Southern Pacific Company. Since 1955, quartzite has
been obtained intermittently from the Lakeview
quarries near Alico Siding.

The Lakeview quarries are connected with State
Highway 190 by a privately maintained gravel road
about a mile long that is suitable for heavy trucks.
The railroad loading point is on the standard gage line
of the Southern Pacific Company at its crossing of
State Highway 190, roughl\- 2'/^ air miles southeast of
Lone Pine and 6 miles by road from the Lakeview
quarries.

Previous Work

The only published geologic maps covering the
Lone Pine quartzite deposits know n to the writer are
the Death V'alley sheet of the State map (Jennings,
1958), and the compiled map of the Owens V^alley
region (Bateman and iMerriam, 1954). The geologic
map of the New York Butte quadrangle (Merriam and
Smith, 1951, unpublished) was not available to the
writer. The Eureka Quartzite has been described in
the nearby Ubehebe Peak quadrangle (McAllister,
1955), in the Talc City Hills (Hall and Mackevett,
1958; Gay and Wright, 1954), and in Mazourka Can-
yon (Langenheim and others, 1956).

As shown on the Death Valley sheet (Jennings,
1958), the southwest face of the Inyo Alountain south-
east of Lone Pine is underlain by long, narrow fault
blocks of Paleozoic rocks that trend northwest par-
allel to the mountain front. These fault blocks arc
composed of successively older rocks ranging from
Permian, high on the mountain front, to Ordovician
at its base. Ordovician rocks, consisting of the Ely
Springs Dolomite, the Eureka Quartzite, and the
Pogonip Limestone, crop out in two places, one near
Alico Siding and Dolomite, the other near Swansea.

Method of Work

Using the plane table method, a 2,000-foot by 900-
foot area, herein called the Lakeview area, that in-
cludes the principal Lakeview quarries was mapped
(Plate 1) on a scale of 1 inch equals 100 feet. Magnetic
azimuths were used, and a datum plane was chosen so
that Station A had an elevation of 4,200 feet, appro.x-
imately that determined by inspection of the New
York Butte quadrangle. A structure section, scale 1

inch equals 30 feet, was measured across the central part
of the Lakeview area. Outcrops of the Eureka
Quartzite between Alico Siding and Swansea were
plotted on a map (figure 1), scale 1:31,250, prepared
by enlarging a portion of the New York Butte quad-
rangle. Three and a half weeks were spent in the field
between November 1958 and October 1959.

Descripfive Geology

Between Alico Siding and Swansea, the Eureka
Quartzite occurs conformably in a sequence of pre-
dominantly dolomite beds that strike roughly parallel
to the mountain front. It is assumed that the Eureka
Quartzite is underlain by the Pogonip Limestone and
overlain by the Ely Springs Dolomite as is the case
in the nearby Talc City Hills.

As shown on figure 1, there are three outcrops of
the Eureka Quartzite. One trends southeast through
the Lakeview area and the Lakeview quarries to the
quartzite mill, where it disappears beneath the fan at
the mouth of a large canyon. The rocks dip southwest
at angles of 75° to vertical, and the younger beds lie
to the southwest. The second outcrop crosses the can-
yon mentioned above about 5^ -mile northwest of the
quartzite mill and runs south at an angle to the moun-
tain front to the edge of the alluvium just north of
Dolomite. The beds associated with the second out-
crop dip steeply to the northeast, and the younger
rocks lie to the northeast. The third outcrop crosses
the end of a spur just southeast of Swansea. As in the
outcrop near Dolomite, the beds dip steeply northeast.

iMost of the discussion that follo^\•s pertains to the
Lakeview area f Plate 1).

Stratigraphy

All the beds in the Lakeview area that underlie the
Eureka Quartzite are assumed to be upper members
of the Pogonip Limestone. The lowest unit, which
lies northeast of the Lakeview area except for a small
area near Station F, consists of 100 to 200 feet of
brown-weathering, siliceous beds composed mostly of
alternating siliceous and carbonate layers up to about
6 inches thick. The unit forms prominent outcrops
and is the most conspicuous unit associated with the
Eureka Quartzite in the Lakeview area. Practically all
the beds above the brown-weathering, siliceous unit
are composed of carbonate rock that is dark gray on
the fresh surface and lighter gray on the weathered
surface. The gray unit is about 250 feet thick. Most
of it is dolomite; but the lower 80 feet, difltcrentiated
on A-A Plate 1 but not on the map, is composed
of porous-weathering, gray limestone. Northwest of
the hairpin turn on the road to the north quarry,
where exposures are good, the gray dolomite contains
sparsely distributed lenses of brown sandstone about
24 inches in diameter and 8 inches thick. In the same
area, a bed of gra\' quartzite 3 to 5 feet thick occurs
about 100 feet below the top of the gray dolomite.
The same or a similar quartzite bed occurs on the

California Division of Mines and Geology

Bull. 187

.SOUTH OUARRV, LAKEVlEW- DEPOSlt ^ :'"'-' ^^Cr^~-\^^~' 'j '

^0/ ■ - , ^

118*^00'

K££LER I Ml.
fURNACF CREEK 0-4 M/

Figure 1. Geologic mop of Eureka Quartzite near Owens lake. New York Butte 15-minute quadrangle, Inyo County. By W. E. Ver Planck, Oct.
7-8, 1959.

1966

QUARTZITE

s^^m^,_

..jf-

Photo I. Lokeview Quortzite deposif: View northwest along ttie strike of steeply dippjng Urdovician rocks at the base ot the Inyo Mountains
near Dolomite. The siliceous brown beds of the Pogonip Limestone are at the right ecJge of the dark outcrop. The Eureka Quortzite, center, is
marked by the white cuts and dumps.

hillside east of Station C, but no quartzite was ob-
served in the poorly exposed dolomite between Sta-
tion B and Station F. Outside of the Lakeview area
the contact between the gra\' dolomite and the over-
lying Eureka Quartzite seems to be conformable;
but in most of the area the two formations are sepa-
rated by an outcrop of soft, white, granular material
that contains abundant calcite. This relationship is
further discussed under structure.

The Eureka Quartzite forms two prominent out-
crops, one extending northwestward from the vicinity
of the north quarry, the other in the vicinity of the
south quarry and the talc workings. The two areas
are separated by a flat, alluvium-covered saddle in
which bedrock does not crop out. The formation,
which is about 400 feet thick, is divisible into a lower,
impure, relatively thin-bedded part containing much
iron-stained quartzite, and an upper part of massive,
uniform, and more pure quartzite. Except in artificial
openings the Eureka Quartzite is uniformly covered
with quartzite debris that conceals its details.

The contact between the Eureka Quartzite and the
overlying Ely Springs Dolomite, as exposed in the
quarries, is sharp and conformable. The Ely Springs,
which consists of about 150 feet of gray dolomite, is
made up of a lower unit of nodular dolomite and an
upper unit of gray dolomite, which is nodule-frcc.

The lower unit is characterized by the presence of
closely spaced, lenticular nodules up to 6 inches in
diameter that arc composed of rrcmolite and calcirc.
The weathered surface, \\ ith its projecting, dark-gray

to black nodules, is distinctive. Nodule-free beds of
gray dolomite occur, in places, close to the base of
the Ely Springs. Higher in the section, beds with
nodules become fewer; and there are none in the
upper, or gray dolomite, unit. The base of the gray
dolomite unit \\as mapped at the top of the highest
nodular bed.

The gray dolomite unit of the Ely Springs is very
similar to the gray dolomite of the Pogonip. Both con-
tain disseminated tremolite crystals about 0.05-inch
long and also clumps of bladed tremolite crystals.

The gray dolomite of the Ely Springs is overlain
b\' two dolomite units that the writer has not identi-
fied. Thcv are shown together as "white dolomite" on
Plate 1. The lower unit consists of about 100 feet of
pale gray dolomite with abundant disseminated tremo-
lite needles as much as %-inch long. It contains a few
white dolomite beds 1 to 5 feet thick. The pale gray
trcmolitic domolite is overlain by a thick upper unit
of massive, coarsely crystalline white dolomite that
seems to extend uniformly from the southwest edge
of the mapped area to the valley floor. The \\ eathered
surfaces of the two units are similar. Both have a
sandy texture and are tan in color. The weathered
surface of the pale gray tremolitic dolomite is onl\-
slightl\- darker than that of the white dolomite.

The Eureka Quartzite and the dolomite beds above
and below it are cut by dikes of deeply weathered
porphyritic diorite with phenocrysts of hornblende
and feldspar. The dikes are a few inches to 5 feet
\\ idc. Probably most are approximately parallel to the

California Division of Mines and Geology

Bull. 187

Photo 2. Eureka Quartzite near
Lakeview Talc workings: View of
the slope southeast of the south
quarry (sky line) showing cuts and
dumps of Lakeview talc deposit
along the contact of the Eureka
Quartzite (left) with gray dolomite
of the Pogonip Limestone (right).

bedding of the sedimentary rocks, but some cut across
the bedding.

Granitic rock intrudes the Eureka Quartzite just
north of Dolomite, but was not observed elsewhere
in the Alico-Swansea area. Near Dolomite, a sill-like
body of granitic rock 50 to 100 feet thick occurs in
the quartzite a few feet below its contact with nodu-
lar dolomite and has penetrated cracks in the quartzite.

Structure

Throughout the Lakeview area the beds strike
northwest and dip steeply south^\•est except in the
north corner, where they are overturned. They lie on
the west limb of a faulted anticline, the cast limb of
whicii is represented by the east-dipping Eureka
Quartzite and associated rocks north of Dolomite.
None of the major faults that occur in the Alico-
Swansea area was located, but minor faults are nu-
merous. One is a bedding plane fault that, to the
northwest of the Lakeview area and for most of its
length within it, separates the Eureka Quartzite from
the Pogonip Limestone. From a point about 300 feet
due cast of Station C to the soutiieast edge of the
Lakeview area, where the beds depart from their gen-
eral northwest trend, it cuts across the Pogonip beds.
At the southea.st edge of the Lakeview area and to the
southeast it is a bedding plane fault in the Pogonip
limestone. The fault trace is a strip 30 to 60 feet wide
of powdery material that contains calcite. It is exposed
in road cuts near the hairpin turn on the north quarr\-
road, in a prospect pit east of the road, and in a tunnel
east of the talc workings. East of the South quarr\-,
where exposures arc poor, the fault trace probably is
represented by a strip of soft soil.

It is to be noted that in the Lakeview area only about
150 feet of the gra\' l'"l\' Springs Dolomite lies above
the Eureka Quartzite compared with 920 feet in the
Talc City Hills (Hall and .Mackevett, 1958, p. 7). A

bedding plane fault ma\- cut off the Ely Springs Dolo-
mite, but the writer found no evidence of it.

In the vicinity of the talc workings, the quartzite
outcrop terminates along an irregular boundary as if
it had broken by tension acting in a direction parallel
to the strike. A quarter of a mile to the southeast and
outside of the Lakeview area is the end of another
body of quartzite that has the same relationships with
the Pogonip and El\- Springs beds as the quartzite in
the Lakeview area. This southern body of quartzite
disappears beneath alluvium at the quartzite mill, still
farther to the southeast, .\long the southeast edge of
the Lakeview area the El\' Springs beds and the white
dolomite that overlies them swing east, and southeast
of the Lakeview area, the white dolomite occupies the
space where quartzite might be expected. The area
between the two quartzite bodies is complexly faulted
so that the gray dolomites of the Ely Springs and of
the Pogonip, which elsewhere lie above and below the
quartzite, are in fault contact.

There may be a similar discontinuity of the quartzite
beneath the saddle between the north and south quar-
ries. The writer found no outcrops in the saddle itself
or on the slope west of it. Scanty evidence of a cross
fault was found to the east, where a gull\' from the
saddle crosses the siliceous brown beds of the Pogonip.
Cross faults do offset the Eureka Quartzite and the
siliceous brown beds northwest of the Lakeview area.

The Eureka Quartzite in Detail

The Eureka Quartzite in the ."Mico-Swansea area is
not cspcciall\- uniform. Onl\' a portion of the forma-
tion is of high purit\-, and the sections exposed in the
various quarries are not identical.

In the Lakeview quarries, high-purity quartzite seems
to be confined to the uppermost 100 to 150 feet of the
fonuation. It consists of massive, gra\ish quartzite with
bedding plane slips or joints 10 to 15 feet apart. These

1966

QUARTZITE

joints are I to 6 inches thick and filled with iron-
stained, soft, calcite-bearing material. On the hanging
wall side, a few feet of dark gray to black quartzite
separates the massive quartzite from the overlying
nodular dolomite beds. On the footwall side, the mas-
sive quartzite is bounded in some places by lower grade
quartzite and in other places by a dike. The main part
of the Eureka Quartzite, 250 to 300 feet thick, consists
of iron-stained quartzite, platy black, impure quartzite
with disseminated pyrite, slaty phyllite, thin carbonate
beds, and relatively thin beds of unstained quartzite.
Dikes are abundant. Joints are filled with powdery
calcite, probably caliche derived from the carbonate
rocks of the area.

South of the saddle, the Eureka Quartzite has been
exposed b\' benches of the south quarry that almost
encircle the knoll surmounted by Station C. As shown
on Section A-A and Table 2, the massive hanging wall
unit, which consists of high-purity quartzite, is about
110 feet thick in this area. Analyses 1 and 2, Table 1,
indicate, however, that only the upper 55 feet (unit 6,
Table 2), which consists of medium gray, vitreous
quartzite, contains less than 0.25 percent impurities.
Analyses 3 to 5, Table 1, indicate that the quartzite
from the lower 55 feet (unit 5, Table 2) contains 0.25
to 0.5 percent impurities. Megascopically, the quartzite
from the lower section is similar to that of the upper
except that it contains streaks of darker gray and is cut
by iron-stained cracks.

No significant difference was detected with the
microscope. The quartzite consists of a mosaic of an-
hedral, irregularly interlocking quartz grains, many
of which exhibit strain shadows. In size they range
from 0.05 millimeters to as much as 3 millimeters and
average 0.3 to 0.6 millimeters. Traces of the original
rounded sand grains are present but are largely oblit-
erated by the recrystallization that resulted from meta-
morphism. Non-quartz grains are very sparse and only
a little more abundant in the dark, stained quartzite
than in the clean gray quartzite. They include clumps
of sericite 0.01 to 0.1 millimeter in diameter composed
of crystals in the order of 0.005 millimeters in longest
dimension, muscovite and biotite flakes up to 0.1 milli-
meter in longest dimension, and iron oxide grains 0.05
to 0.1 millimeters on a side. Feldspar was not observed.

The main part of the formation, about 260 feet
thick, is relatively thin-bedded and impure but contains
layers of clean gray quartzite up to 10 feet thick in the
central part. (Analysis 6, Table 1). The basal 145 feet
(unit 1, Table 2) consists of thin-bedded, shaly, black
quartzite with abundant iron stain and caliche-filled
cracks.

Some interesting impure rocks occur interbedded
with high-purit\- quartzite in the middle part of the
formation. The 25-foo? section of quartzite just below
the massive hanging wall unit (unit 4, Tabic 2) con-
tains platy, black, layers with disseminated pyrite,
much of which is altered to limonite. In thin section
the black quartzite is seen to be composed of quartz

Table I. Chemical Analyses of Quartzite from
Lakevieiv Deposit '
(in percent)
1 2 S 4 S

99.59
0.14
0.00
0.00
0.10
0.02
0.00
0.02
0.02
0.11

99.35
0.31
0.07
0.00
0.00
0.00
0.00
0.01
0.07
0.19

99.25
0.45
0.00
0.00
0.11
0.02
0.00
0.02
0.07
0.04

99.23
0.45
0.14
0.00
0.00
0.00
0.00
O.OI
0.02
0.15

99.57
0.37
0.05
0.00
0.08
0.00
0.00
0.01
0.02
0.04

Division of Mines laboratory, June 1961.

Si02= 99.66

.•\l2O3 0.16

FejOa' 0.00

TiO= 0.00

P:05 _ 0.00

CaO 0.00

MgO 0.00

Na^O 0.02

K=0 0.02

H=0' 0.14

1 Analyses by W. H. Nisson,

- By difference.

^ Total iron.

' Loss on ignition.

1 Sample Al-3, 402 feet from southwest end of section A-A',

Plate 1.

2 Sample A 1-4, 441 feet from southwest end of section A-A',

Plate 1.

3 Sample Al-5, 454 feet from southwest end of section .A-.\',

Plate 1.

4 Sample Al-6, 469 feet from southwest end of section A-\\

Plate 1.

5 Sample Al-7, 500 feet from southwest end of section A-A',

Plate 1.

6 Sample Al-9, 530 feet from southwest end of section .\-A',

Plate 1.

with as much as 10 percent of fine-grained claylike
material, sericite, limonite, mica, and zircon. The
quartz occurs mostly as a mosaic of irregular, inter-
locking grains 0.07 to 0.2 millimeters in size and also
as rounded grains 0.3 to 0.7 millimeters in size, rnan>-
of which are composed of more than one crystal. Li-
monite forms cubes 0.07 to 0.3 millimeters on a side. Py-
rite was not observed in the thin section examined. The
clay and sericite occur as thin films 0.005 millimeters
wide between quartz grains, as clumps 0.07 to 0.2 milli-
meters in diameter, and as veinlets up to 0.1 millimeter

Table 2. Section of Eureka Quartzite at South Quarry,
Lakei'ieiv Deposit.

Stratigraphic thichiess
(in feet)
Ely Springs Dolomite
Eureka Quartzite

Upper, massive unit of high-purity quartzite
6. Massive, medium-gray, stain-free quartzite 55
5. Massive quartzite with dark gray streaks

and iron-stained cracks 55

Lower (main) unit, relatively thin-bedded and
impure

4. .Medium-gray quartzite, quartzite with
dark streaks, and platy, black, pyrite-
bearing quartzite _ 25

3. Medium-gray quartzite and soft, gray,
clay-like layers — 35

2. Medium-gray quartzite and relatively hard,
tremolitic, quartz-rich rock 55

1. Thin-bedded, shaly, black quartzite with

iron stain and caliche-filled cracks 145

Fault

Pogonip Limestone

California Division of Mines and Geology

Bull. 187

wide. Clay and sericite have penetrated and embayed
the quartz grains, and much of it is iron-stained. One
rounded zircon grain 0.2 millimeters in diameter was
observed. It is interesting that these iron-bearing beds
pass beneath the summit of the knoll, and the high-
purity quartzite lies beneath its flank. Locally at least,
high-purity quartzite cannot be distinguished by its
resistance to weathering.

A 35-foot section near the center of the formation
(unit 3, Table 2) consists of beds of medium gray,
stain-free quartzite, up to 5 feet thick, separated by
layers of soft, yellow-green and gray, clay-like mate-
rial. Little could be identified with the microscope
e.xcept abundant tremolite and sparse, rounded quartz
grains. Some quartzite has been quarried from this
unit.

The 55-foot section below the one just described
(unit 2, Table 2) consists of quartzite beds separated
by layers of relatively hard, tremolitic, quartz-rich
rock. Thin sections of two specimens were e.xamined.
One consists of interlocking quartz grains 0.07 to 0.3
millimeters in size with 20 percent tremolite; the other
(photo no. 4) consists of rounded quartz grains, some
composed of more than one crystal, with 40 percent
tremolite. The tremolite occurs as thin films between
and penetrating quartz grains, as crescent-shaped
clumps 0.07 by 0.3 millimeters between quartz grains,
and as clumps as much as several millimeters in diam-
eter that completely surround one or more quartz
grains. Limonite cubes pseudomorphous after pyrite
0.07 millimeters on a side are present but not abundant.

Photo 4. Photomicrograph of quartz-rich rock from the midcJIe port
of the Eureka Quartzite, Lakeview deposit. Rounded quartz groins in
a matrix of tremolite. Plane polarized light.

Photo 3. Photomicrograph of Eureka Quartzite from Lakeview
deposit. Sample Al-3 from the high-purity upper port of the forma-
tion, consisting almost entirely of quartz. Crossed nicols.

.Much of the tremolite is in the form of interlocking
needles in the order of 0.02 by 0.1 millimeters, but in
tremolite-rich areas it forms single crystals as much as
1 millimeter across.

The origin of the soft, cla\-like lasers in unit 3
and the tremolitic, quartz-rich layers in unit 2 has not
been determined. Perhaps the central part of the
Eureka Quartzite ma>' once have been a sequence of
sand beds alternating with sandy dolomite or lime-
stone beds. It is possible that the solutions that pro-
duced the talc at the Lakeview talc xvorkings, which
are onl}- about 500 feet from the south quarry, may
have altered the carbonate layers into cla\' and tremo-
lite, leaving the disseminated quartz grains unchanged.
It is to be noted that elsewhere in the Lakeview area
dolomite contains only disseminated tremolite crystals.

Nortii of the saddle, the upper high-puritv part of
the Lurcka Quartzite is exposed in the north quarry,
but the main part of the formation is exposed only in
cuts along the north quarry road. As shown on section
B-B', Plate 1, and Table 3, the hanging wM unit of
massive, high-purity quartzite (unit 4) is about 150
feet thick. The main parr, which is about 300 feet
thick, contains a second unit of massive quartzite
(unit 2, Table 3,) 50 feet thick and 50 feet above the
base o( the formation. This quartzite is similar to the

1966

QUARTZITE

hanging wall unit, except that it contains sparsely
disseminated specks of iron oxide. It has not been
developed and is assumed to be non-commercial. Be-
tween these massive quartzite units lies a sequence of
less resistant beds (unit 3, Table 3) consisting of rela-
tively thin quartzite beds, dikes, and thin carbonate
layers. The basal 50 feet of the formation (unit 1,
Table 3) consists of platy, black, iron-stained phyl-
lite. The two massive quartzite units persist northwest-
ward be_\'ond the limits of the Lakeview area. South of
the saddle, however, nothing was found within the
main part of the formation that corresponds to the
lower quartzite unit.

Outside of the Lakeview area, the Eureka Quartzite
is exposed near the quartzite mill and near Swansea.
At the quartzite mill, the formation, which is over-
turned and dips steeply east, has been benched across,
exposing the contacts of the Eureka Quartzite with
nodular dolomite of the Ely Springs on the west and
with a dike on the east. The Eureka Quartzite is about
300 feet thick and is mostly thin-bedded, impure
quartzite with shal\' layers and dikes. It seems to lack
the upper unit of massive, high-purity quartzite.

A section of the Eureka Quartzite about 200 feet
thick is exposed in the quarry near Swansea. Pogonip
Limestone lies beneath the quartzite to the west, and
the quartzite is overlain by nodular dolomite of the
Ely Springs to the east. Faulting complicates the rela-
tions south of the quarry. The quartzite is highly

Table 5. Section of Eureka Quartzite at North Quarry,
Lakeview Deposit.

Ely Springs Dolomite Stratigraphic tliickness

Eureka Quartzite (in feet)

Upper, massive unit of high-purity quartzite

4. Massive, medium-gray, stain-free quartzite 150
Lower (main) unit, relatively thin-bedded and
impure

3. Relatively thin-bedded quartzite and thin

carbonate layers 200

2. Massive, medium-gray quartzite with dis-
seminated grains of iron oxide 50

1. Platy, black, iron-stained phyllitc 50

Fault

Pogonip Limestone

brecciated and contains steeply dipping layers of soft
material 5 to 10 feet wide. The quartzite itself is a
light to medium gray, vitreous material that averages
0.105 percent alumina and 0.085 percent alkalies.*

Talc is associated with the Eureka Quartzite near its
discontinuity in the southeastern part of the Lakeview
area. The largest deposit is at the Lakeview talc work-
ings, where it occurs close to the footwall contact of
the quartzite and apparently is a replacement of the
quartzite. Some talc also occurs near the northwest end
of the quartzite body that lies southeast of the Lake-
view area. No talc was observed northwest of the
Lakeview talc workings.

* Average partial analysis of quartzite shipped in July 1954. Arthur G.
Moore, written communication, March 1961.

^^it^

Photo 5. South Quarry, Lakeview Quartzite deposit, in 1957: View of the northwest end of the south quarry showing an early stage in the
quarrying of the massive, high-purity, hanging wall beds of the Eureka Quartzite. Photo by L. A. Wright

California Division of Minks anu Geology

Bull. 187

Photo 6. South Quarry, Lakeview Quartzile deposit, in March 1957. View of the northwest end of the south quarr>
showing initial operations in the top central part of the Eureka Quartzite. The lower face has been drilled with horizontal
holes and loaded ready for blasting. The equipment on the upper bench is being used to clean up loose rock preparatory to
drilling.

Operations

In 1953, Gladding, McBean & Co. conducted an in-
tensive search in the Alojave desert region for quartzite
suitable for the manufacture of super duty silica brick
(Brooks, 1955). A quartzite was desired having less than
0.25 percent alumina and alkalies and meeting certain
physical specifications, including a proper size distri-
bution of the crushed material. Late in 1953, samples
of the Eureka Quartzite from outcrops near the Cerro
Gordo mine. Talc City, Keeler, and Independence
were tested, and satisfactory test bricks were prepared.
The company then narrowed its search to the east face
of the Inyo Mountains northwest of Keeler, \\here
the Eureka Quartzite is closer to rail transportation
than anywhere else in California. During 1954, plant
run tests were made on 800 tons of quartzite, and
possible quarry sites were evaluated. Commercial pro-
duction began in August 1955. During 1955 and the
first part of 1956, quartzite was obtained from the
deposit near Swansea. Operations were then trans-
ferred to the Lakeview deposit.

Lakeview quarries

Location: NE'/4 Sec. 4, T. 16 S., R. 37 E., M.D.,
6'/4 air miles east southeast of Lone Pine. 0\vncr:
Gladding, McBcan & Co., 2901 Los Feliz Boulevard,
Los Angeles 39. General Refractories Company has an
interest in the operation \\hich, in effect, allows it to
obtain what cjuartzite it needs. The quarrying, proc-
essing, and hauling of the quartzite to tiie railroad
loading point south of Lone Pine is done on contract
by the Brownstone Mining Company, William Skin-

ner and Gus V'oget, P.O. Box 396, Bishop. Brown-
stone Mining Company owns the quartzite mill. Sev-
eral tens of thousands of tons of quartzite have been
produced since 1956 for the manufacture of super
duty silica brick.

The property consists in part of lode claims located
by H. Stewart and H. Taylor of Big Pine, who de-
veloped the Lakeview talc deposit, and in part of addi-
tional placer claims located by Gladding, McBean &
Co. after 1953. Quartzite was obtained at first from
the south quarr)-. In March 1957 a stratigraphic thick-
ness of about 100 feet in the top central part of the
formation had been opened, and careful work was
required to separate the comparatively' thin layers of
quartzite from the interbcdded waste. This part of
the quarr\' has not been worked since then. Later in
1957, the quartzite was stripped across its full width,
exposing mixed low-grade material to the cast and
massive high-purit\- quartzite to the west of the orig-
inal workings. A substantial tonnage was taken from
the west side workings, but it seems unlikely that
much more could be obtained there xvithout forming
a steep, high, and dangerous face or moving a pro-
hibitive amount of waste. The north quarry was
opened in 1958. Probably future operations xvill be
conducted there, because the topography is such that
comparatively little stripping is necessary, and because
the hanging wall unit of high-purity quartzite is
thicker than at the south quarry. In the north quarry-
area, readily obtainable reserves in the massive, hang-
ing wall unit arc in the order of half a million tons.

1966

QUARTZITE

The quarry is operated whenever it is necessary to
replenish the stock pile of processed quartzite, from
which shipments are made continuously. Benches 10
to 20 feet high are maintained by blasting horizontal
holes. Wagon drills with tungsten carbide insert bits
are used, and tiie charges are detonated with electric
caps. Dump trucks of about 10 tons capacity take the
broken rock to the quartzite mill, which is about half
a mile southeast of the quarries and not far above the
level of the valley. At the mill the quarry rock is first
run through a jaw crusher and then sized with a
double trommel that has a coarse screen placed inside
a fine screen. The oversize is crushed again with a
second jaw crusher and recirculated through the
screen; and the undersize, which contains most of the
impurities present in the quarried rock, is discarded.
The middle size, approximately minus 2 inches and
plus '4 inch, is trucked to the stockpile and railroad
loading point near Lone Pine. Electric power for the
operation of the mill is generated at the site.

Swansea quarry

Location: SE'4 Sec. 24, T. 16 S., R. 37 E., iM.D.,
'/2 mile southeast of S\\"ansea -and 1 1 air miles south-
east of Lone Pine. Owner: Inyo Marble Company;
leased to Gladding, .McBean & Co., 2901 Los Feliz
Boulevard, Los Angeles 39 (1961). A substantial ton-
nage of quartzite for the manufacture of super duty
silica brick was produced on contract by Mineral
Materials Company in the latter part of 1955 and the
first part of 1956. All equipment has been removed
from the property.

The quarr\' has been opened on the northwest end
of an outcrop of the Eureka Quartzite that crosses a
projecting nose of the Inyo Mountains. It has been
driven southeast several hundred feet and has three
benches 10 to 20 feet high, the lowest of which is about
25 feet above the level of the highway. Reserves are
several hundred thousand tons.

Dolomite

Brownstone Mining Compan\', operator T){ the
Lakeview quartzite quarries, produced dolomite at
times in 1958 and 1959 when the quartzite operation
was idle. A quarry in white dolomite was developed
just south of the mapped area, and test cuts were
made elsewhere, including one in the \\ hite dolomite
west of the north quarry. Several hundred tons of
dolomite were processed for white roofing granules
and terrazzo chips in the quartzite mill, which was
modified for this purpose by the addition of fine
screens, bins, and sacking equipment. The dolomite
venture was not successful, in part because the pres-
ence of dikes made the quarrying of clean dolomite
difficult, and in part because of marketing difficulties.
Some dolomite was sold locally as garden rock.

Talc

The talc deposit on the Lakevie\\' propert)', \\ hich
is called the Lakeview talc deposit, was located and
developed by H. Taylor and H. Stewart of Big Pine

^ttti^-.vm

Photo 7. Mill, Lakeview Quartzite deposit; Quarry-run rock is
crushed and sized with jaw crushers and a trommel screen to approxi-
mately minus 2 inches, plus Vi inch. The tines, which contain most of
the impurities, are discarded.

On the hillside above the mill, dark nodular dolomite of the Ely
Springs (left) is in contact with the Eureka Quartzite (right). The
section is overturned here. Camera facing northwest. Photo by L. A.
Wright.

(Norman and Stewart, 1951, p. 118). The workings
explore a steeply dipping body of talc 7 to 10 feet
wide along the footwall of the Eureka Quartzite
where it seems to be broken off. They consist of a
75-foot adit, which at the portal follows the quartzite-
dolomite contact, and a winze sunk close to the portal.
A shaft on the hillside above the portal probably con-
nects with the adit near its face. In 1947, some talc
was obtained from a stope above the adit level and
shipped to a mill at Zurich, Inyo County. The mine
has been inactive since December 1947.

Quartzites of the Oro Grande Series
near Victorville

Units of the Oro Grande Series near Victorville, San
Bernardino County, have furnished several million tons
of high-purit\- quartzite since 1928. Most of the output
has been consumed by the portland cement industry,
but up to 1955 some of it was used in the manufacture
of silica brick.

The Oro Grande Series of late Paleozoic, probably
Carboniferous, age is limited in occurrence and is non-
uniform compared with some of the early Paleozoic
formations of the Basin-Range province. At the type

18 California Division of Mines and Geology Bull. 187

Table 4. Cheviical Analyses of Quartzite fro?)! the Series on the northeast slope of Quartzite Mountain is

Oro Grande-Victorville District. as follows, bottom to top, average thickness in feet:

(in percent) ^ ^jj ^^.j^j^.^ dolomite, 1,200; (2) dark schist-hornfels,

350; (3) blue-gra\- limestone, 250; (4) schist-quartzite,

SiO= 99.04' 99.37^ 98.90 99.04 98.57 ^q. (5) lo^.-gr quartzite, 250; (6) black schist with

fS :.:.:.r.. S'-t^ 2:^8 l\l S:n SS Uniestone subunits,500; (?) upper quartzite, 250.

•j-jOj 0.0 0.0 0.04 0.04 0.05 ■'■"^ '^^^'° quartzite units are indistinguishable from

P,Ob 0.0 0.0 - - - each other. They are composed of vitreous, light to

CaO 0.0 0.0 0.23 0.15 0.05 medium gray, massive quartzite \\ith only occasional

•MgO 0.0 0.0 0.08^ 0.04^ 0.17^ suggestions of bedding. Weathered surfaces and joint

Na=0 0.014 0.01^ 0.24- 0.^2 0.15 surfaces commonlv are ironstained. Chemical analvses

KjO 0.200 0.009 - - - • ■ T u.' , T u- • u ■■ •

j^^Q Q1Q QQg _ _ _ are given in labia 4. In thin section, the quartzite is

1 By difference. Seen to be composcd mostly of quartz in the form of

2 Total alkalies. irregular, interlocking grains ranging from 0.2 to I

1 Upper quartzite from SEK SEW Sec. 9, T.6.X., R.4.W., millimeter in diameter. The rounded outlines of the

S.B. Analysis by W. H. Nisson and Lydia Lofgren, Di- original sand grains can be detected here and there but

vision of Mines laboratory, August, 1961. j^^^stlv have been obliterated. Finelv divided sericite is

2 Lower quartzite from SEV; NE'/. Sec. 16 T.6N R.4.\\ .. ^^.j^gi^. dis^ibuted but not abundant, both along grain

S.B. Analysis by W. H. Nisson and Lydia Lofgren, Ui- , ■ . ,.,,,.,. . ^„'^. .

vision of .Mines laboratory, August, 1961. boundaries and included ^\•lthln quartz grains. Calcite

3 Typical analysis of quartzite from the Atlas quarry. Analysis ^^'^^ not detected, and feldspar is very scarce. Minute

furnished by Gladding, .McBean & Co. (Bowen, 1954, p. grains of sphene, tourmaline, zircon (?), magnetite,

176). biotite, limonite, and pyrite were identified but are not

4 Clean quartzite from the Emsco quarry. Analysis furnished abundant.

by Gladding, .McBean & Co. (Bowen, 1954, p. 178). -phe stratiirraphic sections of the various fault blocks

5 Typical analysis of quartzite from the Riverside quarry. cannot be correlated with the type section with COn-

.-Vnalysis furnished bv Gladding, McBean & Co. (Bowen, r , v , ri/-> ■ nt

1954 p 178) ' ndence because the structure of the Quartzite Moun-
tain area is complex and the units of the type section

locality on Quartzite .Mountain, and within an area of 'f ^^ characteristic properties. It is thought, however,

about ^ square miles (Plate 3) the series contains, ho^^-- ^^at most of the massive quartzite units probably are

ever, large masses of uniform, high-purity quartzite. equivalents of unit 7 of the type section.
Limestone deposits, associated with the quartzite, arc

of great commercial importance and for many years Uuor z/ e ijuames ^^^^^

have supplied portland cement plants at Victorville Location: NE'4 SE'/. Sec. 17, T. 6 N., R. 4 W., S.B°!

and Oro Grande. The Quartzite Mountain area lies .•- j„ ^j,^^ northeast of Oro Grande. Owner: Mineral

miles north of \ ictorvil e and 1 to 4 miles east or Oro ,," • i /- ii .--n- ,. • „ \ „ \ u, „

„ , „- ., , -1 , , • 1 t t .Materials Company, 114.1 Westminster Avenue, Alham-

Grande, or 8) miles by railroad or highway from Los t, c- • j ■ in^n ,.u \»i .- ,.,,.,- i,.,^

, , r. 1 ir. ■■,, J <-x ^ J 1 bra. Since it was opened in 1939, the Atlas quarrv has

Angeles. Both \ ictorville and Oro Grande are on the , , , -^ „nn I taa nnn » c ,. v„ „'^.^i,.

^, . , „ „ , ^^ . _, .^ ... . produced 1>0,000 to 200,000 tons of quartzite, mostly

combined Santa re and Union Facinc main line to Los ^ , , >i j . i . • ,u„,„ nSi

, , ,, TTOTTi .^^, for sale to portland cement plants in southern Cau-

Angclcs and close to U.S. Higiiway 66-91. r ■ n S mrr c ^x » ► ^^a <•„..

^ ^ ■' forma. Up to 19.15, some of the output was used tor

Previous Work and Acknowledgments silica bricK.

The Quartzite Mountain area is included in Bowcn's . The deposit consists of a lenticular, partly fault
( 1954) report on the geology and mineral resources of hounded mass of quartzite 100 to 2?0 feet thick, 900
the Barstow 30-minute quadrangle. As part of a larger ^^^ long, and ^^■.th a maximum width of >00 feet. The
study, the U.S. Geological Survey remapped the area, quartzite is thoroughly fractured, and m places it con-
using the newly available 15-minute base maps (Dib- tains clay-fiUcd seanis up to !:-inch thick. Most joints
blee: 1960). Bowen and Ver Planck (1965) also have ^''^, ""on-stamed. The deposit is underlain by schist
remapped the Quartzite Mountain area on a scale of ^'",''- '^" ^'^^ ^^^ '''^': '^ f'^'" '^"^ "/ imcstonc. A typi-
1 : 12,000 and have described its nonmetallic mineral "'''">'"' "^ ^"^'"^'^'^ *■■"'" ^'^^ ^^'^^^ 'l"^"-".^' '^ S'^"^"
resources. The discussion that follows is summarized in a e .
from that report. Reserves of easily obtainable high-purit\' quartzite

probably arc relatively small.

Descripf/Ve Geology -phg deposit has been opened from the east side. The

The Oro Grande Series is a sequence of mctamor- quarry is semicircular with benches 20 feet high and
phic rocks that has been complexly folded and faulted. is 800 feet long and up to 300 feet wide. Blast holes arc
Rocks of the Triassic (?) sidewinder Volcanic Scries made with -wagon drills that use steel with tungsten
intrude and overlap the Oro Grande Series. Both series carbide insert bits. In 1960 the practice was to work
are intruded by granitic rocks of early Cretaceous or the quarry intensively about once a year and to main-
late Jurassic age. The t\pe section of the Oro Grande tain a stock pile of quarry-run rock in the Los Angeles

1966

QUARTZITE

1 9 f

Photo 8. Atlas quarry, Mineral Materials Company: View northwest across lower bench.
Company has quarried 150,000-200,000 tons of quortzite, mostly for portlancJ cement.

Since 1939, Mineral Materials

area. When the quarry furnished quartzite for sihca
brick, the company had a crushing and screening plant
at the quarr\- for the removal of fines. The fines con-
tain most of the impurities present in the quarry-run
rock.

fmsco (Emsco Quartzite)

Location: NW'/4 NE'/4 Sec. 11, T. 6 N., R. 4 W.,
S.B., 4.2 miles east northeast of Oro Grande. Owner:
Southwestern Portland Cement Company, 1034 Wil-
shire Boulevard, Los Angeles 17. The quarry was
opened about 1928 by Emsco Refractories Company,
now a division of Gladding, A4cBcan & Co., and has
produced about 100,000 tons of quartzite for silica
brick. It \\as last operated about 1945.

The quarry has been opened in a ridge of quartzite
that borders the valley east of Quartzite Mountain. The
quartzite has a maximum exposed width of 400 feet.
It dips north-west at 40° to 60° and is overlain by lime-
stone that has been quarried on a large scale for use in
the manufacture of portland cement. To the east it
is overlain by alluvium and very likely is cut off by
intrusive granitic rock only a short distance cast of
the alluvium contact. The quartzite is shattered and
cut by dikes of granitic rock. Reserves are about 3
million tons. The quarry measures 300 feet by 300 feet
and has a face up to 75 feet high. No equipment re-
mains on the property. An analysis of clean quartzite
from the Emsco quarry is given in Table 4.

Riverside Cement Company

Location: NE% NW'/4 Sec. 17, T. 6 N., R. 4 W.,
S.B., 1 i 4 miles northeast of Oro Grande. Owner: River-
side Division, American Cement Co., 621 South Hope
Street, Los Angeles 17. The quarry has been operated
intermittently since about 1940 and has furnished
several hundred thousand tons of quartzite, mostly for
Riverside's portland cement plant at Oro Grande. It
also has furnished quartzite for the manufacture of
silica brick.

The deposit consists of massive quartzite that occu-
pies most of an isolated hill 700 feet in diameter that
rises about 100 feet above local ground level. The
quartzite dips north and is underlain by schist. The
quartzite is fractured and iron-stained near a north-
trending fault zone that crosses the deposit. A t\pical
analysis of quartzite from the Riverside quarry is given
in Table 4.

The quartzite on the cast half of the deposit has been
cut down 50 to 100 feet below the original top of the
hill. An estimated 1 Yi million tons of quartzite remain
above the level of Oro Grande Canyon, w hich is just
nortii of the deposit.

Southwesfern

Location: W'/z NE'X, SE'X NVV;4 Sec. 11, T. 6 N.,
R. 4 VV., S.B., 4.1 miles cast northeast of Oro Grande.
Owner: Southwestern Portland Cement Company,
1034 Wilshirc Boulevard, Los Angeles 17. At one time
the Southwestern Portland Cement Company obtained
limestone and other portland cement raw materials on a

California Division of Mines and Geology

Bull. 187

large scale from a group of ten quarries in section 1 1 .
Since the quartzite deposits were opened, about 1928,
more than a million tons have been produced for the
company's plant at \"ictor\ilIe. Little if any quartzite
has been quarried since 1951 when the company began
to use limestone with a higher silica content than that
which was used before.

The deposit consists of a ridge of massive quartzite
bordering the valley east of Quartzite Mountain and in
the northern part of which is the Emsco quarry. The
quartzite forms a steeply dipping body up to 750 feet
wide with an outcrop length of 2,500 feet. It is bor-
dered on the west by limestone and on the east by
alluvium, beneath which granitic rock has intruded
and cut off the quartzite. As indicated by bore hole
analyses, the deposit ranges from 83 to 96 percent silica
and averages about 94 percent silica.

Quartzite has been obtained from several places. A
quarry at the south end of the quartzite hill, just north-
east of the center of section 11, measures 300 feet by
1 50 feet and has a face 40 feet high. At the north end
of the same hill, some quartzite has been obtained from
the east side of a quarry that was worked mostly for
limestone. A large tonnage of quartzite also has been
taken from south end of the same outcrop. Reserves
of quartzite within 100 feet of the surface are estimated
to be 10 million tons.

Some Undeveloped Deposits

Many millions of tons of quartzite without over-
burden are exposed on the summits and upper slopes
in the central part of the Quartzite Mountain area. No
roads have been built into these areas, and, so far as
known, the quartzite deposits have not been sampled
by the operating companies. The quartzite of the
Quartzite .Mountain northwest and Quartzite Mountain
(upper unit) deposits seems to be less fractured and to
contain fewer impurities than that of the other deposits
described below.

Klondike

Location: SW'/4 NE'/4 Sec. 17,T. 6N., R. 4 W., S.B.,
1 'X miles northeast of Oro Grande. Owner: Riverside
Division, American Cement Co., 621 South Hope
Street, Los Angeles 17. The deposit consists of a large
body of quartzite that has not been developed but is
readily accessible.

The ridge east of the Shay and Klondike quarries is
capped by massive quartzite that lies in the a.xis of a
plunging s\ncline. The outcrop area is 1700 feet long
and 600 feet wide, and the quartzite is several hundred
feet thick. A granitic dike bi.sects the deposit close to
its long axis. The quartzite is limited by the Klondike
fault to the west and is underlain by schist, whicli
crops out on the east side. Reserves within 100 feet of
the surface are 8 million tons. The deposit could be
developed easily from the road to the upper benches
of the Klondike quarry, which crosses the north end
of the ridge.

Quartzite Mountain Northwest

Location: N'/j N/2 Sec. 16andpartof Sec. 9, T. 6N.,
R. 4 W., S.B. (pro).) on the summit and upper north
slope of the peak 1 mile west of Oro Grande beacon
and 2 miles cast northeast of Oro Grande. Owner:
Riverside Division, American Cement Compan\", 621
South Hope Street, Los Angeles 17. An enormous ton-
nage of quartzite is exposed without overburden, but
it is undeveloped and not yet penetrated by roads.

Massive quartzite several hundred feet thick crops
out along the ridge crest in the trough of a northwest-
plunging syncline. The quartzite is underlain by schist
and is exposed without overburden within an area 4.000
feet long and 1,500 feet wide. In the northeastern part
of this area the quartzite of the syncline is overlapped
by another quartzite unit that forms part of a thrust
plate. The quartzite contains minor interbedded lenses
of schist and, at least on the surface, iron-stained cracks
and joints. Reserves within 100 feet of the surface are
estimated to be 36 million tons.

Quartzite Mountain Southwest

Location: S'A NE',4, NW!4 SE!4 Sec. 16, T. 6 N.,
R. 4 W., S.B. (proj.), Yz mile west of Oro Grande bea-
con and 2'/2 miles east northeast of Oro Grande.
Owner: not ascertained. The deposit is undeveloped,
inaccessible, and relatively' small.

The deposit consists of massive quartzite, probably
the equivalent of unit 5 of the type section, that crops
out near the summit of the western part of Quartzite
Mountain. The quartzite is probably about 100 feet
chick and is exposed without overburden within an
area of roughly 500,000 square feet. It lies on dolomite
and is overlain by schist, beneath which it dips at a
relatively low angle. Reserves within 50 feet of the
surfac-e are estimated to be 2 million tons.

Quartzite Mountain (upper unit)

Location: NVV'/4 NVV'/^ Sec. 15, NEU NE'/4 Sec.
1 6, T. 6 N., R. 4 W., S.B. (proj.) on the southwest slope
of Quartzite Mountain and 2!2 miles east northeast of
Oro Grande. 0\\ner: Southwestern Portland Cement
Company, 1034 AV'ilshire Boulevard, Los Angeles 17.
The deposit contains large, undeveloped reserves in
steep terrain of difficult access.

Massive quartzite, unit 7 of the type section, is ex-
posed at the surface in the troughs of two parallel
synclines that plunge northwest. The outcrop area is
roughly 2,500 feet long by 500 feet wide. The quartz-
ite is underlain 1)\- schist \\hich, in limited areas in
the western s\nclinc, has been brought to the surface
by a combination of folding and faulting. Reserves
within 100 feet of the surface are about 10 million
tons.

Quartzite Mountain (lower unit)

Location: A strip from the center to the northwest
corner of Sec. 1 5, T. 6 N., R. 4 W., S.B. (proj.) on the
summit and northeast face of Quartzite Alountain and
3 miles east northeast of Oro Grande. Owner: not as-
certained. The deposit contains a substantial tonnage

1966

QUARTZITE

.•i*J'i-Jfes ■>■ '^'i

Photo 9. Zabriskie Quortzite, Dublin Hills: View northeast of jagged outcrop of Zabriskie Quortzite
in NW '4 Sec. 35, T. 22 N., R 6 E., S.B.

of quarczite in a relatively inaccessible location and
has not been developed.

A quartzite body, unit 5 of the type section, that
averages 250 feet thick, crops out for about 4,000 feet
across the steep northeast face of Quartzite Mountain.
It dips steeply southwest into the mountain and is
overlain by a thick schist unit. Beneath it and sepa-
rated bv a thin schist unit is limestone, unit 3 of the
type section. The quartzite is relatively accessible at
the northwest end above Quarry 12 of the Southwest-
ern Portland Cement Company. Perhaps 5 million tons
of quartzite could be obtained from the outcrop with-
out excessive stripping. If it were quarried together
with the underlying limestone, perhaps a larger ton-
nage would be available.

Coxcomb Ricfge

Location: SE'/4 SE'X Sec. 10, NE'/4 NE/4 Sec. 15,
T. 6 N., R. 4 W., S.B., 3 miles east northeast of Oro
Grande. Owner: not ascertained. The area contains
an enormous mass of quartzite that is undeveloped but
readily accessible.

Massive quartzite several hundred feet thick crops
out for about 1,800 feet along the coxcomb ridge
northeast of Quartzite Mountain. It is underlain by
schist and is exposed without overburden on the entire
northwest slope of the ridge except for a small area,
where it dips beneath limestone. The deposit could be

reached easily anywhere along its northwest edge. Re-
serves are estimated to be 16 million tons within 100
feet of the surface.

Zabriskie Quartzite Near Shoshone

Previous Work

The Zabriskie Quartzite Member of the Wood
Canyon Formation (Lower Cambrian) is a homoge-
neous, persistent unit of high-purity quartzite that oc-
curs widely in the Amargosa-Death \"alley area of
Inyo County and as far west as the east face of the
Panamint Range. It is remote from industrial centers
and lias not been explored or developed commercially.

Several large bodies of the Zabriskie Quartzite oc-
cur in the vicinity of Shoshone and not far from State
Highway 127. Shoshone is about 80 miles from Dunn
Siding, the nearest railroad loading point. Zabriskie
Quartzite crops out prominently in the Dublin Hills
just west of Shoshone, on McLain Peak 10 miles south
of Shoshone, and on the west face of the Resting
Spring Range east of Shoshone.

The Zabriskie Quartzite was first described by Haz-
zard (1937, pp. 309, 310), who measured a detailed
stratigraphic section through the Paleozoic rocks ex-
posed in the Nopah and Resting Spring Ranges. The
quartzite was named after Zabriskie Station on the

California Division' of Mines and Geology

Bull. 187

Photo 10. Photomicrograph of Zobriskie Quortzite from Dublin Hills
deposit. Sample Z-I from the central part of the formation, consisting
almost entirely of quortz. Crossed nicols.

now abandoned Tonopah and Tidewater Railroad.
Using the formations defined by Hazzard, Mason
(1948) mapped an area around Tecopa and Shoshone
on a base map enlarged from the Avaw atz Mountains
60-minute quadrangle. Charles W. Chesterman of the
Division of Mines and Geology is remapping the
northeast quarter of the Shoshone L^-minute quad-
rangle.

Descripfive Geology

As shown b\- Noble and Wright ( 1954, plate 7), the
region around Shoshone contains fault block moun-
tains separated by alluviated valleys. These fault
blocks, although complicated by cross faulting and
thrust faulting, are essentially tilted homoclines made
up of later Precambrian sedimentary rocks. Paleozoic
sedimentars- rocks, or Tertiary volcanic rocks. The
Paleozoic rocks lie disconformahly on the later Pre-
cambrian rocks and arc unconformabh- overlain b\-
the Tertiary rocks.

A nearl\- unbroken secjucncc of Paleozoic rocks, al-
most 23,000 feet thick from the Lower Cambrian to
the Pcnns>'lvanian, occurs in the Nopah and Resting
Spring Ranges. These ranges consist of east-dipping
homoclines in which the beds strike at a slight angle
to the trend of the ranges. Older beds occur to the
south, and successively \ounger ones occur to the
north. The Lower Cambrian section, almost 10,000
feet thick, is heterogeneous and characterized hv the
presence of clastic sediments. The Post-Lower Cam-

brian rocks, on the other hand, consist almost entirely
of limestone and dolomite.

■Much more restricted Lower Cambrian sections oc-
cur in other fault blocks near Shoshone. In the Dub-
lin Hills, east-dipping. Lower and Middle Cambrian
formations are unconformably overlain bv Tertiary-
volcanic rocks. A faulted section of Lower Cambrian
rocks is exposed on McLain Peak.

In the section measured by Hazzard in the Resting
Spring Range, the top of the Zabriskie Quartzite
.Member lies 630 feet below the top of the Wood
Canyon Formation. The Wood Canyon Formation
is a heterogeneous sequence, 3,033 feet thick, of
quartzite, sandstone, shale, and limestone with Lower
Cambrian fossils in the upper 1,100 feet. Only the Za-
briskie .Member contains high-purit\-, vitreous quartz-
ite, and this is confined to the upper 100 feet. The
lower 60 feet is composed of sandy shale and shaly
quartzite. This in turn is underlain by gray, micaceous,
plat\- shale interbedded Mith fine-grained, bro\\n-
\\eathering sandstone. The vitreous upper part of the
Zabriskie is overlain b\- brown-weathering, plat\-
quartzite interbedded ^ith dark, greenish shale.

The Zabriskie QuartzHe in Detail

The main, high-purity part of the Zabriskie Quartz-
ite, wherever it is found, consists of massive, vitreous
quartzite that is indistinctly cross-bedded. It is tan-
nish- to pinkish-Mxathering and forms blocky talus.
The freshly broken rock is faintl>- pink to light gra\-
in color. Lender the microscope it is seen to be com-
posed of quartz grains 0.1 to 0.7 millimeters in diam-
eter, averaging perhaps 0.2 millimeters. Many of the
larger grains are rounded. .Most consist of a single
crystal, but a few are composed of aggregates of small
quartz grains that perhaps represent grains of recrvs-
tallized chalcedony or quartzite in the original sand.
The rounded grains have overgrowths of quartz \\ith
the same optical orientation as the main part. The
finer quartz grains are anhedral bur not notably inter-
locking.

Xon-quartz grains are not abundant. Sericite occurs
in the form of films 0.005 millimeters thick between
quartz grains. Small grains of tourmaline, zircon, mag-
netite, and limonite are sparse.

Dublin Hilli

Location: SW'X Sec. 35, T. 22 N., R. 6 E., S.B.,
about 2 miles \\est southwest if Shoshone. Owner:
not ascertained. The deposit is undeveloped but readily
accessible. It lies about ^4 -mile south of the improved
road leading to the Shoshone pcrlite deposit, but a
nearly level connecting road across the intervening fan
could be made comparativcl\' easily.

The quartzite forms a north-trending ridge 750 feet
long and 80 feet high that is surrounded by talus and
fan material. .Most of the ridge is underlain by quartz-
ite that strikes N. 5° W. and dips 50° NE. As shown
on figure 3, the summit of the ridge is underlain by
faintly pinkish to grayish, vitreous quartzite of high

1966

QUARTZITK

|R. 6 E
36°00' .^

NEVADA STATE LINE 32 Ml
DEATH VJkLLEY JUNC 25 /

ne-iB'

TOPOGRAPHY FROM U.S. GEOLOGICAL SURVEY

Figure 2. Mop of the Dublin Hills, Inyo County, showing location of Zobriskie Quarlzite, and Stirling Quartz-
ite. From unpublished map of northeast quarter of Shoshone ISminute quodrangle, by C. W. Chesterman.

California Division of Mines and Geology

Bull. 187

IE
LlJ

EXPLANATION

ALLUVIUM AND TALUS

ZABRISKIE QUARTZITE MEMBER

WOOD CANYON EM. UNDIFFERENTIATED
100 FEET

■■'■"'''^iisfp'

•^P^

;^^

Figure 3. Structure section through Dublin Hills Quortzite deposit, Inyo County. April 16, 1958.

C.>
,^^^

^ \* .y O <J

■C ^ -Vr <i- <?>
■?-?■ ^ '^^ ■* N.50°W.

<<^

2
<

£C
UJ

EXPLANATION

TALUS AND FLOAT

ZABRISKIE QUARTZITE MEMBER

$\^\Xv^ WOOD CANYON FM. UNDIFFERENTIATED

100 FEET

Figure 4. Structure section through McLoin Peak Quortzite deposit, Inyo County. April 16, 1958.

1966

QUARTZITE

Table S. Chemical Analyses of Quartzite from the
Dublin Hills Deposit.'
1_ 2 S__

Si02= 98.41% 99.81% 99.39%

AL-03 0.32 0.53 0.36

FeaOs 0.056 0.092 0.04

TiO-' _ - — 0.0 0.0 0.0

P2O6 Nil Nil 0.0

CaO 0.0 0.00 0.0

MgO 0.0 0.00 0.0

NasO 0.017 0.015 0.016

K2O _ _..-^ 0.086 0.272 0.081

H=0 0.11 0.28 0.11

^ .Analyses by W. H. Nisson and Lydia Lofgren, Division of Mines labo-
ratory, August 1961.
- By difference.

1 Sample Z-4, 180 feet from west end of section, figure 2.

2 Sample Z- 1 , 2 80 feet from west end of section, figure 2 .

3 Sample Z-12, 375 feet from west end of section, figure 2.

purit\-. Chemical analyses are given in Table 5. Veinlets
of opaque, white quartz with open, crystal-lined cracks
^/-i 0-inch \\ide cut the quartzite in places. Low on
the west side of the ridge, dark gray, banded quartzite
and interbedded platy brown sandstone that underlie
the high-purity quartzite are exposed. A specimen of
the dark, banded quartzite was examined with the
microscope and found to be made up of rounded to
subrounded quartz grains 0.07 to 0.7 millimeters in
diameter. Their average diameter is 0.2 to 0.3 milli-
meters. An amorphous material with low birefringence
forms films around the quartz grains and fills the inter-
stices between them.

The ridge in the southwest quarter of section 35
contains at least a million tons of quartzite, above the

wash level, that could be obtained with a minimum of
stripping. A very much larger tonnage exists in the
ridge in the northwest quarter of section 35, but it
probably would be more difficult to quarry. The Za-
briskie quartzite also crops out for more than a mile on
the relatively inacessible west face of the Dublin Hills
in sections 2, 3, and 10, T. 21 N., R. 6 E., S.B., and in
Section 26, T. 22 N., R. 6 E., S.B. (see figure 2).

Mciain Peak

Location: NW'/4 Sec. 18, T. 20 N., R. 7 E., S.B.;
about 10 air miles south of Shoshone. Owner: not ascer-
tained. The deposit is undeveloped but contains a large
tonnage of quartzite exposed without overburden.

McLain Peak is designated VABM 2688 but not
otherwise named on the Shoshone 15-minute quad-
rangle, 1951 editition. The Zabriskie Quartzite forms a
dip slope, prominent from the north, that trends north-
east from the summit. The beds in the dip slope strike
N. 40° E. and dip about 35° SE. At the northwest edge
of the dip slope, the surface drops precipitousl>' to less
resistant beds that underlie the Zabriskie Quartzite. To
the southeast, the Zabriskie beds are exposed at the sur-
face and dip nearl\' parallel to it for 300 to 500 feet.
Approximately half a mile northeast of the summit in
the direction of the strike, the Paleozoic beds pass
beneath high level fan gravel at an elevation of about
1,800 feet. Here gray, banded, pebbly quartzite that
underlies the Zabriskie crops out. At an elevation of
2,100 feet, as shown on figure 4, a stratigraphic thick-
ness of about 40 feet of slightly pink to brown, vitreous
quartzite of high purity lies on the gray quartzite.

Photo 11. View south from State High-
way 127 south of Shoshone. The smooth
slope to the left of the summit is under-
lain by the Zabriskie Quartzite.

Californfa Division of Mines and Geology

Bull. 187

/ ■' ' jiO» •< OBw^'-* 1^ Wis) ■ '

.♦,1 '

imm.
I

Photo 12. Photomicrograph of quartz rock from Sur Series, Fre-
mont Peak deposit. Quartz (low relief) oncJ dipside (high relief). Plane
polarized light.

At least 2 million tons of the Zabriskie Quartzite are
exposed on A^cLain Peak without overburden. Quarry-
ing, however, would be difficult, not onlv because of
the steepness of the slopes, but also because the deposit,
although only 1 Vi miles from the paved road to
Tecopa, would be hard to reach with a road.

9.es\\nq Spring Range

The Zabriskie Quartzite is exposed for at least .i
miles along the steep west face of the Resting Spring
Range east and southeast of Shoshone. There are two
outcrops. One is south on the Pahrump Valley road
in sections 27 and .^4, T. 22 N., R. 7 E.; the other is
north of Resting Spring in sections 13 and 24, T. 21
N., R. 7 E. At both localities the quartzite crops out
high on the mountain side and dips steeply into it.
The nearest paved roads are 2 to 4 miles away.

Quartz Rock Deposits of Gabilan Range

Quartz rock is associated \\ ith carbonate rocks of the
Sur Series near Fremont Peak in the northern part of
the Gabilan Range, about 75 miles south of the San
Francisco Bay area. The deposits are undeveloped, and
limited data indicate that the quartz rock is not of the
highest puritw It ma\', however, be useful for some
commercial purposes, particularly in view of the fact
that the deposits are of substantial size and arc rela-
tively close to centers of industry.

Descripiive Geology

In the northern part of the Gabilan Range, metasedi-
ments of the Sur Series occur as roof pendants sus-
pended in the Late Jurassic or Early Cretaceous Santa

Lucia Quartz Diorite. In an east-trending roof pendant
at Fremont Peak, the Sur Series is at least 8,000 feet
thick and consists of a sequence of quartz-mica schist,
limestone, and dolomite that dips steeply north (Bowen
and Gray, 1959). In places, bodies of carbonate rock
have been replaced to varying degrees by silica. \Vhere
the replacement is complete or nearly so, the resulting
quartz rock is a vitreous material that resembles
quartzite.

Fremonf Peak Deposit

Location: Sec. 35, T. 13 S., R. 4 E., M.D. (proj), '/i-
mile east of Fremont Peak and 6^2 miles south of San
Juan Bautista. Ownership: the deposit lies on fee land
belonging to the Reeves Ranch, and the mineral rights
arc held by the Ideal Cement Company, 620 Denver
National Bank Building, Denver 2, Colorado.

As mapped by Bowen and Gray (1959, plate 1), a
bod\- of quartz rock, having an outcrop width of 500
to 1,000 feet and 3,000 feet long, extends east from the
vicinity of the Fremont Peak State Park headquarters
buildings. Almost all of the deposit lies beyond the
limits of the park. The deposit dips steeply, and is
exposed b\- gulleys for a vertical distance of 400 feet.
Onl\- the central part of this body consists of clean
quartz rock. At the west end, where replacement of
the carbonate rock has not been complete, the body
consists of a brecciated, porous to cavernous mass of
silica with residual limestone in the form of thin lenses
and nodules as much as an inch in diameter. At the east
end it contains well over 50 percent of limestone and

Photo 13. Photomicrograph of quartz rock from Sur Series, Fre-
mont Peok deposit. Crossed nicols.

1966

QUARTZITE

dolomite. In an area near the center, estimated to be
500 feet long and 200 to 300 feet wide, replacement
has been nearly complete. There the quartz rock is a
medium to dark gray, vitreous material having a rough
surface and cut by vuglike, crystal-lined cracks. In thin
section it is seen to be composed mostly of anhedral
quartz grains with as much as 10 percent of calcium
silicate minerals and unreplaced calcite. The quartz
grains are notably non-uniform in size, ranging from
0.1 millimeter to as much as 3 millimeters in diameter.
The\' seem to be larger in areas where residual calcite
is sparse. Calcite occurs as grains 0.01 millimeter or less
in diameter within the larger quartz grains and also as
0.2 to 0.3 millimeter sized grains dispersed among
quartz grains of about the same size.

Reserves of quartz rock containing 90 percent or
more silica are estimated to be several hundred thous-
and tons.

Quartzite in ihe Hodge Volcanic Series

Quartzite from the Hodge Volcanic Series, which
occurs 10 to 15 miles southwest of Barstow, furnished
quartzite for the manufacture of silica brick during
the 1920's. The deposits, although small, contain high-
purity quartzite and are only 3 or 4 miles from a paved
highway and the combined Santa Fe and Union Pacific
main line to Los Angeles.

Descriptive Geology

The Hodge Volcanic Series, of probable Paleozoic
age, is a sequence of metavolcanic rocks that crops out
within an area of 5 or 6 square miles on the north side
of the iMojave River northwest of Hodge (Bowen,
1954, pp. 34-36). About 10,000 feet of metamorphosed
andesite, dacite, and rhyolitc flows, tuff, and tuflFaceous
sediments are exposed in a northwest-dipping homo-
cline. The lower half, which has been weakly sheared,
consists of massive, brownish and dark green rocks.
The upper half, which has been strongly sheared, con-
sists of alternating units of dark quartz-biotite schist
and white muscovite schist. Lenticular quartzite bodies
occur in the upper half. Most of them are 10 to 20 feet
thick and 200 to 300 feet long, but a few are as much
as 200 feet thick and 1,000 feet long.

Typical specimens of the high-purity quartzite con-
sist of a slightly grayish, vitreous material composed
of a fine-grained mosaic of irregular, interlocking
quartz crystals. The grains range from 0.07 to 0.25
millimeters in size, averaging about 0.2 millimeters. No
trace of original sand grains was observed with the
microscope. Non-quartz material, consisting of iron
oxide grains and fine, intergranular sericite, is very
sparse.

Some of the ({uartzite bodies may have been lenses
of sandstone or chert originally. However, the pres-
ence of crystal-lined cavities and hematite, originally
pyrite, indicate that many of them arc metamorphosed
quartz veins (Bowen, 1954, p. 35). LTnmctamorphosed
quartz veins also cut the quartzite bodies.

Photo 14. Phofomicrograph of quarzite from the Hodge Volcanic
Series, Goiconda deposit. Consists almost entirely of quartz. Crossed
nicols.

Goiconda (Emsco Canister, Leahy Ganister) quarry

Location: SW;/4 Sec. 36, T. 9 N., R. 4 W., S.B., 4
miles west of Hodge. Owner: W. E. Leahy, 4238
Edgehill Drive, Los Angeles (1954). The deposit is
about 5 miles by road from the old Victorville-Barstow
highway by way of Wild Crossing. About 1 '/4 miles
of the road is unimproved. Tucker and Sampson (1930,
p. 302) reported that about 1930, Emsco Refractories
Company produced a few hundred tons of quartzite
for silica brick from one of several quartzite lenses on
the Leahy property. There has been no recent activity.

The quartzite body that has been developed under-
lies the southern of two ridges that trend N. 65° E. in
the southwest 'A of section 36. The ridge is 300 to
400 feet long and perhaps 250 feet wide. Dark quartz-
biotite schist crops out low on the north side of the
ridge; light muscovite schist is exposed on its south
flank. The ridge contains a central layer of high-purity
quartz that is in sharp contact with brittle, opaque,
ofi^-white vein quartz mixed with quartzite on the
south and dark-weathering, vuggy quartz rock con-
taining as much as 25 percent voids on the north. The
quartzite is 20 to 25 feet wide at the west end of the
ridge but narrows to only 5 feet at the east end. Cross
cutting veins and brecciation in the central part of the
ridge indicate that the quartzite may have been cross
fractured. Reserves of high-purity quartzite probably
are not more than I 50,000 tons.

The deposit has been developed on the west end
by a quarry with a face 60 to 75 feet wide and 40 feet
high. A drift adit has been driven east just south of
the quarry in light schist beneath the south flank of
the ridge.

Kennedy (Alias Fire Brick Co. Ganiiler) quarry

Location: Near center Sec. 3 1, T. 9 N., R. 3 W., S.B.,
2 miles northwest of Hodge. Owner: John J. Ken-
nedy, Daggett (1953). The deposit is 3 miles by road

California Division of Mines and Geology

Bull. 187

^r^'^^i

:-^ >i

Photo 15. A steeply dipping quartzite body 200 to 300 feet long
and 75 to 100 feet wide was quarried for silica brick during the
1920's.

from the old V'ictorville-Barstovv highway by way of
the Hinkley cut-off. Dietrich (1928, pp. 97 and 194)
reported that in 1927 the Atlas Fire Brick Company
was mining quartzite for silica brick at the rate of
3,000 to 4,000 tons a \ear. There has been no recent
activity.

The surface expression of the quartzite bod\- is a
knoll that rises a few feet above a smooth surface cut
in metavolcanic rocks. The knoll is elliptical in plan
with its long axis roughly east and west. The quartzite
body is 200 to 300 feet long and 75 to 100 feet wide.
Most of the quartzite is light to medium gray. It has
been thoroughly shattered, and much of it is iron-
stained and has joints containing thin films of mica.
V^ein quartz is scarce. The rock that immediately en-
closes the quartzite lens is light colored schist, but
dark schist crops out southeast of the knoll. Reserves
of high-purity quartzite above the local base level arc
.small.

The principal development, a cjuarrN' at tiie w est end
of the knoll, has a crudely horseshoe-shaped face 10 to
1 5 feet high and 60 feet long that has been advanced
100 feet into the outcrop. A waste dump has been
built out from the knoll for 50 to 75 feet. A cross-cut
trench just west of the dump has exposed light colored
schist and gray quartzite on the south side of the
quartzite body. A second quarry at the east end of the
knoll has a face 25 feet long and 15 to 20 feet high.

The following is the analysis of quartzite from the
central part of the \vcst quarry face (analysis by W.

H. Nisson and Lydia Lofgren, Division of Alines
laboratory, August 1961).

SiOa' 99.44%

AUOi 0.39

FeaOa 0.056

TiOo 0.0

P0O3 0.0

CaO 0.0

AlgO 0.0

Na.O 0.002

KoO 0.04

H2O 0.07

' By difference.

Deposit in Section 29

Location: Near the common '/4 corner of Sees. 28,
29, T. 9 N., R. 3 W., S.B., 2 miles north northwest of
Hodge. Owner: not ascertained. The deposit is un-
developed and comparatively small.

An outcrop of quartzite up to 50 feet thick and
about 2000 feet long trends N. 40° E. and projects 50
feet above the general ground level. The massive,
vitreous quartzite is flanked by talus-covered slopes,
beneath which lies light colored muscovite schist. The
quartzite ranges from off-white to dark gray in color.
In places it is heavily iron-stained, and it is cut by nu-
merous quartz veins a few inches to 1 foot thick.

Some Impure Quartzites
Quarizifes of Ibe Kernville Series

Quartzites of the Kernville Series occur wideK' in
the southern part of the Sierra Nevada. So far as is
known, none of them is of high purirv, but the .Mono-
lith Portland Cement Company quarries a large ton-
nage of material that averages 85 percent SiOj for use
in the portland cement plant at .Monolith.

The Kernville Series is the name given by Miller
(1931, p. 335) to the pre-batholith metasediments
around Kernville. As much as 15,000 feet of phyllite
and schist \\ith limestone and impure quartzite of
probable Paleozoic age are exposed in the Kernville
30-minute quadrangle (Miller and Webb, 1940). The
metasediments occur as steepl\' dipping, elongated roof
pendants that trend north to northeast. One roof
pendant, along the Kern River, is more than 15 miles
long. The Kernville Series also occurs in the Brecken-
ridge Mountain 15-minute quadrangle (Dibblee and
Chcsterman, 1953), and similar metasediments that
probably belong to the Kernville Series occur around
Tehachapi.

Alonolith Portland Cement Compans- quarries im-
pure quartzite from deposits near the center of section
14, T. 32 S., R. 33 E., M.D., just northwest of the lime-
stone quarr\- and 2 miles northwest of the Portland
cement plant at Alonolith. Alicaceous, iron-stained
quartzite forms a body several hundred feet wide that
crops out for at least half a mile along the crest of a
spur just west of the limestone deposit. The quartzite
and limestone, together with a minor proportion of

1966

QUARTZITE

schist, form a north-trending roof pendant in granitic
rock. The quartzite is shattered, and it contains lenses
of schist and stringers of granitic rock and pegmatite.

The quartzite itself is a medium to dark gray,
coarsely crystalline material with abundant biotite,
plagioclase, and grains of iron oxide; and has a silica
content of from 70 to 90 percent. A specimen of the
typical material used by the Monolith plant was ex-
amined and found to consist largely of interlocking
quartz grains with very irregular boundaries. Their size
ranges from 0.07 millimeters to 3.25 millimeters and
averaged about 2 millimeters. Rectangular flakes of
biotite, mostly iron-stained, from 0.07 to 0.3 milli-
meters square are grouped in clumps up to 0.07 milli-
meters in diameter. The biotite flakes are oriented but
not concentrated in layers. Plagioclase, largely altered
to sericite, occurs as rounded grains 0.3 to 1.3 milli-
meters in diameter. Chlorite and muscovite also are
present in minor proportions.

The Monolith plant consumes roughly 100,000 tons
a year of quartzite containing 85 percent SiOo. Because
quarrying has to be to some degree selective to obtain
material of this grade, several openings with faces 70
to 75 feet high have been made along the nose of the
ridge that is underlain by the quartzite. Quarrying is
accomplished by blasting a combination of down
holes and toe holes made with wagon drills that have
tungsten carbide-insert bits. Quarry run rock is re-
duced in the main crushing plant, which is periodically
scheduled for this use.

Prospecf Mountain Quartzite

The Prospect iMountain Quartzite occurs widely in
southeastern California. As far as the writer knows, it
is impure; but the possibility that it may contain usable
bodies of high-purity quartzite should not be over-
looked. It is a well known Lower Cambrian formation
in the Great Basin, with its type locality near Pioche,
Nevada. In California it is found in the eastern part of
San Bernardino County from the Kingston Range in
the north to the Ship Mountains in the south and as
far west as the Newberry Mountains. Its relation to
the Wood Canyon Formation, the Stirling Quartzite,
and other Lower Cambrian formations of the Death
Valley country is still in doubt.

In California, a ma.ximum of about 4,000 feet of the
Prospect Mountain Quartzite are exposed within areas
of as much as 10 square miles. At many localities it
occurs at the base of a thick section of Paleozoic rocks
and lies with depositional contact on granitic and
metamorphic rocks of probable early Prccambrian
age. It is heterogeneous and in many places contains,
in addition to quartzite, shale, slate, carbonate, rock,
sandstone, and conglomerate. The quartzite parts are
likely to be thin bedded and cross bedded. Conglomer-
ate lenses composed of quartz and chert pebbles are
characteristic, especially near the base. Relatively mas-
sive sections of vitreous quartzite 50 to 100 feet thick
occur in the iMarble Mountains, in the Clark Moun-

tains, and near Toughnut Spring in the Providence
Mountains, but the quartzite contains feldspar, mica,
and iron oxide minerals.

A specimen from near Toughnut Spring, as seen in
thin section, is composed of quartz with several per-
cent of limonite and a little sericite. About 75 percent
of the quartz is in the form of a mosaic of interlocking
grains averaging 0.1 millimeter in size; the rest occurs
as well rounded grains that average 0.7 millimeters in
diameter. Much of the limonite occurs as veinlets up
to 0.7 millimeters thick. In places, discontinuous and
branching veinlets form veinlet systems as much as 10
millimeters wide.

Saragassa Quartzite

The Saragossa Quartzite occurs in a relatively small
area near Baldwin Lake, San Bernardino County (Guil-
lou, 1953) and also in the Newberry Mountains
(Gardner, 1940). From indirect evidence, its age is
thought to be Paleozoic, perhaps pre-Carboniferous.
It is feldspathic and iron-stained but has been used to a
limited extent as decorative building stone.

On Gold Mountain, northwest of Baldwin Lake,
gently dipping Saragossa Quartzite occurs in a thrust
plate and may be more than 1,000 feet thick if the sec-
tion has not been repeated by faulting. Within an area
of several square miles, the quartzite has no over-
burden or is covered only by quartzite rubble or a
thin layer of old alluvial gravel. Much of it is frac-
tured and readily breaks into rectangular blocks and
slabs 3 to 6 inches thick that are stained medium to
dark brown by limonite. Some of the quartzite is more

Imm

Photo 16. Photomicrograph of micaceous quartzite from the Kern-
ville Series near Monolith. Quartz, light; biotite, dark. Plane polarlzecJ
light.

California Division of Mines and Geology

Bull. 187

^kV'^:>-'^.'^-^-'

.t^tt>

Photo 17. Photomicrograph of Stirling Quartzite from the Dublin
Hills. Consists of rounded grains of quortz with thin films of sericite.
Plane polarized light.

massive and nearly free from iron stain, but all of it
contains several percent of feldspar and mica.

A. Coleman has produced a modest tonnage of deco-
rative building stone from outcrops in sections 6, 7,
T. 2 N., R. 2 E.; and sections 1, 12, T. 2 N., R. 1 E.,
S.B. In a report released by the Board of Building and
Safety Commissioners, City of Los Angeles, samples
were found to have a compressive strength of 36,770
pounds per square inch and a water absorption of 0.1.^
percent. The stone was approved for use as solid ma-
sonr\' and as veneer.

Photo 18. Photomicrograph of Stirling Quartzite. Some field as
Photo 17 under crossed nicols.

Sfirling Quarizife

The Lower Cambrian Stirling Quartzite, which
underlies the Wood Canyon Formation in the Death
\'alley-Amargosa \'alle\' area, is generally heteroge-
neous and impure. Its maximum reported thickness, in
the Nopah Range, is about 2,600 feet. It consists of
three members: a lower member of massive, gray
quartzite; a middle member of red, shaly, micaceous
quartzite with dolomite lenses; and an upper member
of massive, gray quartzite. The massive quartzite is an
aggregate of rounded quartz, chert, feldspar, and iron
oxide grains 0.01 -inch in diameter that have not been
completely recrystallized.

A specimen of the Stirling Quartzite from NE'/4
SWVi Section 23, T. 22 N., R. 6 E., S.B., on the north
side of the Dublin Hills (figure 2) is a non-vitreous,
pinkish to purplish gray material composed of well
rounded quartz grains 0.3 to 0.7 millimeters in diam-
eter. x\ngular quartz grains 0.05 millimeters in size fill
the interstices. Most of the large grains are surrounded
by thin films of sericite. Rounded grains of recrystal-
lized chert, plagioclase, and microcline are present in
proportion of less than 1 percent.

Vitreous Quarfzife of Eagle Mounfains, Riverside County

A great thickness of vitreous quartzite occurs in the
Eagle Mountains at the base of the sequence of meta-
sedimentary rocks that contains the Eagle iMountains
iron deposits. The largest outcrops lie 1 to 2 miles west
of the Eagle .Mountain iron mine of Kaiser Steel Cor-
poration, near the summit of the range. The age of the
quartzite has not been determined.

The metasedimentary sequence has been preserved
in a west-plunging anticlinal dome that extends east-
west for about 6 miles across the northeastern part of
the Eagle Mountains (Harder, 1912). Highly meta-
morphosed rocks that unconformably underlie the
metasedimentary sequence are exposed in the core of
the structure. Intrusive, sill-like masses of quartz mon-
zonite have invaded the structure, cutting out parts of
it and partly to completely altering carbonate units to
iron ore. The western part of the structure is nearly
intact; but toward the east, only the flanks remain
(Harder, 1912, fig. 3). The Eagle Mountain iron mine
lies near the eastern end of the north limb.

The vitreous quartzite, which occurs at the base of
the metasedimentary sequence, is most widely exposed
in the Avestern half of the structure. There its outcrop
is more than 5,000 feet wide and its thickness probably
more than 1,000 feet (Harder, 1912, pp. 31, 32). The
\itrcous quartzite is overlain by schistose, feldspathic
quartzite, which in turn is overlain by lime silicate-
rich quartzite and the carbonate rocks that contain the
iron ore deposits. The vitreous quartzite is made up
of massive beds of coarse grained, recrystallized
(luartzite that is pale gray to yellow and brown on
weathered surfaces. Limited data indicate that, al-
though feldspar and mica arc scarce, the quartzite
contains disseminated grains of iron o.xide.

1966

QUARTZITE

Photo 19. Dry pressing of fire brick. Phoia courtesy of Gladding, McBean & Co,

Quarrying and Processing

Methods

Quartzite is a relatively low priced commodity.
The price of quartzite produced in the Victorville area
is around |5.00 per ton but varies, depending on the
tonnage purchased. The freight rate is high compared
with its value. Early in 1961, the rate by rail from
Lone Pine to Los Angeles was 161^ cents per hundred
pounds.

The California quartzite operations arc relatively
small. They are primarily producers of quartzite for
specialized purposes; and, because they are far from
consuming centers, the operators have but little oppor-
tunit)^ to broaden their markets or to dispose of by-
products. Processing is simple. Quartzite is either

shipped as it comes from the quarry or crushed and
screened to specifications.

Because quartzite is very abrasive, it causes severe
wear and damage to equipment such as drill bits,
shovel teeth, and screens that are subject to abrasion.
Because quartzite is brittle, it is relatively easy to blast
and crush. Because the impurities in quartzite are likely
to be soft, bcneficiation can be effected by crushing,
screening, and the rejection of fines. Crushing machin-
ery and other sources of highly toxic silica dust arc
provided with dust collectors. Often personnel wear
dust masks to obtain additional protection.

Quartzite is quarried by standard methods. In Cali-
fornia, blast holes are made with wagon drills equipped
with tungsten carbide-insert bits. Relatively small
shovels and trucks arc used. Jaw crushers arc used if
crushing is required.

California Division of Mines and Geology

Bull. 187

Performance Data

In 1955, the Swansea quarry was producing Eureka
quartzite at an average rate of 800 tons per day
(Brooks, 1955). Equipment included two wagon drills,
using 2% -inch tungsten carbide-insert bits, that w-ere
supplied bv two compressors, each with a capacity of
600 cubic feet per minute. As a bit was worn out after
drilling 50 feet of hole, the cost of bits was 35 cents
per cubic yard of rock broken. The consumption of
explosive was 54 -pound per cubic yard. The teeth of
the No. 6 Northwest shovel used to load the broken
quartzite wore out and had to be I'eplaced after every
8 to 1 2 hours of use.

Some figures are available for a much larger opera-
tion at Rock Springs, Wisconsin (Aleschter, 1958),
which, in 1958, had a capacity- of 275 tons per hour
of quartzite railroad ballast. The quarry had a face 80
feet high. Blast holes 1 1 inches in diameter and 85 feet
deep were made by churn drilling. W'ith a bit \\eighing
650 pounds and a drill stem weighing 4,200 pounds,
drilling was at the rate of 5 to 7 feet per hour. Every
5 to 10 feet, bits had to be reforged and resharpened,
at which two men were employed full time. Blasting
was accomplished with ammonium nitrate. Seven or
eight holes were blasted together to produce 50,000
tons of broken quartzite. Secondary breaking, if re-
quired, was done with a drop ball. The broken rock
was processed with a 60 by 48-inch jaw crusher, sec-
ondary crushers, and vibrating screens to two sizes of
railroad ballast (1% by %-inch and %-inch by No.
16); the fines were discarded. The manganese steel
jaws of the primary crusher had to be rebuilt with
hardsurfacing metal after each shift. Screen plates and
cloths were replaced ever\- three weeks.

Utilization
In General

At present the uses of high-purity quartzite in Cali-
fornia are limited to the manufacture of silica brick
and Portland cement. If the fcrrosilicon and silicon
industries were to be established in this state, probably
some of the quartzite in California would be suitable
to supply them.

For silica brick, silicon, and fcrrosilicon, high-purit\'
silica in lump form is required. Both the chemical and
physical properties of the raw material are important.
A material such as silica sand, no matter how pure,
could not be used. For portland cement, however, the
suitability of a silica raw material depends mostly on
its chemical properties. Its physical form is relatively
unimportant, and the material chosen depends largely
on economic factors such as availability and cost in
terms of its SiO^ content. The use of (luartzitc by some
of the Portland cement plants in California is an ex-
ception to standard practice.

Quartzite is an unlikely source of silica that is to
be used in sand or powder sizes. Because of the rela-
tively high cost of quarrx'ing, crushing, and grinding

quartzite, and because the quartzite deposits are rela-
tively remote from transportation and markets, silica
sand ordinarily can be obtained at a lower cost. Most
users of pulverized quartz specify a high degree of
whiteness in addition to chemical purity. With the
possible exception of parts of the Eureka Quartzite,
most quartzite in California probably would not meet
the color test.

Silica Brick

Silica brick are standard and special refractory
shapes that are composed essentially of forms of silica
capable of withstanding high temperatures. Silica brick
valued at more than $42 million were produced in the
United States during 1958 (Clark and McDowell, 1960,
p. 700) and accounted for about 15 percent of the
production of refractory brick of all kinds. Silica brick
are an acid refractory; that is, they react at high tem-
peratures with basic materials such as lime, magnesia,
and alkalies. Perhaps their most useful property is the
ability to support loads at high temperatures. They
are, in addition, resistant to furnace gases, and are rela-
tively cheap. Because of the high thermal expansion
of silica, the>- are sensitive to thermal shock and sus-
ceptible to spalling. If kept above 1,200° F., however,
they perform well, because in that temperature range,
the thermal expansion of silica is small. They are espe-
cially suited for use in furnace crowns and wide-span
sprung arch roofs. By far the largest use of silica brick
is for the roofs of basic open hearth steel furnaces.
They are also used for lining parts of coke ovens, re-
verberatory furnaces, roofs of glass melting tanks, and
many other types of furnaces.

Trends in the Steel Industry

Technical changes are taking place in the steel in-
dustry that are reducing the consumption of silica
brick. Not only is the amount of silica brick used in
the construction of open hearths declining, but the
open hearth process itself ma\- be displaced.

One of the factors in increasing the efficiency of the
open hearth process has always been the need for re-
fractories that would permit higher furnace tempera-
tures. Gradually the performance of silica brick has
been imprtncd. Super duty silica brick, the highest
(]uality now available, were developed during World
War II. In laboratory tests, super duty silica brick with
a load of 50 pounds per square inch have withstood
temperatures of 3,080" to 3,090° F. before failure oc-
curred (A. P. Green Fire Brick Co., 1961). Because
the melting point of pure silica is about 3,110° F., no
great improvement in the performance of silica brick
seems possible.

For some tiiuc, basic brick made of magncsite and
chromitc have been available for the construction of
open hearth roofs that last longer and allow higher
operating temperatures than silica roofs. Until re-
cently, however, the cost of basic roofs in terms of
the pounds of refractory consumed per net ton of
steel produced has been greater than that of silica roofs.

1966

QUARTZITE

Basic roofs were first used commercially during World
War II in Europe where the difference in cost between
basic brick and silica brick was relatively small. Plant
tests of all-basic roofs began in Canada and the United
States about 1943. Since 1954 the conversion to basic
roofs has been accelerated; and by 1959, of approxi-
mately 900 open hearths in Canada and the United
States, 136 had all-basic roofs (Sommer, 1959).

The use of oxygen in steel making is likely to de-
crease the demand for silica brick still further. Basic
oxygen processes such as the L D (United States
Steel, 1957, p. 285) and Kaldo (Johansson, 1957) do
not make use of the open hearth at all. The L D
process resembles the basic Bessemer process except
that the blowing is with oxygen instead of air, and
it can treat low-phosphorus raw materials. It was
designed to use raw material charges consisting of
more than 70 percent of hot metal (crude melted iron
from the blast furnace), which cannot be treated
efficiently in the basic open hearth. The basic oxygen
converter is lined with tar-bonded dolomite-magnesite
or high lime-magnesia clinker (Harbison-Walker Re-
fractories Co., 1961).

The L D process was developed in Austria, where
scrap steel, one of the raw materials required for the
basic open hearth, was in short supply. Plants at Linz
and at Donawitz began commercial production in May
1953 (Cuscoleca, 1954). Soon after that, an L D proc-
ess plant was built in Canada (McMulkin, 1955), and
in March 1959 the Kaiser Steel Corporation installed
three L D converters at Fontana (California Magazine
of the Pacific, I960;' Chemical Week, 1959). Basic
oxygen processes have been found to be versatile and,
at least under some circumstances, less expensive to
install and operate than the basic open hearth process
(Philbrook, 1958).

Plant tests have demonstrated that the capacity of
the basic open hearth can be significantly increased by
using ()X)gen (Brion and others, 1961; Howkins and
others, 1961; Pearson, 1959). The tests were made with
furnaces having both basic and silica roofs, but basic
roofs are required to obtain the maximum increase pos-
sible. The future of the open hearth process is not yet
apparent, but it has been suggested that the open hearth
may not survive in its present form (Moore, 1961).

Silica Brick Industry in California

Three companies produce silica brick in California;
Gladding, McBean & Co. at South Gate, General Re-
fractories Conipany at Los Angeles, and Harbison-
Walker Refractories Company at Warm Springs.
Brooks (1955) has summarized the history of the silica
brick industry in California. The Atlas Fire Brick Com-
pany, in 1918, was the first to produce silica brick in
California. The quartzite was obtained from the Ken-
nedy deposit northwest of Hodge, San Bernardino
County. This operation was taken over by the F.msco
Refractories Company in 1928. At about that time,
quartzite deposits in the Quartzite Mountain area near

Photo 20. Setting silica brick in a periodic kiln. Photo courtesy of
Gladding, McBean & Co.

Oro Grande, San Bernardino County, were developed
to take the place of the small deposits near Hodge.
Gladding, McBean & Co. absorbed the Emsco Refrac-
tories Company in 1944.

The Tillotson Clay Products Company began the
manufacture of silica brick during the 1930's. This
company was purchased by General Refractories Com-
pany in 1943.

The Harbison-Walker Refractories Company bought
a plant in Warm Springs, Alameda County, that had
belonged to Laclede-Christy Company and converted
it to the manufacture of basic brick in 1952. The next
year, the company began the manufacture of super
duty silica brick at Warm Springs, using quartzite
from near Grants Pass, Oregon.

By 1953, steel makers in southern California were
using super duty silica brick from out-of-state sources
in preference to standard brick made locally of quart-
zite from the Quartzite Mountain area. Gladding, Mc-
Bean & Co., after a search that began as early as 1947
and was intensified in 1953, developed deposits of the
Eureka Quartzite near Owens Lake, from whicii super
duty brick could be made. Since 1955, all of the silica
brick produced in southern California have been made
from the Eureka Quartzite.

Method ol Production

As the first step in the manufacture of silica brick,
quartzite is ground in a dry pan and carefully sized
to produce a product consisting of angular particles
ranging in size froiu about 6 mesh (3.3 millimeters) to

California Division oi Mines and Gf.ology

Bull. 187

Photo 21. Photomicrograph of silica brick— plain light. Sharply defined, angular fragments of ganister set in moderately crystal-
lized groundmass. Overall textural appearance of the brtck is not markedly different from thot of an unflred brick.

1966

QUARTZITE

Photo 22. Photomicrograph of silica brick— crossed nicols. Field identical to Photo 21. Bright clear areas In ganister fragments
indicate residual quartz. Note degree of fracturing in quartz indicative of shattering that accompanies alpha-beta inversion within
quartz as it passes through 575° C. temperature range. Cristobalite has formed along ganister fractures and in some ganister frag-
ments cristobalite predominates. The sharp contrast in the degree of ganister conversion is probably related to different crystal struc-
ture of quartz grains within the original ganister. Tridymite is more apparent in the brick than is indicated by the photomicrograph.
Two small zones of tridymite (T) are noted in the sketch.

California Division of Mines and Geology

Bull. 187

dust. In some plants, ball mills are used to make a fine
fraction that is mixed with the product from the dry
pan. A particle size distribution is desired that results
in a minimum of voids in the tamped material. At one
of the plants in California, 15 percent of the ground
product is coarser than 10 mesh, and 65 percent is be-
tween 100 and 150 mesh.

Next, the ground quartzite is mixed with I to
3 percent of hydrated lime to form a ceramic
bond, an organic binder to provide green strength
before the bricks are burned, and enough water to
bring the mixture to the desired consistency. The
mixture is then formed into specific brick shapes with
a mechanical press. The green brick, which are very
fragile, are carefully dried under controlled conditions
to avoid cracking.

The brick are burned in a tunnel kiln or round
downdraft kiln in which the temperature is slowly and
uniformly raised to 2,700° or 2,800° F., then cooled
uniformly to room temperature over a period as long
as a month. During the burning process, the coarser
particles of quartz mostly change to tridymite and
cristobalite, high temperature forms of silica that are
metastable at room temperature. The fine quartz, com-
bining with lime, iron oxide, and impurities, forms a
molten silicate that mostly cools as a glass. The amount
of glass in modern brick varies between 10 and 20 per-
cent. At operating temperatures, the glass is molten,
while at cooler temperatures, it serves as a groundmass
that hinds the brick into a solid mass.

The Mineralogy of Silica Firebrick *

Fired silica brick is composed of two distinct frac-
tions: 1) Large ganister fragments that are mosth" con-
verted to cristobalite. 2) Fine grained groundmass con-
sisting of: a) tridymite cr\stals, b) silicate glass, c)
CaFe silicate crystals, d) opaque iron oxides. Con-
verted ganister fragments and groundmass are of ap-
proximately equal portions in normal brick; each
accounting for 30 to 50 percent of the brick volume.
Voids comprise between 15 and 30 percent of an
average brick's volume.

As silica brick generally contains more than 95 per-
cent SiO^., the service performance of the brick de-
pends to a great extent on the bcha\ior of the various
forms of silica. Silica exists in seven crystalline modifi-
cations: two forms of quartz, two of cristobalite, and
three of tridymite. The transformations that occur
within the same silica mineral type (e.g. alpha tridy-
mite to beta tridymite) take place ^\ith considerable
rapidity and are accompanied by a small energy
change. The transformations that occur between
different silica minerals (e.g. quartz-cristobalite-tridy-
mite) proceed slowly and arc accompanied by con-
siderable energy changes that result in volume expan-
sion and a corresponding decrease in specific gravity.
The technology of brick manufacture is largely con-

* This section on Mineralogy by J. Monow Elias, Geological Engineer;
Gladding, McBcan & Co.

cerned with reducing this volume of expansion to
within safe limits in the finished brick product.

Quartz. Control of brick expansion during service
is accomplished by preparing and firing the brick in a
manner that will convert all or nearly all of the quartz
to its polymorphs of cristobalite and tridymite. Meth-
ods for accomplishing a near total conversion are
multiple. It is certain that strained or flawed quartz
is more conducive to conversion than perfect crystal-
line quartz. G. R. Rigby et al (1946, p. 78) suggests
that for a given firing schedule a brick \\ith a low
quartz content is obtained by: 1) Choosing a ganister
which is finely crystalline and is associated with im-
purities. 2) Crushing the ganister to a fine size. 3)
Using the maximum allowable addition of lime. No
information was found in the available literature re-
garding the role of iron oxide in the conversion of
quartz.

The mode of the conversion of quartz to cristobalite
varies with the nature of the original rock. The first
modification that quartz undergoes during firing is
the change from alpha to beta varieties that occurs at
573°C. (964°F.). This inversion is usually accompanied
by shattering which is aggravated by large grain size
and rapid temperature change (see photos 20 and 21).
D. W. Ross (1918) warns that rapid heating through
the inversion temperature range is likely to result in
friable punk\' brick and recommends that the firing
temperature should not be allowed to exceed 1,350° C.
(2,460°F.) until a large fraction of the quartz is con-
verted. There is some question about validity of this
theory in modern brick manufacture as shattered
quartz is either healed and welded by cristobalite and
tridymite or totally converted into the high tempera-
ture minerals. It should be noted that in 1918, the year
of Ross' investigation, firing methods rarely converted
an\- of the ganister fragments to high temperature
silica minerals. The normal brick of that time had a
low cristobalite-tridymite content, and contained up
to 30 and 40 percent quartz. Alteration of quartz to
cristobalite and trid\mitc occurs within ganister frag-
ments whenever there is impure cementing material.

Cristobalite. \^ery fine crystals of cristobalite begin
to form in brick groundmass above temperatures of
870°C. (1,600°F.). At somewhat higher temperatures
conversion occurs around the pcriphcr\' of ganister
fragments and in fragment cracks that formed during
the shattering of quartz as it inverted from alpha to
beta forms. Cristobalite forms entirely at the expense
of the (]uart/. within ganister fragments as the maxi-
mum firing temperature is approached. This cris-
tobalite is often characterized by a delicate fish scale
structure. In a normal fired brick the maximum cristo-
balite content is reached at approximately the same
time in the firing schedule that quartz is disappearing.
Cristobalite is not again formed unless the temperature
exceed 1,482°C. (2,700°F.) and the brick is over-fired.
If over-firing does take place cristobalite is reformed

1966

QUARTZITE

at the expense of tridymite which is unstable above
temperatures of 1,482°C.

The author's petrographic examination supplies in-
formation that is in accord with the findings of Rigby
et al (1946, p. 77); that conversion of quartz to cris-
tobalite can and does occur in a solid state without an
intermediate melt or solution period. It is otherwise
difficult to explain how large angular shaped areas
representative of original ganister fragments can be
completely converted to cristobalite. If solution or
digestion of ganister fragments had occurred, indefi-
nite gradational zones rather than discernible bound-
aries would be expected between the original ganister
fragments and the bonding matrix.

Tridymite. Tridymite represents the end product
of the conversion of quartz in the usual temperatiux
range for silica brick manufacture. Trace amounts of
the mineral may form at temperatures below 1,090°C.
(2,000°F.), but tridymite does not constitute an im-
portant part of the brick until temperatures have
reached about 1,315°C. (2,400°F.). The mineral first
appears as small crystal grains in the brick ground-
mass, and as occasional crystals in the impure zones
of the ganister fragments. As firing continues, the
number and size of the crystals increases and con-
spicuous wedge shaped twins and laths become visible
(see photos 22 and 23).

The mode of trid\mite formation is complex. There
is petrographic evidence that suggests it forms both
from a solution state as precipitation crj'stals, and also
as a direct solid state crystallization product from
cristobalite.

Bv far the largest proportion of tridymite ft)und in
silica brick is formed through a melt or solution stage.
Tridymite formed in this manner is found in the
groundmass and digested portions of the ganister frag-
ments. The digestion zones often occur as a reaction
rim completely surrounding ganister fragments. They
are a result of progressive corrosion and digestion of
the fragment's outer surface by semi-molten ground-
mass material. Digestion probably occurs during the
high temperature soaking period of the firing cycle.
The reaction rim consists of a mixture of tridymite
and silicates of calcium, iron, aluminum, etc. Glass is
present in only minor amounts.

Crystallization of tridymite through a solid stage
is characterized by large isolated crystals randomly
oriented within ganister fragments that were con-
verted to cristobalite during an earlier period of the
firing schedule.

It is probable that tlic network of elongated tri-
dymite crystals that is formed in brick of certain
manufacture bears an important relation to the rigid-
ity of silica brick at high temperature. In the ground-
mass of sound brick, wedge and lath shaped crystals
of tridymite form a continuous network with glass
filling the interstices between tridymite crystals. Tri-
dymite that is associated with groundmass glass prob-
ably formed by a process in which the smallest ganis-

ter fragments passed into solution in the glass melt
followed by almost immediate precipitation of tridy-
mite. LeCliatelicr and Bogitch (1918, p. 15) say that
this crystallization will be accomplished the more
completely and rapidly if the quartzite used is finely
or even very finely ground. They also warn, however,
that a certain portion of large fragments is necessary
to prevent formation of cracks whose propagation
happens easily when material is uniformly fine.

Glass. The iron, aluminum, calcium, etc., oxides
that compose the impurities of quartzite, plus the
added CaO and FeO mineralizers react and combine
with some silica of the groundmass to form a molten
silicate that mostly cools as a glass. A small portion
of the silicate melt precipitates out as a crystalline
material.

The amount of glass in modern brick manufacture
varies from 10 to 20 percent. Its color ranges from
colorless to yellow to muddy-brown depending upon
the relative abundance of CaO, FeO, and the various
impurity oxides. The occurrence of glass is restricted
to the brick groundmass where it is usually found
surrounding and interstitial to tridymite crystals (see
photos 22 and 23). Occasional concentrations of semi-
pure glass occur in certain brick and are probabK-
attributable to poor mixing.

The crystalline material that is precipitated from
glass is mosth' a "solid solution" of no precise for-
mula, ranging in composition between wollastonite
(CaOSiOo) and fayalitc (2FeOSi02). These CaFe
silicates crystallize as minute grains adjacent to, or
disseminated through, the glassy areas of the brick.

It is the opinion of many research workers that the
interspersion of small amounts of CaFe silicate crys-
tals through the glass add viscosity to it and are partl\-
responsible for the absence of pronounced plastic flow
of brick at high temperatures. Reinforcement of the
glass through association with tridymite crystals (and
cristobalite) is also important in counteracting plastic
flow at elevated temperature. The combination of
these associations account for the exceptional strength
of silica brick in service regardless of the 10-20 per-
cent molten glass content wiiicli should give rise to
plastic flow and failure.

A method of estimating the glass and CaFe silicate
content of silica brick is proposed b\- Rigby et al
(1946, p. 77): "An appro.ximate idea of the glass con-
tent of a silica brick can be obtained by adding to-
gether the percentage of all oxides other than silica
and assuming tliat these flux w ith about twice their
own weight of silica, in other words the total per-
centage of fluxing oxides is trebled."

The approximate nature of this method is empha-
.sized by an interesting statement of H. M. Kraner
(1944). He claims that "lime does not increase the
amount of liquid at operating temperauires over that
provided by the normal impurities of the raw mate-
rials of the brick, but in fact reduces it, the reduction

California Division of Mines and Geology

Bull. 187

Photo 23. Photomicrograph of silica brick— plain light. Corroded and digested ganister fragments set in o well-crystallized ground-
mass. Perfect lath- and wedge-shaped crystals of tridymite are easily recognized in the groundmoss and stand out in controst to the
interstitial dark-colored gloss and CoFe silicates.

\ GANIS-

\ TER
s
\

/ \

GANIS- \

TER \

V.'

GROUNDMASS

GANIS- ,
\ TER \

.-^

GANISTER

FRAGMENT

1966

QUARTZITE

Photo 24. Photomicrograph of silica brick— crossed nicols. Field identical to Photo 23. Well-formed tridymite crystal net with inter-
stitial glass and very fine grained CoFe silicates. Rounded areas of cristobalite represent original angular fragments of ganister.
A skeleton outline showing the shape of an original ganister fragment that has undergone strong corrosion and digestion can be
traced around one of the cristobalite areas as shown in the sketch.

( :>

CRISTO-
BALITE

<!i

TRIDYMITE CRYSTALS
GLASS 8. CaFe SILICATE MATRIX

I C

CRISTOBALITE

California Division of Mixes and Geology

Bull. 187

of CaO from 2-1% resulting in 5% increase in liquid
at high temperature."

Opaque Iron Minerals. Iron oxide does not always
combine with silica to form iron silicates or CaFe sili-
cates in the brick groundmass. Where uncombined
iron does occur it takes the form of blebs, clusters,
and dendrites of opaque iron oxide minerals. The iron
minerals are generally in the form of hematite
(FeoOrO, magnetite (Fe^jOj), or a solid solution of
the two.

Uncombined iron oxides can probably be related
to either poor mixing or a too large addition of iron
oxide for "mineralizing" purposes. The effect of un-
combined iron oxide on brick service is unknown.

Specifico/fons

At one time silica brick were made from quartzite
that contained enough clay, mica, or feldspar to fur-
nish the ceramic bond. It is now known that alumina
and alkalies are critically deleterious impurities that
act as fluxes to lower the softening temperature of
silica brick, even when present in amounts of less than
1 percent. Lime, iron, and most other impurities are
less harmful. Present practice is to use the purest
quartzite that can be obtained. The amounts of alu-
mina and alkalies are limited by the specifications for
silica brick. Siiper duty silica brick has a flux factor
of 0.5 or less.*

The following is a t\pical analysis of a quartzite mix
used in the manufacture of super duty silica brick by
Gladding, McBean & Co.

SiO, - -- 96.40%

AI263 0.15

Fe.Oa 0.59

Tib:- ._..... - 0.04

CaO 2.49

MgO - 0.08

NaoO 0.12

KoO

Ignition Loss 0.02

99.89

Average chemical analysis taken .April 20, 1955 from production brick at
South Gate plant. Arthur G. Moore, WTitlen communication, March
1961.

The desirability of quartzite cannot be determined
b\' chemical means alone. Different t\pes of quartzite
invert to cristobalite and tridymite at different rates of
speed, the rate of conversion being influenced by the
size of the quartz crystals, the grading of the (juartzite
fragments, and the amount and t\pc of the fluxing
oxides. Flawed or strained quartz is more conducive
to conversion than perfect crystal grains, and a quartz-
ite that breaks readily into angular fragments will \ield
a better brick than one which disintegrates into rounded
fragments. These quartzite requirements usually are
associated with a well-metamorphosed quartz sandstone

* A.S.T.M. tentative classification C4I6-58T. Flux factor ctiuals the per
cent of alumina pi
brick has a flux factor of more than 0.5 but docs not contain more

cent of alumina plus twice the percent^ of olkalies. Standard silica
brick has a flux factor of more tha
than 1 to 1.25 percent impurities.

that has not been contaminated by igneous intrusions
or hydrothermal solutions.

Quartzite is the form of silica that is usually used
in the manufacture of silica brick. Novaculite is suit-
able and is used where it is available. Some plants use
high-purity silica sand as part of the source of the
finer sizes in the mixture of ground silica. V^ein quartz,
ho\\ever, is unsatisfactory.

Porfland Cement

The Manufacture of Portland Cement

The raw materials used in the manufacture of port-
land cement are limestone and a ^\ide variety of iron-
bearing, aluminous, and siliceous materials that may
include quartzite. They are blended in the desired
proportions, finely ground, and calcined in rotary
kilns. The kiln product, called clinker, is then proc-
essed further to produce portland cement. Kiln feeds
fall M ithin the following analysis range:

CaO 42-44%

SiOo 13-15

AI063 4-6

FcOa 2-3

CO, 33-35

Others Up to 3

Magnesia and the alkalies are deleterious. Magnesia,
perhaps the most critical, is limited to a maximum of
5 percent in the finished cement. Alkalies tend to
volatilize and pass out of the kiln, but for low alkali
cements, a maximum of 0.6 percent is tolerated.

Most portland cement plants use limestones that
have enough impurities to provide part of the alumina
and silica required in the kiln feed. The additional
alumina and silica that are required are supplied by
adding materials such as clay, schist, alluvium, or even
granite. Often the magnesia and alkali content of these
materials limits the proportions that can be used. Some
form of silica makes up part of the kiln feed if
enough silica is not present in the other ingredients.

California Plants Tfiat Use Silica

Relativcl)' few portland cement plants have to add
silica to their kiln feeds. For some plants that use
siliceous limestone, silica may be a critical ingredient
that limits the kinds and proportions of the aluminous
materials that can be used. The following table lists
the portland cement plants in California that use
silica.

Plant Silica material

Pacific Cement and

Aggregates Co.,

Davenport Sandstone

Monolith Portland Cement

Co., Monolith iMicaceous quartzite

Permancntc Cement Co.,

Cushcnl)ur\ Siliceous mine tailings

California Portland Cement

Co., Colton High-purit.\ quartzite

Riverside Cement Division,

Crestmore High-purit\ (]uartzitc

1966

QUARTZITE

Specifications

Because plant practice is so varied, the specifications
of silica for use in the manufacture of portland cement
cannot be generalized. A silica material that is suitable
for one plant is unlikely to meet the needs of another.
Plants use the cheapest material, in terms of its SiO^
content, that is available and has the desired chemical
composition. Quartzite has no intrinsic advantage over
vein quartz or silica sand. Other things being equal,
quartzite is less desirable than sand because it is abra-
sive and is relatively difficult to grind.

If the main ingredients are high in magnesia and the
alkalies, there would be very little tolerance for these
impurities in the silica.

Ferrosilicon and Silicon

Ferrosilicon is an allo\' of iron and silicon that is
usually produced from metallic iron and lump quartz-
ite or quartz in the electric furnace. The relative pro-
portions of iron and silicon can vary within a wide
range. Alloys containing 20 percent or less silicon,
called silvery pig iron by the United States Bureau of
Mines, also can be made in the blast furnace. Alloys
that contain more than 95 percent silicon, called silicon
metal, are produced in the electric furnace; but the
charge contains no iron.

Ferrosilicon is used principally as a deo.xidizing
agent in the manufacture of steel and for the addition
of silicon to alloy steel and cast iron. It also is the
reducing agent in the silicothermic or ferrosilicon
process of making magnesium metal from dolomite.
Silicon metal is used as an alloying agent in nonferrous
metallurgy and as an intermediate in the manufacture
of silicones.

Nearly pure silicon, containing only a few parts per
billion of impurities, is a very high priced material that
is used in small amounts for rectifiers, diodes, tran-
sistors, and solar cells. The starting material is metal-
lurgical grade silicon or a silicon compound such as
silicon tetrachloride. It is nor discussed further in this
report.

The Industry in California

Three plants have produced ferrosilicon or silicon
in California, but none was in operation in 1961. Dur-
ing World War I, the Noble Electric Steel Compan>'
produced ferrosilicon of 75 percent silicon content at
Heroult, Shasta County (Bradley and others, 1918, pp.
20-22). The Noble Electric Steel Company enterprise
was part of an effort to convert local mineral resources
into high priced specialty products, principally high-
quality pig iron and fcrromanganese, that could be
marketed in the east. It did not survive the return to
normal demand and prices that followed the war. The
ferrosilicon was produced in a small, 600-kilowatt fur-
nace from impure, siliceous material that probably was
obtained locall)'.

The second, and largest, of the California plants was
that of Kaiser Aluminum and Chemical Corporation
and its predecessor the Pcrmanente .Metals Corporation

at Permanente, Santa Clara County. It also operated
under the special circumstances that prevail during
times of war. From August 1942 to May 1944 it pro-
duced ferrosilicon of 75 percent silicon content for a
silicothermic magnesium plant at Manteca, San Joaquin
County, one of a number of plants built by the Federal
Government to supply the military demand for mag-
nesium during World War II. Following the war, the
Permanente plant produced some ferrosilicon of 50
percent silicon content for the Kaiser Steel Corpora-
tion at Fontana. It was operated at capacity again
from June 1951 to June 1953 during the Korean crisis,
when the Manteca plant was reactivated. Since then
the jManteca plant has been dismantled, but the Per-
manente plant has been maintained and operated from
time to time to furnish amorphous silica that is re-
covered from the furnace fume and used as a bonding
agent in the manufacture of basic refractory brick.
It has three 8,000 K\"A furnaces, each with a capacity
of 575 tons per month of ferrosilicon containing 75
percent silicon (Davis, 1954, P. 389). It consumed
vein quartz from the White Rock deposit, Mariposa
County, and quartz cobbles from the Bear River near
Colfax, Placer Count\'.

The third plant is that of Silicon Metals Division,
Ward-Lee Chemical Corporation at Dixieland, Im-
perial County, which produced silicon metal for a
few months during 1958 (F. H. Weber, Jr., Dec. 2,
1958, unpublished report). The company planned to
market silicon for alloying with aluminum in the Los
Angeles area but was unable to produce material of
acceptable grade. The plant had a single electric fur-
nace with an estimated capacity of 6': tons of silicon
per day. Quartz was obtained from deposits in San
Diego County.

Method of Production

Both ferrosilicon and silicon usuall\' are made in
three-phase electric furnaces of the arc-resistance t\pe.
Such a furnace consists of an open-topped, cylindrical
or rectangular steel shell that is lined with carbon
blocks. The charge, consisting of lump silica, charcoal
or coke, and, if ferrosilicon is being produced, shred-
ded iron or steel, is introduced through the open top.
Electric energy is applied through three vertical elec-
trodes that project into the charge. At the high tem-
perature produced b\^ the arcs between the electrodes
and by the passage of the current through the charge,
the silica is reduced by the carbon to liquid silicon that
collects in the bottom of the furnace. If the charge
contain iron, it melts and alloys -with the silicon. Peri-
odically, the furnace is tapped, and the ferrosilicon or
silicon is cast into pigs. After the pigs have cooled,
they are crushed.

Ferrosilicon and silicon furnaces range in size from
9 feet in diameter and 10 feet high to as much as 22
feet in diameter and 14 feet high. Power requirements
are from 4,000 kilo\\atts to 13,000 kilowatts or more.
The consumption of electricity, which depends on the
silicon content of the product, is lYz to 3 kilowatt-

California Division of Mines and Geology

Bull. 187

hours per pound of ferrosilicon of 50 percent silicon
content, or 5 to 6 kilowatt-hours per pound of ferro-
silicon of 75 percent silicon content (Mantell, 1940,
pp. 492, 493, 499). Voltages are in the range of 75 to
150 volts. Electrodes, which are of carbon or graphite,
are 2 to 3 feet in diameter. Current densities are 30
to 60 amperes per square inch of electrode surface.
Electrode consumption is 50 to 80 pounds per ton of
product.

Specifications

Quartzite or quartz containing 98 to 99 percent SiO^
is required for the production of ferrosilicon or sili-
con. The ferrosilicon plant at Heroult used siliceous
material containing 5 to 10 percent of iron, but in

present practice only a few tenths of a percent of iron
and alumina are tolerated. Only traces of most other
oxides are allo\\ed. Compounds of arsenic, phosphor-
ous, and sulphur are especially objectionable because
they form poisonous gases in the furnace.

Ph\sically, the silica should be a tough material that
does not crumble in the furnace. It should be crushed
to minus 3 or 4 inches, and it should contain no minus
%-inch material.

Either quartzite or quartz that meets the above spe-
cifications can be used. The California plants have used
quartz from veins, pegmatites, and deposits of quartz
cobbles because these sources were more convenient
than deposits of quartzite. Quartzite, however, is used
in otiier parts of the United States.

1966

QUARTZIIE

ANNOTATED BIBLIOGRAPHY

Allen, John Eliot, 1946, Geology of the San Juan Bautista ijuad-
ranglc, California: California Div. Mines Bull. 133, pp. 9-75
(quartzite in section through Sur Series near Gabilan School,
p. 20).

Averill, Charles V'olney, 1931, Preliminary report on economic
geology of the Shasta quadrangle: California Div. Mines Rept.
27, pp. 2-65 (quartzice-bearing metasedimcnts including Abrams
Formation, pp. 7-9) .

Averill, Charles Volney, 1937, Mineral resources of Plumas
County: California Div. Mines Rept. 33, pp. 79-143 (Grizzly
Formation, Taylorsville Formation, Shoo Fly Formation after
Dillcr 1908, pp.' 84, 85).

Barca, Richard Albert, 1966, Geology of the northern portion of
Old Dad Mountain quadrangle, San Bernardino County, Califor-
nia: California Div. .Mines and Geol. Map Sheet 7, scale 1:62,500
(Prospect Mountain Quartzite near Old Dad Mountain and Sevcn-
teenmile Point).

Batcman, Paul C, and Merriani, Charles W'., 1954, Geologic
map of the Owens Valley region, California: California Div.
Mines Bull. 170, map sheet 11 (map, scale 1:250,000, shows un-
differentiated Ordovician rocks).

Bowcn, Oliver E., Jr., 1954, Geology and mineral deposits of
Barstow quadrangle, San Bernardino County, California: Califor-
nia Div. Mines Bull. 165, pp. 7-185 (quartzite-bcaring Oro Grande
Series, pp. 23-34; quartzite in Hodge Volcanic Series, pp. 34-36;
plate 1, scale 1:125,000, shows undifferentiated Oro Grande Series
and quartzite bodies in Hodge Volcanic Series).

Bowen, Oliver E., Jr., and Gray, Cliffton H., Jr., 1959, Geology
and economic possibilities of the limestone and dolomite deposits
of the northern Gabilan Range, California: California Div. Mines
Special Rept. 56, 40 pp. (quartzite and quartz rock in Sur Series,
pp. 13, 19, shown on Plate 1, scale 1:15,840).

Bowen, Oliver E., Jr., and Ver Planck, W. E., 1965, Stratigraphy,
structure, and mineral resources in the Oro Grande Series near
Victorville, California: California Div. .Mines and Geol. Special Re-
port 84, 41 pp. (quartzite described in detail, shown on map, scale
1: 12,000).

Bradley, Walter W., and others, 1918, Manganese and chro-
mium in California: California Min. Bur. Bull. 76, pp. 20-23 (pro-
duction of fcrrosilicon and ferromanganese by Noble Electric
Steel Co.).

Brion, D. F., and others, 1961, Operating experience with open-
hearth lances: Jour. .Metals, vol. 13, pp. 300-302 (use of oxygen
in the basic open-hearth process).

Brooks, Baylor, and Roberts, Ellis, 1954 (1955), Geology of the
Jacuniba area, San Diego and Imperial Counties: California Div.
Mines Bull. 170, map sheet 23 (description of quartzite in the
Julian Schist).

Brooks, Richard F., 1955, Discovery and development of super-
duty refractory quartzite in California; unpublished paper. Am.
Iniit. Min. Met. Engr., Southern California Section, Fall Meeting.

California .Magazine of the Pacific, 1960 (March), vol. 50, no. 3,
p. 24, Kaiser Steel Corporation (production of steel by L.D.
process).

Carlson, Denton W., and Clark, William B., 1956, Lode gold
mines of the Alleghany-Downieville area. Sierra County, Cali-
fornia: California Jour. Mines and Geology, vol. 52, pp. 237-272
(geology after Ferguson and Gannett, 1932; Relief Quartzite,
p. 241, shown on pi. 8, scale 1:24,000).

Chem. Eng. News, 1955 (May 9), vol. 33, no. 19, p. 1948, From
the inferno-silicon (production of silicon from quartzite b\' Dow
Corning Co. at Midland, Michigan).

Chem. Week, 1959 (Nov. 14), vol. 85, no. 2, p. 79 (use of LD
process by Kaiser Steel Corporation).

Cbcstcrman, Charles W., 1942, Contact metamorphic rocks of
the Twin Lakes region, Fresno County, California: California Div.
.Mines Rept. 38, pp. 243-290 (quartzite, pp. 251, 252).

Chesterman, Charles W., Geologic map of the northeast quarter
of the Shoshone quadrangle (unpublished).

Clark, C. Burton, and McDowell, J. Spotts, 1960, Refractories,
in Industrial Minerals and Rocks, 3d ed., pp. 699-712, New York,
Am. Inst. Min. Met. Petroleum Engr. (production statistics of
refractories, including silica brick, p. 700).

Clark, C. W., 1921, Lower and Middle Cambrian formations
of the Mohave Desert: Univ. Calif. Dept. Geol. Sci. Bull. vol. 13,
pp. 1-7 (quartzite, called Prospect Mountain Quartzite in Haz-
zard 1954, at base of Paleozoic section in Marble Mountains).

Clark, Lorin D., 1954, Geology and mineral deposits of the
Calaveritas quadrangle, Calaveras County, California: California
Div. .Mines Special Rept. 40, 23 pp. (quartzite in the Calaveras
Formation, p. 6).

Cox, Dennis Purver, Geology of the Helena quadrangle. Trinity
County, California, Stanford University, unpublished Ph.D. thesis,
1956 (Chanchelulla Formation).

Creasey, S. C, 1946, Geology and nickel mineralization of the
Julian-Cuyamaca area, San Diego County, California: California
Div. Mines Rept. 42, pp. 15-29 (quartzite in Julian Schist, p. 18;
quartzite near Inspiration Point shown on plate 3, scale 1:9,600).

Crosby, James W., Ill, and Hoffman, Samuel R., 1951, Fluor-
spar in California: California Jour. Mines and Geology, vol. 47,
pp. 619-638 (Prospect Mountain Quartzite near Clark Mountain,
pp. 628, 629, shown on fig. 2, scale 1:54,000).

Cuscoleca, Otwin, 1954, Development of oxygen steelmaking:
Jour. Metals, vol. 6, pp. 817-827 (basic oxygen practice at Linz
and Donawitz, Austria).

Davis, Fenelon F., and Jennings, Charles W., 1954, Mines and
mineral resources of Santa Clara County, California: California
Jour. Mines and Geology, vol. 50, pp. 321-430 (ferrosilicon plant
at Permanente, p. 389).

Dibblee, T. W., Jr., 1952, Geology of the Saltdale quadrangle,
Kern County, California: California Div. .Mines Bull. 160, pp. 7-43
(quartzite in Rand Schist, p. 13; chert and quartzite, member 10 of
Garlock Scries, p. 16, shown on pi. 1, scale 1:62,500; quartz con-
glomerate in Paleozoic (?) metasedimcnts east of Redrock Can-
yon, p. 19).

Dibblee, T. W., Jr., 1954, Geology of the Redrock Canyon-
Last Chance Canyon area, Kern County: California Div. Mines
Bull. 170, Map sheet 13 (description of quartz conglomerate,
shown on map, scale 1:62,500).

Dibblee, T. W., Jr., 1960, Preliminary geologic map of the
Victorville quadrangle, California: U.S. Geol. Survey Map Sheets
.MF-226, MF-229, MF-233 (quartzite-bearing Oro Grande Series).

Dibblee, T. W., Jr., and Chesterman, Charles W., 1953, Geology
of the Breckenridge Mountain quadrangle, California, 56 pp.
(quartzite in the Kernville Series, p. 15, shown on pi. 1, scale
1:62,500).

Dietrich, Waldemar Fenn, 1928, The clay resources and ceramic
industry of California: California Div. Mines and Mining Bull.
99, 385 pp. (silica brick plant of Atlas Fire Brick Co., p. 97;
quartzite deposit (Kennedy) near Hicks, p. 194).

Diller, J. S., 1908, Geology of the Taylorsville region, California:
U. S. Geol. Survey Bull. 353, 128 pp. (quartzite in Grizzly Forma-
tion, pp. 14-16; quartzite in Taylorsville Fomiation, pp. 17-19;
quartzite in Shoo Fly Formation, p. 23).

Donnelly, Maurice, 1934, Geology and mineral deposits of the
Julian district, San Diego County, California: California Div.
Mines Rept. 30, pp. 331-370 (quartzite in Julian Schist, pp. 337,
338).

Dudley, Paul H., 1935, Geology of a portion of the Perris block,
southern California: California Div. .Mines Rept. 31, pp. 487-506

California Dimsion of jMinfs and Geology

Bull. 187

(quartzite in Elsinore Metamorphic Series, called Santa Ana For-
mation in Engel 1959, near Goodhope mine, p. 494).

Durrell, Cordell, 1940, iMetamorphism in the southern Sierra
Nevada northeast of Visalia, California: Univ. Calif. Dept. Geol.
Sci. Bull. V. 25, pp. 1-117 (Homer Quartzite, pp. 13, 32, shown
on map 1, scale 1:125,000).

Durrell, Cordell, 1943, Geology of the Sierra Nevada northeast
of Visalia, Tulare County, California: California Div. .Mines Rept.
39, pp. 153-168 (Homer Quartzite, p. 158, shown on pi. 3, scale
1:125,000).

Engel, Rene, 1959, Geology of the Lake Elsinore quadrangle,
California: California Div. Mines Bull. 146, pp. 9-58 (quartzite in
Santa Ana Formation, pp. 17-21).

Eric, John H., and others, 1955, Geolog>- and mineral deposits
of the Angels Camp and Sonora quadrangles, Calaveras and Tuol-
umne Counties, Cahfornia: California Div. .Mines Special Report
41, 55 pp. (quartzite in Calaveras Formation, p. 8).

Evans, James R., 1966, Geology and mineral deposits of Alescal
Range quadrangle: California Div. .Mines and Geology Bull, (in
press) (brown weathering, vitreous quartzite in Prospect Mountain
Quartzite).

Everhart, Donald L., 1951, Geology of the Cuyamaca Peak
quadrangle, San Diego Count>', California: California Div. .Mines
Bull. 159, pp. 51-115 (quartzite in Julian Schist, pp. 58-60).

Ferguson, Henry G., and Gannett, Roger W., 1932, Gold quartz
veins of the Alleghany district, California: U.S. Geol. Survey
Prof. Paper 172, 139 pp. (Relief Quartzite, p. 12, shown on pi. i,
scale 1:12,000).

Fiedler, William .Morris, 1944, Geology of the Jamcsburg quad-
rangle, Monterey County, California: California Div. .Mines Rept.
40, pp. 177-250 (quartzite in Sur Series, p. 182).

Gardner, Dion L., 1940, Geology of the Newberry and Ord
Mountains, San Bernardino County, California: California Div.
.Mines Rept. 36, pp. 257-292 (quartzite in earlier Precambrian met-
asediments. Prospect Mountain Quartzite, Saragossa Quartzite, pp.
262-266, shown on pi. 2, scale 1:250,000).

Gay, Thomas E., Jr., Geology of Upper CofTee Creek, Etna
quadrangle, California, University of California, Berkeley, unpub-
lished .M.A. thesis, 1949.

Gay, Thomas E., Jr., and Wright, Lauren A., 1954 (1955),
Geology of the Talc Cir>- area, Inyo County: California Div.
Mines Bull. 170, map sheet 12 (description of Eureka Quartzite,
shown on map, scale 1:24,000).

Goldman, Harold B., 1957, Stone, dimension: California Div.
Mines Bull. 176, pp. 591-606 (Red Rose quartzite deposit, p. 602).

Greife, J. L., and others, 1959, Geology of the .Mazourka Can-
yon area. Independence quadrangle, Inyo County, California:
Geol. Soc. America Bull. vol. 70, pp. 1722, 1723 (abstract; includes
undifferentiated Eureka Group consisting of interbcdded quartz-
ite, limestone, dolomite).

A. P. Green Fire Brick Co., 1961 (Jan.), Silica refractories:
Brick & Clay Record, vol. 138, no. 1, pp. 71, 106-109 (properties
and uses of silica brick).

Grose, L. Trowbridge, 1959, Structure and petrology of the
northeast part of the Soda Mountains, San Bernardino County,
California: Geol. Soc. America Hull. vol. 70, pp. 1509-1548 (Pros-
pect Mountain Quartzite, pp. 1516, 1517, .shown on plate 1, scale
1:31,680).

Grout, Frank F., 1932, Pctrograph>- and petrology. New York,
.McGraw-Hill, 522 pp. (quartzite, pp. 366-368).

Guillou, Robert B., 1953, Geology of the Johnston Grade area,
San Bernardino County, California: Califomia Div. Mines Special
Rept. 31, 18 pp. (Saragossa Quartzite, quartzitc-bearing Chicopec
Formation, pp. 7-10, shown on pi. 1, scale 1:24,000).

Hall, Wayne E., and .MacKevctt, E. .M., 1958, Economic geology
of the Darwin quadrangle, Inyo County, California: California
Div. Mines Special Rept. 51, 73 pp. (Eureka Quartzite in Talc
City Hills, p. 7, shown on pi. 2, scale 1:21,000).

Harbison-Walker Refractories Co., 1961 (Jan.), Basic refrac-
tories: Brick & Clay Record, vol. 138, no. 1, pp. 70, 71, 96 (uses
of basic refractories; refractories for the basic oxygen steel proc-
ess).

Hadle\-, Jarvis B., 1948, Iron ore deposits in the eastern part of
the Eagle .Mountains, Riverside County, California; Cahfornia Div.
Mines Bull. 129, pp. 3-24 (vitreous quartzite, pp. 4. 5, shown on
pi. 2, scale 1:2,400).

Hamilton, Warren B., 1956, Geology of the Huntington Lake
area, Fresno County, California: Califomia Div. .Mines Special
Rept. 46, 25 pp. (quartzite, p. 7, shown on pi. 1, scale 1:63,360).

Harder, E. C, 1912, Iron-ore deposits of the Eagle .Mountains,
California: U. S. Geol. Survey Bull. 503, 81 pp. (vitreous quartzite,
pp. 30-35, shown on pi. 1, scale 1:12,000, fig. 3, scale approx.
1:62,500).

Hart, Earl W., 1959, Geology of limestone and dolomite in the
southern half of the Standard quadrangle, Tuolumne County,
California: California Div. Mines Special Rept. 58, 25 pp. (quartz-
ite and metachert in the Calaveras Group, p. 12, shown on pi ">
scale 1:9800).

Hazzard, John C, 1933, Notes on the Cambrian rocks of the
eastern Alojave Desert, California: Univ. Calif. Dept. Geol. Sci.
Bull. vol. 23, pp. 57-80 (quartzite, called Prospect Mountain
Quartzite in Hazzard 1954, in Alarble .Mountains, Providence
.Mountains, Ship Mountains).

Hazzard, John C, 1937a, Paleozoic section in the Nopah and
Resting Springs .Mountains: California Div. Alines Rept. 33, pp.
273-339 (Stiriing Quartzite, p. 306, Zabriskie Quartzite, p. 309,
Eureka Quartzite, pp. 324, 325; columnar section, fig. 3).

Hazzard, John C, 1937b, Paleozoic in the Providence Alountains,
San Bernardino County, Califomia: Geol. Soc. America Bull.
Proc, pp. 240, 241 (abstract; Lower Cambrian Toughnut Quartz-
ite, renamed Prospect Mountain Quartzite in Hazzard 1954).

Hazzard, John C, 1954 (1955), Rocks and structures of the
northern Providence Alountains, San Bernardino County, Cali-
fornia: California Div. Alines Bull. 170, chap. 4, contr. 4, pp. 27-35
(Prospect Alountain Quartzite, table 1, pi. 2, scale 1:31,680).

Heinrich, E. William, 1956, Alicroscopic petrography. New
York, AIcGraw-Hill, 296 pp. (quartzite, pp. 206-209).

Henshaw, Paul C, 1942, Geolog>' and mineral deposits of the
Cargo Aluchacho Alountains, Imperial County, Califomia: Cali-
fornia Div. Alines Rept. 38, pp. 147-196 (Vitrefrax Formation,
pp. 153, 154, shown on pi. 2, scale 1:48,000).

Hershey, Oscar H., 1901, Aletamorphic formations of north-
western California: Am. Geologist, vol. 27, pp. 225-245 (quartzite
in Abrams Formation, p. 226).

Hewett, D. F., 1956, Geology and mineral resources of the
Ivanpah quadrangle, California and Nevada: U. S. Geol. Survey
Prof. Paper 275, 172 pp. (Prospect Alountain Quartzite in Ivanpah
.Mountains, Clark Alountains, Kingston Range, Old Dad Moun-
tains, pp. 29-31, shown on pi. 1, scale 1:125,000).

Hinds, Norman E. A., 1932, Paleozoic eruptive rocks of the
southern Klamath Alountains, California: Univ. Calif. Dept. Geol.
Sci. Bull. vol. 20, pp. 375-410 (ChancheluUa Formation, pp. 392,
393).

Hinds, Norman E. A., 1933, Geologic formations of the Red-
ding- Weavcrville districts, northern California: California Div.
.Mines Rept. 29, pp. 76-122 (quartzite in .\brams Formation, p. 81;
ChancheluUa Formation, p. 85, shown on pi. 3, scale 1:250,000).

Hopper, R. H., 1947, Geologic section from the Sierra Nevada
to Death V^alley, Cahfornia: Geol. Soc. .\mcrica Bull. vol. 58,
pp. 393-432 (Zabriskie Quanzite, p. 406; Eureka Quartzite, p. 407;
both shown on pi. 1, scale 1:220,000).

Hoppin, Richard A., 1954, Geology of the Palen Alountains
gypsum deposit. Riverside Count\-, California: California Div.
Alines Special Rept. 36, 25 pp. (quartzite in Alaria Formation,
p. 14, shown on pi. 1, scale 1:9600).

Howkins, J. E., and others, 1961, .Analysis of open-hearth oxygen
injection: J<iur. Metals, vol. 13, pp. 292-297.

1966

QUARTZITE

Hulin, Carlton D., 1925, Geology and ore deposits of the Rands-
burg quadrangle, California: California Min. Bur. Bull. 95, 152 pp.
(quanzite in the Rand Schist, p. 25).

Irivin, William P., 1960, Geologic reconnaissance of the northern
Coast Ranges and Klamath Mountains, California, with a summary
of mineral resources: California Div. Mines Bull. 179, 80 pp.,
(quartzite in Abrams Formation, pp. 18, 19; Chanchclulla Forma-
tion, p. 21; quartzitc-bcaring metasedimcnts, p. 24).

Jahn,s, Richard H., and Muehlbergcr, William R., 1954 (1955),
Geology of the Soledad basin, Los Angeles County: California
Div. Mines Bull. 170, map sheet 6 (description of quartzite in
Pelona Schist, shown on map, scale 1:84,000).

Jahns, Richard H., and Wright, Lauren A., 1951, Gem-and-
lithium-bearing pegmatites of the Pala district, San Diego County,
California: California Div. Mines Special Rept. 7A, 72 pp. (quartz-
ite-bearing metasedimcnts, p. 9).

Jeffrey, J. A., and Woodhouse, C. D., 1931, Note on a deposit
of andalusite in California; its occurrence and technical import-
ance: California Div. Mines Rept. 27, pp. 459-464 (quartzite near
White Mountains andalusite deposit, p. 460).

Jennings, Charles W., 1958, Death Valley sheet: California Div.
Mines Geologic Map of California, scale 1:250,000 (undivided
Ordovician rocks, including Eureka Quartzite, in Owens Valley
and Nopah Range; undivided Cambrian rocks, including Zabriskie
Quartzite, in Nopah and Resting Spring Ranges).

Johansson, Folke, 1957, Swedish oxygen steelmaking: Jour.
Metals, vol. 9, pp. 972-975 (Kal-Do process).

Kraner, H. M., 1944, Determining the quality of silica brick:
Natl. Open Hearth Conference, A.LM.E., Proc. vol. 27, pp. 30}-
309.

Krauskopf, Konrad B., 1953, Tungsten deposits of Madera,
Fresno, and Tulare Counties, California: California Div. Mines
Special Rept. 35, 83 pp. (quartzite, p. 5, shown on pi. 1, scale
1:125,000).

Kupfer, Donald H., 1954 (1955), Geology of the Silurian Hills,
San Bernardino County: California Div. Mines Bull. 170, map
sheet 19 (description of quartzite in Pahrump Series, shown on
map, scale 1:36,000).

Laniey, Carl A., 1948a, Old Dad Mountain iron-ore deposit, San
Bernardino County, California: California Div. Mines Bull. 129,
pp. 59-68 (quartzite, called Prospect Mountain Quartzite in Hew-
ett, 1956, pp. 62, 63, shown on fig. 21, scale 1:4000).

Lamey, Carl A., 1948b, Iron Hat (Ironclad) iron-ore deposits,
San Bernardino Count>', California: California Div. Mines Bull.
129, pp. 97-109 (quartzite, called Prospect Mountain Quartzite in
Hazzard, 1954, in Marble Mountains, p. 103, shown on pi. 10,
scale 1:6000).

Langenheim, R. L., Jr., and others, 1956, Middle and Upper (?)
Ordovician rocks of Independence quadrangle, California: Am.
Assoc. Petroleum Geologists Bull. vol. 40, pp. 2081-2097 (quartzite
in undifferentiated upper part of Eureka Group, pp. 2092, 2093).

Larsen, Esper S., Jr., 1948, Batholith and associated rocks of
Corona, Elsinore, and San Luis Rev quadrangles, southern Califor-
nia: Geol. Soc. .America Mem. 29, 182 pp. (Paleozoic quartzites,
p. 17; quartzite in Bedford Canyon Formation, p. 19).

Larsen, Esper S., Jr., 1951, Crystalline rocks of the Corona,
Elsinore, and San Luis Rey quadrangles, southern California;
California Div. Mines Bull. 159, pp. 7-50 (Paleozoic schists and
quartzites, Bedford Canyon Formation, p. 14 — condensed from
Larsen 1948).

Le Chatelier H., and Bogitch, B., 1918, Sur les proprictcs rcfrac-
taires de la silica: British Ccrani. Soc. Trans, vol. 17, p. 15.

Lindgren, Waldemar, 1900, Colfax folio, California: U. S. Geol.
Survey Geol. Atlas of the U.S., folio 66 (Relief Quartzite, p. 2,
shown on map, scale 1:62,500).

Lydon, Philip A., and others, 1960, W'cstwood sheet: Cali-
fornia Div. Mines Geologic .Map of California, scale 1:250,000
(undivided Paleozoic rocks, including Shoo Fly Formation, Griz-

zly Formation; undivided Silurian rocks, including Taylorsville
Formation).

Macdonald, G. A., 1941, Geology of the western Sierra Nevada
between the Kings and San Joaquin Rivers, California: Univ. Calif.
Dept. Geol. Sci. Bull. vol. 26, pp. 215-273 (quartzite. p. 220).

MacKevett, Fdward M., 1951, Geology of the Jurupa (Moun-
tains, San Bernardino and Riverside Counties, California: Cali-
fornia Div. Mines Special Report 5, 14 pp. (quartzite in Jurupa
Series, p. 6).

Mantell, C. L., 1940, Industrial electrochemistry, 2d cd.. New
York, McGraw-Hill, 656 pp. (ferrosilicon, p. 492; silicon, p. 493;
table showing raw materials, furnace type, operating details for
ferroalloys, p. 499).

Mason, J. F., 1948, Geology of the Tecopa area, southeastern
California: Geol. Soc. America Bull. vol. 59, pp. 332-352 (Zabris-
kie Quartzite, Stirling Quartzite, table 1, pp. 336-341; pi. 2, scale
1:62,500, shows undifferentiated Wood Canyon Formation, Stirling
Quartzite).

McAllister, James F., 1952, Rocks and structures of the Quartz
Spring area, northern Panamint Range, California: California Div.
Mines Special Rept. 25, 38 pp. (Eureka Quartzite, pp. 12, 13,
shown on pi. 1, scale 1:31,680).

McAllister, James F., 1955, Geology of mineral deposits in the
Ubehebe Peak quadrangle, Inyo County, California: California
Div. Mines Special Rept. 42, 63 pp. (Eureka Quartzite, p. 11).

.McMulkin, F. J.. 1955, Oxygen steel produced at Dofasco can
compete with open hearth: Jour. Metals, vol. 7, pp. 530-534 (plant
of Dominion Foundries and Steel Ltd., Canada).

Melhase, John, 1925, Andalusite in California: Eng. Min. Jour. —
Press, vol. 120, pp. 91-94 (quartz, called quartzite in Wright, 1957,
near White Mountains andalusite deposit, p. 92).

Merriam, Charles W., and Smith, Ward C, Geologic map of
the New York Butte quadrangle, California, scale 1:62,500, U. S.
Geol. Survey, unpublished, 1951.

Merriam, Richard, 1946, Igneous and metamorphic rocks of the
southwestern part of the Ramona quadrangle, San Diego County,
California: Geol. Soc. America Bull. vol. 57, pp. 223-260 (quartz-
ite in Julian Schist, pp. 227, 228).

Merriam, Richard, 1958, Geology of Santa Ysabcl quadrangle,
San Diego County, California: California Div. Mines Bull. 177,
pp. 7-20 (quartzite in Julian Schist, p. 9).

Meschter, Elwood, 1958 (Nov.), Quartzite tough and expensive
but hard to beat for railroad ballast: Rock Products, vol. 61,
no. 11, pp. 78-81, 135, 136 (quartzite quarry at Rock Springs,
Wisconsin).

Miller, William J., 1931, Geologic sections across the Sierra
Nevada: Univ. Calif. Dept. Geol. Sci. Bull. vol. 20, pp. 331-360
(Kernville Series, p. 335).

Miller, William J., 1935, A geologic section across the southern
Peninsular Range of California: California Div. Mines Rept. 31,
pp. 115-142 (quartzite in Julian Schist near Jacumba, p. 120).

Miller, William J., 1944, Geology of the Palm Springs-Blythe
strip. Riverside County, California: California Div. Mines Rept.
40, pp. 11-72 (quartzite in Palm Canyon complex, p. 22; quartzite
in .Maria Formation, p. 26; quartzite in Eagle Mountains, p. 31).

Miller, William J., and Webb, Robert W., 1940, Descriptive
geology of the Kernville quadrangle, California: California Div.
Mines Rept. 36, pp. 343-378 (quartzite in Kernville Series, pp.
349-353, shown on pi. 2, scale 1:125,000).

Moore, A. K., 1961, Future of the open hearth: Jour. Metals,
vol. 13, pp. 303-304.

Noble, Levi F., and Wright, Lauren A., 1954 (1955), Geology
of the central and southern Death Valley region, California: Cali-
fornia Div. Mines Bull. 170, chap. 2, contr. 10, pp. 143-160.

Norman, L. A., Jr., and Stewart, Richard M., 1951, Mines and
mineral resources of Inyo County, California: California Jour.

California Division of Mines and Gf.ology

Bull. 187

Mines and Geology vol. 47. pp. 17-223 (Lakeview talc deposit,
p. 118).

Oakcshott, Gordon B., 1937, Geology and mineral deposits ot
the western San Gabriel Mountains, Los Angeles County, Cali-
fornia: California Div. .Mines Rept. 33, pp. 215-249 (quartzite in
Placerita Formation, p. 222).

Oakeshott, Gordon B., 1958, Geology and mineral deposits of
San Fernando quadrangle, Los Angeles County, California: Cali-
fornia Div. .Mines Bull. 172, 147 pp. (quartzite in Pelona Schist,
pp. 49, 50; quartzite in Placerita Formation, pp. 50, 51).

Page, Ben M., 1951, Talc deposits of steatite grade, Inyo Countv',
California: California Div. Mines Special Rept. 8, 35 pp. (silica
rock, called quartzite in Hall 1958, in Talc City Hills, p. 8, shown
on fig. 5, scale 1:14,000 and larger scale maps).

Patchick, Paul F., Economic geology of the Bullion mining dis-
trict, San Bernardino County, California, University of Southern
California, unpublished M.A. thesis, 1959 (Prospect .Mountain
Quartzite, Ivanpah Mountains).

Pearson, Oscar, 1959 (May 7), New open-hearth practice links
oxygen, sprung basic roof: Iron Age, vol. 183, no. 19, pp. 98-100.

Philbrook, W. O., 1958, Thermochemistry of oxygen steel: Jour.
.Metals, vol. 10, pp. 477-482.

Prout, John \\'.. Jr., 1940, Geology of the Big Blue group of
mines, Kernville, California: California Div. .Mines Rept. 36, pp.
379-421 (quartzite in Kernville Series, p. 391).

Reiche, Parry, 1936, Geology of the Lucia quadrangle, Cali-
fornia: Univ. Calif. Dept. Geol. Sci. Bull. vol. 24, pp. 115-168
(quartzites, pp. 118-121).

Richmond, James Frank, 1960, Geology of the San Bernardino
Mountains north of Big Bear Lake, California: California Div.
.Mines Special Rept. 65, 68 pp. (Chicopee Canyon Formation.
pp. 11-15; quartzite in Furnace Formation, p. 16; both shown on
pi. 1, scale 1:31,680).

Rigby, G. R., White, R. P., Booth, H., and Green, A. T., 1946,
An investigation into the properties of silica bricks: British Ceram.
Soc. Trans, vol. 45, pp. 69-105.

Rock Products, 1957 (March), vol. 60, no. 3, pp. 76-79, From
rock to silicon (quartzite quarry at Clifton Forge, Virginia; manu-
facture of silicon and silicones by Union Carbide and Carbon
Corp.) .

Ross, Donald C, 1958, Igneous and metamorphic rocks of parts
of Sequoia and Kings Canyon National Parks, California: Cali-
fornia Div. .Mines Special Rept. 53, 24 pp. (quartzite near Hospi-
tal Rock, p. 5, shown on pi. 1, scale 1:62,500).

Ross, D. W., 1918, Silica refractories: .\m. Ceram. Soc. Jour.,
vol. I, pp. 447-501.

Silbcrling, N. J., Schoellhamer, J. E., Gray, Clifton H., Jr., and
Imlay, R. W., 1961, Upper Jurrasic fossils from Bedford Canyon
Formation, Southern California: Am. Assoc. Petroleum Geologists
Bull. vol. 45, pp. 1746-1748.

Simpson, Edward C, 1934, Geology and mineral resources of the
Elizabeth Lake quadrangle, California: California Div. Mines
Rept. 30, pp. 371-415 (quartzite in Pelona Schist, p. 380).

Sommer, A. H., 1959, Basic construction in the open-heanh:
Jour. .Metals, vol. II, pp. 623-627.

Troxcl, Bennie W., 1954 (1955), Geology of a part of the
Shadow .Mountains, western San Bernardino County: California
Div. Mines Bull. 170, map sheet 15 (description of quartzite in
Oro Grande Scries, shown on map, scale 1:20,850).

Tucker, VV. Burling, 1926, Imperial County: California Min.
Bur. Rept. 22, pp. 248-285 (quartzite in Coyote Mountains shown
on map facing p. 276, scale 1:31,680).

Tucker, W. Burling, and Sampson, Reid J., 1930, San Bernar-
dino Count)': California Div. Mines Rept. 26, pp. 202-325 (quartz-
ite quarries of Fmsco Refractories Co., Kennedy quarry, pp. 302,
303).

Tucker, W. Burling, and Sampson, Reid J., 1943, .Mineral re-
sources of San Bernardino County: California Div. .Mines Rept.
39, pp. 247-249 (Emsco quarry, p. 542).

United States Steel Corp., 1957, The making, shaping, and treat-
ing of steel, 7th ed.. United States Steel Corp., Pittsburgh. Penna..
1048 pp. (LD process of making steel, p. 285).

Vaughan, F. E., 1922, Geology of the San Bernardino .Mountains
north of San Gorgonio Pass: Univ. Calif. Dept. Geol. Sci. Bull,
vol. 13, pp. 319-411 (Saragossa Quarrzite near Baldwin Lake,
p. 357).

Ver Planck, William E., 1952, Gypsum in California: California
Div. Mines Bull. 163, 151 pp. (quartzite in Maria Formation, Little
.Maria Mountains, p. 16, shown on pi. 2, scale 1:12,000).

Wallace, Robert E., 1949, Structure of a portion of the San
.Andreas rift in southern California: Geol. Soc. America Bull,
vol. 60, pp. 781-806 (quartzite in Pelona Schist, Portal Ridge,
p. 786).

Weber, F. Harold, Jr., 1958 (Dec. 2), California Div. .Mines
unpublished report (silicon plant of Silicon Metals Div., Ward-
Lee Chemical Corp., at Dixieland, Imperial County, California).

Wells, Francis G.. and others, 1949, Chromite deposits near
Seiad and McGufTy Creeks, Siskiyou County, California: U.S.
Geol. Survey Bull. 948-B, pp. 19-62 (quartzite in schist, called
.\brams Formation in Irwin I960, p. 23).

Wiese, John H., 1950, Geology and mineral resources of the
Neenach quadrangle, California: California Div. Mines Bull. 153,
53 pp. (quartzite in Pelona Schist, pp. 12-15; quartzite in Paleozoic
(?) metasediments, pp. 16-18).

Williams, Howel, 1949, Geology of the .Macdoel quadrangle,
California: California Div. .Mines Bull. 151, pp. 7-60 (quartzite
at Yellow Butte, p. 14; quartzite in metasediments near Yreka,
pp. 14, 15).

Wright, Lauren A., 1952, Geology of the Superior talc area.
Death Valley, California: California Div. .Mines Special Rept. 20,
22 pp. (quartzite in Pahrump Series, pp. 9-15, shown on pi. I,
scale 1:4800).

Wright, Lauren A., 1954a, Geology of the Silver Lake talc
deposits, San Bernardino County, California: California Div. Mines
Special Rept. 38, 30 pp. (quartzite in Earlier Precambrian meta-
sediments, pp. 9, 27, shown on pi. 1, scale 1:1800).

Wright, Lauren A., 1954b, Geology of the Alexander Hills area,
Inyo and San Bernardino Counties: California Div. .Mines Bull.
170. map sheet 17 (description of quartzite in Pahrump Scries,
.Stirling Quartzite, shown on map, scale 1:31,680).

Wright, Lauren \., 1957, Kyanitc, andalusite, and related min-
erals: California Div. .Mines Bull. 176, pp. 275-280 (quartzite in
White .Mountains andalusite area, p. 276, shown on cross-section,
fig. 3; quartzite in \'irrcfrax Formation, Cargo .Muchacho Moun-
tains, pp. 276, 277).

Wright, Lauren A., and others, 1953, .Mines and mineral de-
posits of San Bernardino County, California: California Jour.
Mines and Geology, vol. 49, pp. 49-259 (Atlas quarry, p. 196,
tab. list p. 166, quartzite in Earlier Precambrian metasediments
near Yucca Grove, pp. 202, 216; Emsco quarr>", tab. list p. 166;
Golconda quarr>-, tab. list p. 166; Kennedy quarry, tab. list p. 167).

Wright, Lawrence B., 1946, Geology of Santa Rosa .Mountain
area. Riverside County, California: California Div. .Mines Rept.
42, pp. 9-13 (quartzite in Paleozoic (?) metasediments, p. II,
shown on pi. 1, scale 1:30,000).

LIST OF

QUARTZITE DEPOSITS IN CALIFORNIA

1966

QUARTZITE

BASIN-RANGES

Map
No.

Formation (group)
Locality

Site

Geology

Rtmarks and rtfartncti

TfiassicC?) or PdieozoicC?)
Qudrtz conslomerate
El Paso Mtns.

Pre-Mesozoic
Quartzite
While Mms.
site area

indd

Permian

Quartzite in
Series
El Paso Mtns

Garlock

Middle Ordovician
Eureka Quartzite
Lakeview

Mazourka Canyon

Nopah Ranse

Quartz Spring area

Swansea

Talc City Hills

Trail Canyon

Ubehebe Peak area

Lower Cambrian

Zabriskie Quartzite
(member Wood
Canyon fm.)
Aguereberry Point

Sec. 36, T. 29 S., R. 37
E., Sec. 1, T. 30 S.,
R.37E.,MD.,dpprox.
1 mi. E. of Redrock
Canyon in El Paso
Mtns.

Sec. 13, T. 3 S., R. 33
E., MD., 18 mi. N. of
Bishop on west face
of White Mtns.

Mostly Sec. 32, T. 28
S., R. 39 E., Sec. 4,
T. 29 S., R. 39 E.,
MD., in NE. pari El
Paso Mtns.

Sec. 4, T. 16 S., R. 37
E., MD., on lower
slope of Inyo Mtns.,
6mi.SE. of Lone Pine.

West edge T. 12 S., R.
36 E., MD. (proj.),
east side of Mazourka
Canyon, NE. of Inde-
pendence.

N. part T. 23 N., R. 8
E., SB. (proj.), on
west slope near north
end of range-

In and near T. 14 S., R.
41 E., MD. (proj) in
Andy Hills, Last
Chance foothills, south
Rank of Whitetop
Mtn.

SE. cor. Sec. 24, NE.
cor. Sec. 25, T. 16 S.,
R. 37 E., MD., at end
of spur of Inyo Mtns.
just south of Swansea.

T. 18 S., R. 39 E., MD.
(proj.) NE. of White
Swan mine in NW.
part of TalcCity Hills.

T. 18 S., R. 46 E., MD.
(proj.), east face Pan-
amint Range near Trail
Canyon.

T. 14 S., R. 40E.,MD.,
(proj.), 2Vq mi. N. of
Ubehcbc Peak on W.
side Racetrack Valley.

Center of E. edge T. 15
S., R. 45 E., MD.
(proj.) at Augereberry
Point on E. face or
Panamint Range.

Lenticular masses up to
800 ft. thick in meta-
morphic rocks crop-
ping out within 1
square mi. area.

Associated with hornfelsj rounded, flattened quartz
pebbles up to 2 in. long in matrix of dark gray quartzite.

Elongate bodies of Quartzite associated with schist and mctaporphyry; anda-

quartzite several hun-
dred to 1,200 ft.
wide.

Steeply dipping quartz-
ite member 700 ft.
thick with outcrop
2-3 mi. long-

Outcrop 370 ft. wide,
at least Vq mi. long/
dip75''-85'SW.

Quartzite tongues 5-30
ft. thick in Ordovician
rocks that crop out for
5 miles and dip 60*-
80" W.

Outcrop 100-265 ft.
thick, 3 to 4 miles
long; dip 20*-30"
NE.

400 ft- thick, incl. 250
ft. of vitreous quartz-
ite. Total outcrop
length, 2 to 3 miles.

Outcrop 300 ft. wide,
3.000 ft. long, com-
plexly faulted. Steep
dipNE.

440 ft. max. thickness
exposed in NW.-
trending fault slices.
Total outcrop length
several thousand ft.

250 ft. thick.

400 ft. thick; outcrop
several thousand ft.
long.

70 ft. thick, E. dip. Out-
crops for at least 5 mi.
along the mtn. front.

lusitc within or marginal to the quartzite bodies. Lithol
ogy: Light-colored. Weathered surface iron-stained
from included pyrite. In thin section: holocrystalline
with typical hypidiomorphic texture. Principal mineral
is quartz. Feldspar occurs sparingly. Zircon is accessory.

Member 10 of Dibblee (52). Lies on thin-bedded, hard,
gray to brown shale of member 9. Overlain by thin-
bedded tan to brown shale and chert of member 11.
Lithology of the quartzite: Tan, thick-bedded to massive,
very fine grained quartzite with interbeds of chert and
minor interbeds of shale.

Lies on gray dolomite of Pogonip Limestone with possible
bedding plane fault at base. Overlain by dark nodular
Ely Springs Dolomite. Contains basic dikes. Lower part
is platy, iron-stained, and impure. Upper part is massive,
vitreous, high-purity quartzite. Lithology of upper part:
blocky, brown-weathering, outcrops covered with
talus blocks. In hand specimen: light gray, vitreous
quartzite with sparse specks of limonite. In thin section:
mostly anhedral, interlocking quartz grains with small
amount of fine mica and opaque matter. Typical analysis:
Si02, 99.66%; AhQj, 0.16; FesOj, 0.00; TiOj,
0-00; PiOe, 0.00; CaO, 0.00, MgO, 0.00; NaiO,
0.02; KzO, 0-02; H^O, 0.14.

Eureka Group of Langenheim lies on Mazourka Fm. of
Pogonip Cjroup; overlain by Ely Springs Dolomite.
Consists of Barrel Spring Fm. (below), mostly impure
quartzite, shale, limestone; and undifferentiated upper
part, 16()-208 ft. thick, composed of impure carbonate
rocks, shale, and quartzite tongues. Lithology of the
quartzite: individual beds markedly lenticular; blocky,
white- or buff- weathering; massive, vitreous, white,
fine- to medium-grained.

Lies on sandy buff- to brown-weathering Pogonip(?)
Dolomite- CDverlain by dark Ely Sprtngs(?) Dolomite
with chert nodules near the base. Consists of a main
part of massive quartzite with a basal 15 ft. and an
uppermost 2 ft. of platy, impure quartzite. Lithology of
the massive quartzite: reddish- or yellowish brown-
weathering. Has poorly defined bedding planes 2 in.
to 1 ft. apart. Cross bedding present but uncommon.
White to pale pink.

Lies on gray, sandy dolomite of Pogonip Limestone. Over-
lain by dark gray Ely Springs Dolomite v/ith abundant
chert nodules near base. Lower 1 50 ft. consists of inler-
bedded hematitic quartzite, vitreous quartzite, and
platy quartzite. Upper 250 ft. consists of vitreous quartz-
ite. Lithology of the upper part: forms blocky cliffs or
is covered with angular talus blocks. While or pinkish,
vitreous quartzite. In thin section: quartz grains 0.25-
0.30 mm. dia., well rounded with quartz cement in
optical continuity, making an interlocking mosaic.

Lies on gray dolomite of Pogonip Limestone; overlain by
nodular Ely Springs Dolomite. Lithology: white to gray-
ish, vitreous quartzite with numerous steep-dipping
zones 5-10 ft. wide of soft material. Representative
partial analysis: AbOs, 0.105%; alkalies, 0,085%.

Lies on medium graydolomite with dark brown-weathering
siliceous beds of Pogonip Group. Overlain by dark
gray Ely Springs Dolomite with chert nodules. Mostly
vitreous quartzite, but has brown-weathering, in part
platy, quartzite near base- Lithology: white to gray,
massive, vitreous quartzite with virtually no feldspar or
ferromagnesian minerals.

Lies on dolomite beds that contain Lower Ordovician
fossils. CDvcrlain by dark gray Ely Springs(?) Dolomite.
Lithology: yellowish brown-weathering. Beds a few
inches to 1 ft. thick. White, saccharoidal quartzite.

Lies on Pogonip Limestone, which is sandy or quartzitic
in places near the top. Overlain by dark gray Ely Springs
Dolomite containing chert nodules near the base. Lower
part is platy, iron-bearing quartzite with some shale.
Upper part is nearly white, massive, vitreous quartzite.

Lies on micaceous, somewhat shaly, quartzite with a few
beds of dolomite. Overlain by fossilifcrous, green shale.
Lithology: Light pink, cross laminated, saccharoidal
quartzite.

Dibblee 52:19; 54; Ver Planck,
unpublished field notes.

Production of andalusite. JeHrey
31:460; Melhase 25:92;
Wright 57:276, fig. 3.

Dibblee 52:16, pi. 1.

Production of qutrtzite for manu-
facture of super duty silica
brick, 1956 intermittent to
present (1961) by Brownstone
Mining Co- for Gladding,
McBean & Co. Bateman 54;
Jennings 58; herein.

Bateman 54; Greife 59; Langen-
heim 56:2092, 2093.

Hazzard 37a: 324, 325, fig. 3;
Jennings 58.

McAllister 52:12, 13, pi. 1.

Quartzite for manufacture of super
duty silica brick produced 1955
by Mineral Materials Co. for
Gladding, McBean ft Co.
Bateman 54; Brooks 55; Jen-
nings 58; herein.

Gay 55; Hall 58:7, pi. 2; Page
51:8, fig. 5.

Hopper 47:408, pi. 1.

McAllister 55:11.

Hopper 47:406, pi. 1

California Division of Mines and Geology
BASIN-RANGES-Continued

Bull. 187

No.

A3«

Formation (group)
Locality

Location

Geolosv

Remarks and rcfcrcncts

Lower Cambrian
Zabriskie Quartzitc
Dublin Hills (member
Wood Canyon
Formation)

McLain Peak

Nopah and Resting
Spring Ranges

Stirling Quartzite
Alexander Hills

Dublin Hills

Nopah and Resting
Spring Ranges

Tecopa

Later Precambrian

Quartzitc in Pahrump
Series
Alexander Hills

Saratoga Hills

Sec. 35, T. 22 N., R. 6
E., SB., in Dublin Hills
west of Shoshone.

Sec. 18, T. 20 N., R. 7
E., SB., 10 mi. S. of
Shoshone.

Sec. 13, T. 21 U., R. 7
E., SB., 21/2 mi. N. of
Resting Spring on W.
face of Resting Spring
Range (section of
Hazzard 37a). Also
occurs for 1 V^ miles
S. of Shoshone-Pah-
rump road on W. face
of Resting Spring
Range, on E. side Emi-
grant Pass, and near
Noonday mine in
Nopah Range.

Sec. 34, T. 20 N., R. 8
E., SB., on E. side of
Tecopa Pass and ex-
tending to S.

Sec. 23, T. 22 N., R. 6
E., SB., on isolated
spurs along north
edge of Dublin Hills.

Sec. 10(?X T. 20 N.,
R. 8 E., SB., N. of
Noonday mine in No-
pah Range (section of
Hazzard 37a). Also
W. front Nopah
Range 2-4 mi. N. of
Emigrant Pass and for
1 Yq mi. at S. end of
Resting Spring Range.

Sec. 4, T. 20 N., R. 7
E.J SB., in isolated
hiiis just south of
Tecopa Hot Springs.

Sees. 3, 4, 9, T. 19 N.,
R. 8 E., SB. (proj.)
Sees. 32, 33, T. 20
N., R. 8E.,SB.,south
of Tecopa Pass in
Alexander Hills.

Sees. 25, 26, L 19 N.,
R, 5 E., SB. (proj.) in
Saratoga Hills, S. end
Death Valley.

200 ft. thick (may be
repeated by faulting).
Outcrop length 750
ft. in best exposure,
but outcrops in the
area total several mi.

40 ft. thick. Exposed
without overburden
within an area of 50-
100 acres.

Approx. 100 ft. thick.
Total outcrop length
is several mi.

Total thickness 2,000
ft. Outcrop length 2-
3 mi.

East-dipping quartzite
exposed in area of
50-100 acres.

Average outcrop width
3,000 ft. Total out-
crop length is several

Steep-dipping beds ex-
posed in area of 10-
20 acres.

Quartzite-bearing mem-
bers, max. 1,500 ft.
thick; outcrop length,
1-2 mi.

Quartzitc members, max.
800 ft. thick exposed
in E. -dipping, rela-
tively undeformcd sec-
tion with outcrop 2
mi. long.

Lies on purplish gray quartzite containing sandy, micace-
ous, and feldspathic(?) layers. Overlain by brown
quartzite intcrbedded with greenish, schistose shale.
Lithology: faintly pink to grayish, vitreous quartzite
with sparse pin point-sized black and brown specks.
Parts are cut by V's-'nch quartz veins. In thin section:
quartz grains, av. 0.2 mm. dia., many well rounded ■with
oriented overgrowths^ also anhedral grains not notably
interlocking. Scricite, tourmaline, zircon, magnetite,
and limonite present but not abundant. Representative
analysis: SiO:, 99.39%; Al-Oj. 0.36; Fe203, 0.04;
TiOs, 0.0; P20s, 0.0; CaO, 0.0; MgO, 0.0; Na:0,
0.016; KjO, 0.081; H20, 0.11.

Lies on gray, banded quartzite and pebbly quartzite.
Lithology: Brownish-weathering, massive quartzite that
forms blocky talus. In hand specimen: slightly pinkish,
vitreous quartzite with sparse black specks. In thin
section: quartz, mostly in rounded grains. Interlocking
texture not well developed. Has minor interstitial
serieite.

Lies on gray, micaceous, platy shale with brown-weather-
ing sandstone beds. Overlain by rusty brown-weather-
ing, platy quartzite interbedded with dark greenish,
sandy shale. Upper 100 ft. consists of massive, vitreous
quartzite. Lov/er 60 ft. consists of reddish-brown,
sandy shale end shaly quartzite, locally conglomeratic,
v/ith 10 ft. of massive quartzite at base. Lithology of
massive upper part: Salmon-pink- to rusty brown-
weathering, massive, indistinctly cross bedded, pinkish
to light gray quartzite in beds 1-6 ft. thick.

Lies on interbedded shale and quartzite with subordinate
dolomite of upper part of Johnnie Fm. Overlain by
greenish-gray shale, quartzite, and dolomite of low/er
part of Wood Canyon Fm. 3 members. Lower (600 ft.):
massive, gray quartzite, locally pebbly; middle (600 ft.):
red shaly to platy quartzite; upper (800 ft.): light gray,
massive quartzite. Lithology of the massive quartzite:
feldspathic.

Section observed consists mostly of gray quartzite with
brown sandy beds and impure quartzite at the base.
Lithology of the gray quartzite: faintly pinkish, obvious
rounded grains. In thin section: mostly rounded quartz
grains 0.3-0.6 mm. dia. with minor recrystallizcd chert,
plagioclase, and interstitial serieite.

Lies on shale, impure dolomite, or quartzitc of Johnnie
Fm. Overlain by sandstone and shale of Wood Canyon
Fm. 3 members. Lower (1,000 ft.): dense to fine grained
light gray to pinkish quartzite, indistinctly cross bedded,
beds 2 ft. thick. Lenses of quartz pebbles. Partings of
siliceous shale; middle (175 ft.): shaly, micaceous sand-
stone with dolomite lenses; upper (1,200 ft.): gray
quartzite similar to lower member but without pebble
lenses.

Heterogeneous. Light to dark, cross bedded quartzite,
brown to black shale. Beds 5-25 ft. thick. Specimen
from the lightest quartzite consists of quartz grains with
sparse feldspar and limonite.

Lies on earlier Precambrian rocks, mostly gneiss. Overlain
by Lower Cambrian Noonday Dolomite. From base to
top: Crystal Spring Fm. (quartzitc, shale, 1,500 ft.;
cherty dolomite, limestone, massive chert, 900 ft; quartz-
ite, shale, dolomite, diabase sills, 1,900 ft-), Beck Spring
Dolomite (1,200 ft.), Kingston Peak Fm. (quartzitc, 700
ft-; impure conglomeratic quartzitc with dolomite and
quartzite dasts, 1,800 ft).

Lies on earlier Precambrian rocks, mostly quartzite, schist,
and gneiss. Overlain, at least locally, by brown quartzite
of Lower Cambrian Noonday Dolomite. From base to
top: Crystal Spring Fm. (conglomerate member, 20 ft.,
max.; feldspathic quartzitc member, 350-1,300 ft.;
purple shale member; fine-grained quartzitc member,
100-250 ft.; carbonate member; chert member; upper
units). Beck Spring Dolomite, Kingston Peak Fm. (green
quartzitc member, 450 ft,/ conglomeratic quartzitc
member). Lithology of feldspathic quartzite member;
medium light gr<y, coarse-grained pebbly quartzite
grading upward to yellowish, fine to medium grained
quartzite. In thin section: 10-25% feldspar, mostly
microclinc, 2-5% clay and serieite. The remainder is
quartz in angular, poorly sorted grains, some recrystal-
lizcd, some retaining original clastic outlines. Lithology
of fine-grained quartzite member: fine-grained, yellov/-
ish brown, thinly layered to massive, contains lenses of
sandy dolomite. Lithology of grcrn quartzitc member:
olive to greenish gray, finegrained quartzitc and shale.

Chcsterman, unpublished; Mason
48; herein.

Herein.

Hazzard 37a:306, fig. 3; Mason
48; herein.

Wright 54b.

Mason 48; Ver Planck, unpub-
lished field notes.

Hazzard 37a;306, fig. 3; Mason
48.

Mason 48; Ver Planck, unpub-
lished field notes.

Wright 54b.

Wright 52:9-15, pi. 1.

1966

QUARTZITE

MOJAVE DESERT

Formation (group)
Localitv

Location

Geology

Remarks and references

Pre-Mesozoic

Quarlzile in Vitrefrax
Fm.
Cargo Muchacho
Mtns.

Paleozoic (?)

Quartzitc in Maria Fm.
Big Maria Mtns.

Little Maria Mtns.

Palen Mtns.

Saragossa Quartzite
NewbertY Mtns.

Vitreous quartzite series
of Eagle Mtns.

Metasedimenls in Ante-
lope Valley

Quartzites and marble
Fry Mtns.

Permian (?)

Quartzite in Hodge
Volcanic Series
Hodge

Carboniferous

Quartzites of Or
Grande Series
Quartzite Mtn.

In and near Sec. 19, T.
15 S., R. 21 E., SB.
(proi-), west side
Cargo Muchacho
Mtns. near Ogilby.

T. 4 S., R. 22 E,, T. 4
S., R. 23 E., SB,, m
south-central part of
Big Maria Mtns.

Sees. 1, 3, 10, 11, T.
4 S., R. 20 E., SB.
(proj.), approx. 3 mi.
W. of Midland.

NE. cor. T. 2 S., R. 18
E., SB. tproj.), 20 mi.
NE. of Desert Center
near Palen Pass.

Secs. 12, 15, 22, T. 6
N., R. 3 E., SB., on
SW. flank Bessemer
Mtn. and NE. border
Fry Mtns.

Sees. 31-36, T. 3 S.,
R. 14 E., SB. (proj.)
in NE. part of Eagle
Mtns.

Mostly T. 9 N-, R. 17
W., SB.,N. ofQuinn
Ranch at head of An-
telope Valley.

Sees. 18, 19, T. 6 N.,
R. 3 E., SB., along
crest of Camp Rock
Ridge on N. border
of Fry Mtns.

Sees. 28, 29, 31, 33,
T. 9N.,R. 3W.;Sec.
36, T. 9 N., R. 4 W.,
SB , NW. of Hodge.

Sees. 9, 10, 11, 14, 15,
16, 17, T. 6 N., R.
4 W., SB., E. of Oro
Grande on N. slope
of Quartzite Mtn.

Comparatively small

masses of quartzite
associated with mica
schist and quartz-
kyanite rock.

Quartzite units several
hundred ft. thick as-
sociated with meta-
scdiments having total
thickness of several
thousand ft. and out-
crop area of 25 square

Quartzite member 500-
600 ft. thick with
outcrop approx- 1 mi.
long dips 55"-70°
NW.

Quartzite 200-300 ft.
thick with outcrop
several thousand ft.
long.

Exposed thickness, 360
ft. outcrop area 1-2
square mi.

At least 150 ft, thick.
Outcrop area 5,000
ft. wide.

Minor quartzite associ-
ated with marble and
hornfels in unit 2,500

ft. thick.

Comparatively small out-
crops of intcrbedded
quartzite and marble,
max. thickness 490 ft.

Steeply dipping quartz-
ite lenses up to 200
ft. thick; max. strike
length 1,000 ft.

At least 2 quartzite units
several hundred ft.
thick with outcrops
several thousand ft,
long.

In contact with intrusive quartz diorite. White quartzite
at base grading upw/ard into scricite schist or quartz-
mica schist and kyanite-bearing schist, Lithology of the
white quartzite: fine grained, gray quartzitc composed
of equidimensional quartz grains, sparse kyanitc and
iron oxide.

Thin-bedded quartzites, thick bedded quartzites, associ-
ated with crystalline limestone and relatively small
amounts of mica schist and gypsum. Some quartzites are
almost pure,- others are calcareous.

Lies on buff-wcathcring, white limestone with gypsum-
bearing zones. Overlain by dark-weathering, tan lime-
stone with minor quartzite beds. Lithology: brecciated,
faintly banded, tan to white. In thin section: 90% quartz
in interlocking, equidimensional grains. The remainder
is feldspar and biotite.

In northeastern gypsum-bearing scries of Hoppin (54),
quartzite of several types occurs with marble, laminated
marble, lime silicate marble, gypsum, and green schist
in a complexly deformed section. Lithology of relatively
pure quartzitc pink quartzite containing white mica
and scattered euhedra of hematite.

Roof pendants in granitic rocks. Red, pink, brownish-
black weathering, iron-stained, missive quartzite, sugary
in appearance. In thin section: rounded to subroundcd
quartz grains 0.5-1,0 mm. dia., original grains outlined
by sericite. Has quartz overgrowths, Pyrite present.

Lies on gneiss. Overlain by the dolomite-quartzite series
containing the lower iron ore bed of Eagle Mtns.
Lithology; massive, dense, hard, usually coarse grained
quartzite with disseminated grains of iron oxide.

Isolated roof pendants in granitic rock. From base to top:
coarse, blue-white marble, 4,000 ft.; gray and reddish,
sandy limestone, pinkish-gray quartzite, black biotite
hornfels, 2,500 ft; medium- to coarsely-crystalline,
bluish-gray marble 2,500 ft. Lithology of the quartzite:
well bedded, layers a few ft, thick, indistinctly cross
bedded, highly jointed.

Intruded by quartz monzonite. May lie on Saragossa
Quartzite. Lithology of the quartzite: commonly green-
ish, but some is buff or white. In thin section: interpene-
trating, anhedral quartz grains with an amphibole (par-
gasite-?) forming wisps, shreds, radiating Fibers within
or between quartz grains.

Quartzite enclosed in sericite schist and biotite schist.
Lithology of the quartzite: slightly grayish, vitreous,
composed of interlocking quartz crystals, 0.2 mm. av.
dia. Sparse non-quartz grains. Chemical analysis: SiOj,
99.44%; AIiOj, 0.39; Fe20), 0.056; TiO:, 0.0; PiQs,
0.0; CaO, 0,0; MgO, 0.0; Na-Q, 0.002; K!0, 0.04;
H?0, 0.07.

Type section of Oro Grande Series on Quartzite Mtn.,
base to top: white dolomite, 1,200 ft.; dark schist-horn-
fcls, 350 ft,; blue-gray limestone, 250 ft.; dark sehist-
hornfcls, 60 ft.; massive quartzite, 250 ft.; black schist
with limestone subunits, 500 ft.; massive quartzitc indis-
tinguishable from lower quartzite, 250 ft. Lithology of
the quartzites: brown-weathering, pinkish white to
grayish, massive quartzite. In thin section: almost entirely
quartz grains, 0.2-1.0 mm. dia., with irregular bound-
aries/ sparse sericite and muscovite. Typical analysis:
SiOi, 98.90%; AtsQj, 0.16; FeiOj, 0.18; TiOi, 0,04;
CaO, 0.23; MgQ, 0.08; alkalies, 0.24.

Production of kyanite. Henshaw
42:1 53, 1 54, pi. 2; Ver Planck,
unpublished Field notes; Wright
57 276, 277.

Miller 44:26.

Section Twenty Hilts

SE. i^Sec.12,T. 8N.,
R. 2 W., SB., 7 mi. S.
of Barstov/ off Lu-
cerne Valley road

Gently to moderately
dipping quartzite
beds; outcrop several
hundred ft. wide, V^
mi. long.

In (fault-?) contact with granite gneiss. Very coarse
grained, gray to dark gray, somehwal platy quartzite.
In thin section: 90-95% auartz grains, 0.6-1.0 mm.
dia. with interlocking boundaries; crudely banded with
muscovite; minor biotite and magnetite.

Ver Planck 52:16, pi. 2,

Hoppin 54:14, pi. 1.

Gardner 40 265, 266, pi, 2.

Undeveloped (Harder 12:30-35,
pi. 1, fig. 3; Hadley 48:4, 5,
pi, 2; herein.)

Wiese 50:16-18.

Gardner 40:266.

Operations: 1) Golconda quarry,
SW. 14 Sec. 36, T. 9 N., R. 4
W., Emsco Refractories Co.
produced several hundred tons
quartzite approx. 1930 for
silica brick; 2) Kennedy quarry,
Sec. 31, T. 9 N., R. 3 W..
Atlas Fire Brick Co. produced
quartzite at rate of 3,000-
4,000 tons per year during
1920*s for silica brick. Bowen
54:34-36, 176, 177, pi, 1;
herein.

Operations: 1) Atlas quarry, NE.
Vi SE. V4, Sec. 17, Mineral
Materials Co., produced 150,-
000-200,000 tons quartzite,
1939 to present (1961) for
Portland cement and (up to
1954) silica brick; 2) Emsco
quarry, NW. V4, NE. V4, Sec.
1 1 , Emsco Refractories Co.,
produced several tens of thou-
sands of tons quartzitc, approx. -
1928-1945, for silica brick;
3) Riverside Cement Co., NE.14
NW.!4 Sec. 17, produced
several hundred thousand tons
quartzite since approx. 1940
for Portland cement and silica
brick;) 4 Southwestern Port-
land Cement Co., E. part Sec.
11, produced over 1 million
tons quartzite for portland
cement and railroad ballast.
Bowcn 54:23-34, 175-178;
Bowen and Ver Planck, 65;
herein.

Bowcn 54:178; Ver Planck, un-
published field notes.

California Division of Mines and Geology
MOJAVE DESERT-Continued

Bull. 187

Map
No.

As«

Formation (group)
Locality

Shadow Mtns.

Lower Cambrian
Prospect Mtn.
Quartzitc

Bessemer Basin

C!«rlc Mtns.

vanpah Mtns.

Kingston Range

Marble Mtns.

Mesquite Mtns.
(southeast)

Mesquite Mtns.
(northwest)

Old Dad Mtn.

Lower Cambrian

Prospect Mtn. Quartzite
Providence Mtns.

Ship Mtns.

Location

Sec. 31, T. 8 N., R. 6

W., SB., in Shadow
Mtns.

Sec. 5, T. 5 N., R. 5 E.,
SB., on hill NW. of
Gaiway Lalee.

E. part T. 17 N., R. 12
E., to NW. part T.I 7
N., R. 13E.,SB.,ap-
prox. 3 mi. NW. of
Clarlc Mtn.

Sec. 2, T. 15 N., R. 13
E., SB., 3 mi. W. of
Kokoweef Pk,; Sec.
14, T. 15 N., R. 13
E., SB., 2 mi. NW. of
Standard no. 1 mine;
W. 1/2 Sec. 10, L 15
N., R. 14 E., SB.,
near New Trail mine;
N. 1/2 Sec. 22, T. 15
N., R. 14 E., SB.,
near AITured Hillside

T. 20 N., R. 10 E., SB.,
on ridge W. of Rest-
ing Spring road, and
T. 20 N,, R. 11 E.,
SB., on ridge 3 mi.
NE. of Horse Spring.

NE. Va Sec. 28, T. 6
N., R. 14 E., SB,,
approjf. 2 mi. NE. of
Chamblcss at south
end of Marble Mtns.

NE. part T. 18 N., R.
12 E., SB., in Mes-
quite Mtns, W. of
Mesquite Pass.

E. part L 19 N., R. 11
E., SW. slope of the
hills NW. of Winters
Pass.

Sees. 3, 4, T. 12 N., R.
10 E., SB. (pro;.), in
NW. part Old bad
Mtn., Sees. 25, 26,
33, 34, T. 13 N^ R.
10 E., SB., near Sev-
cnteenmile Point.

NE. part T. 10 N., R.
13 E., toSW. partT.
11 N.. R. 14 E., SB.-,
on NW. slope of
Providence Mtns. be-
tween Hayden Wash
and Cornfield Spring
Canyon.

Sec. 9, J. 4 N., R. 15
E., SB., SW. cor. Ship
Mtns. and Sec. 15, T.
5 N., R. 15 E., SB.,
NW. end Ship Mtns.

Comparatively thin, gen-
tly dipping quartzite
units, outcrop areas
up to 800 ft. wide
and V2 mi. long.

Exposed thickness, 75
ft.; outcrop, 1/5-mi.
long.

Exposed thickness at
least 1,500 ft., out-
crop area severa I
square mi.

Relatively small outcrops
exposed in deformed
sections.

Exposed thickness 4,700
ft. Outcrop width 3
mi. Strike length ap-
prox. 2 mi.

Quartzite units several
hundred ft. thick in
total thickness of 390-
450 ft. Strike length
2-3 mi.

3,000-4,000 ft. thick.
Strike length 2 mi.

Max. thickness 500 ft.,
outcrop length several

Quartzite units 50-100
ft. thick in total thick-
ness of at least 2,142
ft. outcrop area, 2-3
square mi.

Quartzite units several
hundred ft. thick in
total thickness of
1,085 ft. Total out-
crop length, several
miles.

Small outcrops of Lower
Cambrian rocks.

Geolosy

Quartzite occurs near base of Oro Grande Series. Over-
lain by platy limc-stlicatc hornfels, schist, and marble.
Lithology of the quartzite: massive to well bedded,
commonly feldspathic.

Lies with depositional contact on t tic rocks. Red-
brown weathering cross bedded quartzite, beds 3-4
in. thick, with sub-rounded chert and jasper pebbles,
especially near base. In thin section: interpenetrating
quartz grains, original sand grains outlined by sericite
and iron oxide. No feldspar observed.

Folded section in fault contact with Goodsprings Dolomite.
Overlain by Pioche Shale. Mostly quartzite but has
shale layers. Lithology; iron-stained, light gray to tan,
coarse to medium grained vitreous quartzite with abun-
dant magnetite. No minerals except quartz and magnet-
ite observed.

Fault contact at base. Overlain by Pioche Shale. Section
near New Trail mine, base to top: conglomerate with
pebbles of quartz, jasper, fiint; cross-bedded, medium
to coarse red quartzite, beds 5-10 ft. thick, 500 ft.;
fine to medium, gray to white quartzite with 12-inch
partings of micaceous phyllite, 200 ft,; gray dolomite.

Lies on Noonday Dolomite. Overlain by Pioche Shale.
Lithology: mostly sandstone. Lowest 1,000 ft., from
base: red shaly sandstone 75 ft.; thin gray dolomite, 100
ft,; Fine grained quartzite with beds of vein quartz and
chert pebbles, 500 ft.; oolitic dolomite at 700-800 ft.
above base, gray dolomite with quartz pebbles up to
y2-in. dia. at 1,000 ft. above base.

Lies on Precambrian granite with depositional contact.
Overlain by Lower Cambrian shale. From base to top:
Quartzite conglomerate with pebbles of quartz, chert,
and jasper, 12 ft.; dark brown to gray quartzite, 351 ft.,
light gray to white quartzite, 55 ft,,- quartzite and shale,
27 ft-; green shale, 40 ft.; bluish limestone, 118 ft.
Lithology of the quartzite: beds y2-3 ft. thick, has peb-
ble lenses and shaly layers. Cross bedded. Gray, white,
or brown. Iron-stained. Quartz, 85-98%; feldspar,
1-14; zircon, apatite, magnetite, 1.

Broad W.-pitching syncline. At base is in fault contact
with Minte Cristo Limestone. Overlain by alluvium.

Lies on Precambrian granite gneiss with depositional con-
tact. Overlain by aluvium. Lithology in SE part: white
granular quartzite with dense, blue-gray, vitreous layers,
thin layers of feruginous dolomite, conglomerate with
V^-in. dia. pebbles. In NW. part: mostly indurated shale.

Lies on Precambrian gneiss with depositional contact.
Overlain by Pleistocene gravel. Lithology: massive
dolomite, mainly in the lower part; quartzite, throughout
the section; black slate, mostly in the middle part; dolom-
ite, quartzite, shale, sandstone, in upper part. The
quartzite units: beds up to 20 ft. thick, cross bedded
locally, with conglomerate lens containing quartz and
jasper pebbles near top. Red-brown, brown, gray or
white.

Exposed in E. -tilted fault blocks. Lies on Precambrian
granite, gneiss, schist with depositional contact. Over-
lain by Latham Shale. From base to top: greenish black,
shaly quartzite with pebble lenses near base, 10 ft.;
limestone, locally dolomitized, 30-50 ft.; dark, platy,
fine grained quartzite, 50 ft.; brownish- weathering,
white, fine bedded quartzite, cross bedded, local peb-
ble lenses, layers 1/2-2 ft. thick, 725 ft.; dark, shaly to
platy, fine grained quartzite, 1 30 ft,; browmsh-weather-
ing, massive, white quartzite, layers 2-6 ft. thick, 120
ft. Lithology at Toughnut Spring (Sec. 30, T. 11 N.,
R. 14 E.): heterogeneous, cross bedded, iron-stained.
Includes shaly layers; fissile, thin bedded quartzite;
layers with quartz and jasper pebbles; white vitreous
quartzite. The while quartzite in thin section: poorly
sorted quartz grains with abundant iron oxide and a
little zircon. Has rounded grains 0.6 mm. dia. in a matrix
of angular, interlocking grains 0,06 mm, -0.3 mm. dia.

Includes Prospect Mtn. Quartzite, Latham Shale, Chambless
Limestone.

Remarks and refcrtnccs

Troxel 54.

(Gardner 40:264, pi. 2.)

Crosby 51:628, 629; fig. 2; Hew-
ett 56:29-31, pi. 1; Ver
Planck, unpublished field notes.

Hewetl 56:29-31, pi. 1; Patchick
59.

Hewett 56:29-31, pi. 1.

Clark 21; Hazzard 33; Lamey
48b:103, pi. 10; Ver Planck,
unpublished field notes.

Hewett 56:29-31, pi. 1.

Barca 66; Hewett 5629-31, pi.
1; Lamey 48a:62, 63, fig. 21.

Hazzard 33; 37b; 55: table 1,
pi. 2; Ver Planck, unpublished
field notes.

Hazzard 33.

1966

QUARTZITE

MOJAVE DESERT-Continued

I Age
Map Formation (group)

No. I Locality

Location

Geology

Ramarhs and references

Soda Mins.

Winte

Later Precambri
Quartzitc ir
Series
Kingston Range

Pahrump

Silurian Hills

Earlier Precambrian
Quartzite In Pelona
Schist
Portal Ridge

Tehachapi Mtns,

Earlier Precambrian

QuartzUes in Rand Schist
Rand Mtns.

Metasediments in
Newberry Mtns.

Mctasediments near Sil-
ver Lalce

Melasedimenis near Yuc-
ca Grove

Sees. 29. 20, 31, 32,
T. 15N., R. 8E.. SB.,
in Quartzitc Hills of
Grose.

Sec. 33, T. 19 N., R.
12 E., adjoining part
T. 1872 N.,R. 12 E.,
SB., NW. side of
Winters Pass.

S. edge T. 20 N., R. 9
E., to E. edge T. 19
N., R. 10 E., SB., on
N. and NW. slope of
Kingston Range.

Mostly T. 17 N., R. 9
E., SB , in Silurian
Hills.

W. part T. 6 N^ R. 12
W. toS. partT. 7N.,
R. 14W.,SB.,onPor.
tal Ridge NW. of
Paimdale.

T. 10 N., R. 16 W., T.
ION., R. 17 W., SB.,
on S. flank of Tehacha-
pi Mtns. facing Ante-
lope Valley.

Center T. 30 S., R. 39
E. to NE. cor. T. 30
S., R. 40 E., MD., in
Rand Mtns., mostly
SW. of Randsburg.

Sec. 33, T. 8 N., R. 3
E.,SB.,on W. sidcof
Kane Wash.

Sees. 21, 22, 23, T. 16
N., R. 9 E., SB.,
(proj.), in hills E. of
Silver Lake.

Sec. 3, 4, T. 15 N., R.
11 E., SB., N. of Yucca
Grove.

Quartzite units several
hundred ft. thick in
total thickness of
2,250 ft. Total out-
crop area 1-2 square

4,200 ft. thick, outcrop
length approx. 2 mi.

Has quartzitic units sev-
eral hundred ft. thick
in max. thickness of
7,000 ft. Total out-
crop length approx.
10 mi.

Quartzitic units with-
in total thickness of
11.000 ft.

Quartzite beds a few
ft. thick.

Minor quartzite beds
associated with 5,000
ft. of schist.

Quartzite beds, max. 10
ft. thick, max. outcrop
length Va mi., in a
great thickness of
schist.

Minor quartzite and
marble in outcrop area
of Vo square mi.

Quartzitc unit 25 ft.
thick, outcrop length,
several thousand feet.

Undetermined but small
extent.

Lies on Lower Cambrian limestone and dolomite. Qvcr-
lain by alluvium. Lower member, impure dolomite inter-
stratified with dark quartzite, 400 ft. thick; middle mem-
ber, massive, dense, white, vitreous quartzilc, 350 ft.
thick; upper member, similar to lower member, 1,500
ft. thick. Lithology of middle member' cross bedded,
fine grained to conglomeratic, clasts angular, mostly
recrystallized. Feldspathic locally. Dark quartzite of
upper member contains 95% quartz, 5% biotite.

Lies on Noonday Dolomite. Qverlain by Pioche Shale.
Lower 1,000 ft.: mostly dense, cherty quartzitc with a
few beds of dolomite and red shale up to 10 ft. thick
and cross bedded conglomerate beds 5-10 ft. thick
with quartz pebbles 1-2 in dia. 2nd 1,000 ft.: mostly
quartzite, dolomite less common, brown-weathering
oolite beds 1 500 ft. above base. Upper 2,000 ft.:
mostly rusty orown-weathenng, thin bedded, fine
grained quartzite. Lithology of quartzitc from upper
part: sandy looking, brownish, iron stained quartzite
composed of quartz with some feldspar.

Lies on earlier Precambrian granite gneiss. Overlain by
Noonday Dolomite From base to top: Crystal Spring
Fm., 1,616-2,200+ ft. thick (lithology varies. N, of
Beck Spring: shale and dolomite with limestone. W. of
Beck Spring: 1,000 ft. of dark brown quartzite. NE. of
Horse Thief Spring; 500 ft. of conglomeratic quartzite
with V2-5-in. clasts at base; arkosic grit; 200 ft. of cross
bedded white sandstone,- 50 ft- of dense black cherty
quartzite; chert and dolomite); Beck Spring Dolomite,
1,137 ft. thick; Kingston Peak Fm., 1,000-2,000 ft.
thick (lithology varies. NE. of Beck Spring: sandstone
and conglomerate with limestone and quartzite cobbles.
NE. of Horse Thief Spring: sandstone and conglomeratic
sandstone with quartz cobbles up to 10 in. aia. SE. of
Horse Thief Spring: 400 ft. of shale and greenish quartz-
ite; sandstone and dolomite with dolomite and quartzite
cobbles; 100 ft, of red, shaly quartzitc and dolomite).

Exposed in a chaos structure beneath Riggs thrust fault.
Quartzitic members, base to top: map unit Aa (mixed
sediments), member 2, granular white quartzitc, 175
ft.; map unit Ab (quartzite and carbonate rocks); member
7, white quartzitc, 320 ft , member 9, white quartzite
and quartz cobble conglomerate, 600 ft ; map unit Ae
(mixed sediments) member 19, impure quartzite with
some conglomerate, 475 ft ; member 22, granular
quartzite and siltstone, 225 ft ; member 23, red-brown
quartzite with iron-rich cement; member 24, vitreous
gray, granular quartzite, 185 ft.; map unit Af (quartzite
and siltstone); member 26, vitreous quartzitc, 80 ft.;
member 28, white vitreous quartzite, 50 ft.; member
30, white vitreous quartzite, 220 ft ; member 31, cross
bedded quartzite, 950 ft,; member 33, massive vitreous,
pinkish quartzite, 380 ft.

Quartzite is associated with a great thickness of schist.
Lithology of the quartzite: clastic characteristics almost
obliterated, banding marked by fine scricite grains,
quartz grains have sutured borders.

Quartz biotite schist banded with quartzite grades into
massive quartzite with dark lines of impurities.

Minor quartzite associated with limestone in upper part
of Rand Schist. White, pinkish, brownish, or manganese-
stained. Purity varies from essentially pure quartzite to
quartzitc with thin layers of brown biotite. Has traces
of original rounded sand grains.

Gneiss grading to orthoclase quartzite and biotite quartz-
ite. Lithology of orthoclase quartzite: blasto-clastic
texture, pink bands of orthoclase and quartz alternating
v/ith dark bands of biotite. Lithology of biotite quartz-
ite: blasto-clastic texture; Quartz, 70%; orthoclase,
20; biotite. Magnetite, titanite, zircon present in both
varieties.

Roof pendant in granitic rocks. From base to top: lower
units, 400 ft,; hornfcis member, 155 ft,; quartz-biotite
schist member, 185 ft.; quartz-muscovile schist member,
125 ft-; marble member, 60 ft.; quartzitc member, 25 ft./
upper units, 400 ft. Lithology of the quartzite: light
gray, medium grained, massive, compact, vitreous. In
thin section: quartz, 90%; feldspar, 10, mica, 2-3.
Quartz grains have sutured boundaries, are markedly
elongate. Feldspar and mica grains are smaller than
quartz grains.

Quartzite included in roof pendant in granitic rocks.

Grose 59:1516, 1517, pi. 1.

Hewett 56:29-31, pi. 1; Ver
Planck, unpublished field notes.

Hewett 56:26, 27, pi. 1.

Kupfer 54.

Simpson 34:378-381; Wallace
49:786.

Wiese 50:12-15.

Dibblee 52:13; Hulin 25:25.

Gardner 40:262, 263.

Wright 54a:9, 27, pi. 1.

Wright 53:202, 216.

California Division of Mines and Geology
COLORADO DESERT

Bull. 187

Map
No"

Age

Formation (group)
Locality

Location

Siie

Geology

Remarks and rcfcrcncts

Paleozoic (?)

Metasediments in Coyote
Mtns.

Sec. 12, T. 16 S., R. 9
E., SB., on S. side
Coyote Mtns.

Outcrop area of quartz-
ite approx. Va sq. mi.

Quartzite and other metasediments intruded by s^dnitic
rocks.

Tucker 26:276.

PENINSULAR RANGES

Pre-Cretdceous

Quartzi*e-bearin9 meta-
sediments
Pala

Red Rose quarry

Upper Jurassic

Quartzite in Bedford
Canyon (Santa Ana)
Fm.
Railroad Canyon

Santa Ana Mtns,

San Luis Rey quad-
rangle

Triassic (?)

Quartzite in Julian Schist
Corral Creek

Cuyamaca

Inspiration Point

Jacumba

Triassic (?)

Quartzite in Julian
Schist
Julian

Quartzite in
Series

Jurupa M(s.

Jurupa

Paleozoic (?)

Quartzite in Palm Can-
yon Complex

Cathedral Canyon

Quartzites in Domeni-
gonl Valley

Quartzite near Santa
Rosa Mtn.

So-central part T. 9 S.,
R. 2W., SB., 2mi. N.
to 3 mi. NW. of Paid.

SW/i Sec. 35, T. 15S.,
R.I E.,SB.,3^mi. NE
of Suncrcst.

Mostly T. 5S., R. 4 W.,
SB., NE. of Elsinorc.

Numerous outcrops.

Numerous outcrops

Cen. part T. 12 S., R. 2
E., SB., lOmi. NE. of
Ramona along Corral
Creek.

BeltfromNE. Cor.T. 14
S., R. 3 E., to cen. T.
16S.,R.4E.,SB.,SW
of Cuyamdca Peak.

Cen. Sec. 16, T. 13 S.,
R. 4E.,SB., ]/2mi.SW.
of Inspiration Point.

SE. partT. 17 S., R. 7 E.,
SB., 21/2 mi. NW. of
Jacumba.

SE. -trending strip 1 mi.
wide from E. part T.
12 S., R. 3E., toSW.
cor. T. 14 S-, R. 4 E.,
SB., through Julian.

Around common cor. T.
1 S., R. 5 W./T. 1 S.,
R. 6 W.; T. 2 S., R. 5
W ; T. 2 S., R. 6 W.

T. 5 S., R. 5 E., SB., ap-
prox. 5 mi. SE. of
Palms Springs in and
near Cathedral Can-
yon.

NE.pirtT.6S.,R.2W.,
SB., S. of Domenigoni
Valley.

Sec. 31,T. 7S., R. 5£.,
SB., 15 mi. SW. of
Indio.

Quartzite and schist,

max. outcrop width

500 ft., strike length
2-3 mi.

Undetermined but small
extent.

Thin quartzite units in
body of metamorphic
rocks with outcrop
area of several square

Thin quartzite units in
several bodies of met-
amorphic rocks with
outcrop areas of many
square mi.

Several bodies of meta-
morphic rock with
outcrop areas of 1 or
2 square mi.

Impure quartzite 300 ft.
thick.

Minor quartzite in chain
of roof pendants total-
ing about 3 square mi.

Lenticular masses of
quartzite 1-500 ft.
thick associated with
schist.

Quartzite associated
with mixed granitic
and metamorphic
rocks.

Minor quartzite associ-
ated with schist.

Apparent thickness as
much as 2,000 ft.

Abundant quartzites and
quartz schists.

Apparent thickness,
12,000 ft.

600 ft. thick; strike
length, ^A mi.

Thin screen of metamorphic rocks separating granodiorite
to N. from gabbroic rocks to S. Lithology: Similar to
parts of Julian Schist.

Red, iron-stained, jointed, impure quartzite in roof pendant.

Roof pendant of slate and phyllite with subordinate
quartzite. Lithology of the quartzite: blackish or reddish
weathering^ feldspathic, contains iron minerals. Sample
from near (jood Hope mine (NW. Vi Sec. 1 5, T. 5 S.,

R. 4 W.) contains 61% quartz.

Roof pendants of argillite and slate ■
pure quartzite.

'ith subordinate

Roof pendants of quartzite and schist. Quartzite is an essen-
tial part of the formation. Lithology of the quartzite:
nearly while to dark gray, fine grained. Commonly im-
pure. Micaceous, feldspathic, grading into arkose,- with
sillimanite.

Laminated quartzite, bands from a fraction of an inch to
several inches thick with mica partings.

Gray to white quartzite locally tnterbcdded with quartz-
mica schist in the form of zones or lenses a few tens of ft.
thick and several hundred ft. long. Lithology of the
quartzite: fine grained, subangular. At least 90% quartz
(mostly 98%), feldspar, mica, small crystals of magnetite.

Usually associated with muscovite-quartz schist. Some of
the quartzite has relict cross bedding.

Light gray, fine grained, foliated, saccharoidal qudrtzite.
Quartz, 91%, sillimanite, 8, magnetite, 1.

Mostly laminated impure quartzite consisting of alternating
quartzite and schist layers from a fraction of an inch to
several inches thick. Forms masses as much as several
hundred ft. thick 1) along W. border of main schist
mass, 2) near Ready Relief mine (Sees. 3, 10, 11, T. 13
S., R. 4 E), 3) near Kentwood in the Pines (Sec. 4, T. 1 3
S., R. 4 E.). Lithology: fine to medium granoblastic.
Quartz, 80%, microclinc, muscovite, magnetite, garnet.

Quartzite associated with marble, gneiss, schist; intruded
by granitic rock. Lithology of the quartzite: yellow-
brown-to dark reddish-weathering, crudely banded,
light gray, vitreous quartzite. Dark bands contain biotite
and chlorite. Some quartzite has disseminated pyrite and
sillimanite (?). Quartz, 80-90%; muscovite, biotite,
hornblende. Grain size, 0.2-2.0 mm.

Metasediments, chiefly mirble, but with quartzites and
quartz schists, injected with igneous material. Lithology
of the quartzites: mostly foliated, light gray, fine to me-
dium grained, biotitic; some arc slightly foliated, fine
grained, with little biotite.

Impure quartzitcj lies on and overlain by slates and schists.
Mostly massive quartzite. Has some thin schist layers and
6 few schist layers as much as 100 ft. thick. Lithology of
the quartzites: much contains little but quartz. Some con-
tains up to 50% feldspar; some is micaceous, grading
into quartz schist. Sutured quartz grains.

Quartzite occurs at the base of a section 10,200 ft. thick
that is intruded by granitic rocks.

Jahns 51:9.

Small tonnage quarried for use as
facing stone. Goldman 57:602.

Dudley 35:494; Engel 59:17-21;
Larsen 48:19.

Engel 59:17-21; Larsen 48:19,
Silbcrling 61.

Larsen 48:20.

Merriam 46:227, 228.

Everhart 51,58-60.

Creasey 46:18, pi. 3.

Brooks 55; Miller 35:120.

Creasey 46:18; Donnelly 34:337,
338; Everhart 51:58-60; Mer-
riam 58:9.

MacKcvett 51:6.

Miller 44:22.

Larsen 48:17.

Wright 46:11, pi, 1.

1966

QUARTZITE

TRANSVERSE RANGES

A»«

Map

Foimation (group)

No.

Locality

Location

Slit

Geology

Rtmvki and rtFtrcncts

Pre-Cr«tdC€Ous

MostlySec. 28, T. 3N.,

Small, thin qua rtzite beds

Typical quartzite: quartz, 73%; feldspar, 25; muscovite, 1;

Oakeshott 37:222, 58:50, 51.

Quartzite in Pldcerita

R. 14 W., SB., in

associated with schist

zircon, rutile, magnetite, 1.

Fm.

Limeroclc Canyon west

and limestone

Little Tujunga

of Little Tujunga Can-
yon.

Carboniferous

Sees. 25, 26, 27, T. 3
N., R. 1 W. SB., E.
of Grecnlcaa Camp.

Scattered patches, 200

Small tongues of massive quartzite m predominantly car-

Richmond 60:16, pi. 1.

Ouartzite m Furnace

ft. thick; max. outcrop

bonate rocks forming roof pendants.

Fm.

length, 4,000 ft.

Greenlead Camp

Prc-Carboniferous

Sees. 25, 26, 36, T. 3

Quartzite units several

Lies on Baldwin Gneiss locally with depositional (?) con-

Guillou 53:7-10, pi. 1.

Quartzilc in Chicopee

N., R. 1 E„ SB., in

tens of ft. thrcl< in

tact. Overlain locally by Furnace Formation (limestone).

Canvon (Chicopee) Fm.
Cnicopee Canyon

Chicopee Canyon

total thickness oF

Four members, base to top: lime-silicate member, ripple-

near Baldwin Lalce

1,150 ft. outcrop

marked member, cross laminated member, upper white

length, several thou-

quartzite member Lithology: mostly quartzite with

sand ft.

abundant feldspar and biotitc except 1) basal 50 ft. of
ripple-marked member: white, platy beds 1-8 in, thick
composed almost entirely of quartz, and 2) upper mem-
ber (150 ft, thick): vague bedding, glossy fracture, iron-
stained, av. grain size less than 0.5 mm. dia.

Holcomb Valley

Sees. 5, 6, T. 2 N , R. 1

Ouartzite unit 370 ft.

Base intruded by tonalile porphyry Overlain by Furnace

Richmond 60:11-15, pi. 1.

E.; Sec. r T. 2 N ,
R. 1 W,, Sec. 36, T.
3 N., R. 1 W„ SB.,

thick in total thick-

Fm, Lower member (1,000 ft thick): cross-bedded

ness of at least 1,320

quartzite, thin-bedded quartzite, micaceous quartzite.

ft. Outcrop area of

Upper member: massive white quartzite (370 ft. thick)

N. of Holcomb Val-

entire formation, 1 sq.

overlain by andalusile-bearing rock (75 ft, thick). Lith-

ley.

mi.

ology: quartzite with abundant feldspar and mica except
massive white quartzite, which is composed almost
entirely of quartz grains 2-5 mm. dia. with sutured,
crcnulated boundaries, Has sparse, minute crystals of
zircon, rutile, sphene, muscovite. Feldspar not observed.

Sarasossa Quartzitc

Approx. Sec. 7, T. 2 N.,

Gently dipping section

Exposed in thrust plate. Lithology: vague bedding, frac-

Production of stained quartzite

Gold Mtn.

R. 2 E., to Sec. 34,

more than 1,000 ft.

tured, heavy iron stain, pinkish or grayish on fresh sur-

for building stone. Guillou

T. 3 N., R. 1 E,, SB.,

(?) thick.

face. In thin section: anhedral, interlocking quartz grains

53:7, pi. 1; Vaughan 22:357;

Baldwin Lalce to Sara-

with feldspar and serictte.

herein.

sossa Spring.

Earlier Precambrian

N. part T. 5 N., R. 13

Thin quartzite beds max.

Thin bedded, fine grained, schistose quartzite

Jahns 54; Oakeshott 58:49, 50,-

Ouartzite in Pelona

W. and S. part T. 6

strike length 1 mi. as-

Simpson 34:378-381.

Schist

N., R. 13 W. to N.

sociated with a great

Sierra Pelona

part T. 5 N., R. 15
W., SB.

thickness of schist.

COAST RANGES

Paleozoic

Quartz rock of Gabilan
Limestone
Fremont Peak

Quartzite in Sur Series
Fremont Peak

Gabilan School

Santa Lucia Range

Sec. 35, T. 13 S., R. 4
E., MD. (proj.; east
of Fremont Peak.

Sec. 35, T. 13 S., R. 4
E., MD-, (proj.) east
of Fremont Peak,

Sec. 16, T. 13 S., R. 3
E IMD., 11/2 mi. W.
or Gabilan School

Santa Lucia Range SW.
of Soledad. Approx.
T. 18 S., R. 5 E.,
MD.

Lenticular body/ outcrop
3,000 ft. long, 500-
1,000 ft, wide.

Lenticular beds 2-3 ft.
thick.

Quartzite up to 180 ft.
thick.

Quartzite layers from a
fraction of an in. to a
few ft. thick in schist
and gneiss.

Silica replacement of carbonate rock, which is associated
with schist of Sur Series and intruded by granitic rock.
Lithology of the quartz rock: gray, vuggy, vitreous
material, mostly quartz in interlocking grains, but with
as much as 10% calcite and calcium silicate minerals.

Minor quartzite associated with schist. Lithology of the
quartzite: pale pink to red, medium to fine grained,
slightly micaceous.

Roof pendant composed of schist, limestone, quartzite. A
section: fine-grained mica schist, 200 ft.; limestone, 250
ft.; light-colored, fine-grained quartzite, 50 ft-; lime-
stone, 300 ft.; pure, well-bedded quartzite, 180 ft,

Quartzite is widespread but not abundant. Lithology:
grayish or tan, fine-grained, vitreous, thoroughly re-
crystallized. None contains more than 90% quartz.
Locally has biotite partings and grades into quartz-bio-
tite gneiss.

Bowcn 59:13, 19, pi. 1; herein.

Bowen 59:13, 19, pi. 1.

Allen 46:20.

Fiedler 44:182; Reiche 36:118-
121.

GREAT VALLEY OF CALIFORNIA

Pre-Cretaceous

Ouartzite NE. of Fresno

A) Sees. 8, 9, 16, 17,
T. 11 S., R. 21 E,,
MD., nr. Friant; B) N.
central part T. 12 S.,
R. 21 E., MD., SW.
of Owens Mtn.

Quartzite layers from
less than 1 in. to 40
or 50 ft. thick. Beds
lens out within short
distance.

Numerous lenticular bodies of quartzite associated with a
great thickness of mica schist. Lithology of the quartzite:
light gray to dark bluish gray, granoblastic texture^ av.
grain size 0.1 to 1 mm. No pure quartzite reported. Con-
tains feldspar, biotite. Some specimens contain horn-
blende, diopside, clinozosite, epidote.

Macdonald 41:220.

Caliform.a Division of Minfs .\\d Geology
SIERRA NEVADA

Bull. 187

Ase

M«p

Formation (group)

Locality

Location

Siie

Geology

Remarks and rcfcrtncts

Pre-Cretaceous

A) S. part T. 8 S., R. 25

Outcrop areas several

Unfoliated impure quartzite with but little mica is inter-

Krauskopf 53:5, pi. 1

Quartzites in E. Fresno

E., N. partT. 9S,, R.

square mi.

bedded with schist and also forms large masses nearly

County

25 E., MD., nr. Tam-
arck Mtn. B) T. 9 S.,
R. 26 E., extending
into T. 9 S., R. 27 E.,
MD., nr. Dinkey

free of schist. Light colored, coarse grained.

Creek. C) SW. cor,
T. 10 S., R. 28 E.,
MD., nr. Woodchuck
Creek. D) NW. part
T. 11 S., R. 27 E.,
extending into T. 11
S., R. 26 E., MD. nr.
Patterson Mtn, E)
NW. part T. 12 S.,
R. 28 E., extending
intoT. 11 S., R. 28 E.,
MD.,nr. Rogers Ridge.
F)NW, cor. T. 13 S.,
R. 29 E., MD., nr. S.
Fork Kings River.

Quartzite near FHospital

Sees. 19, 29, 30, T. 16

Lenticular quartzite out-

Quartzite predominates in SE. part of a roof pendant com-

Ross 58:5, pi. 1.

Rock

S., R. 30 E., MD.,
near Hospital Rock
ranger station, Se-
quoia National Park

crop 3 mi. long, max.
width Yq mi.

posed mostly of schist and limestone. Lithology of the
quartzite: cloudy white to dark gray, massive, fine-
grained. Predominantly quartz, but contains subordinate
feldspar, mica, diopside, apatite, magnetite, zircon.

QuirtzJte near Kaiser

Sees, 25, 26, T. 7 S,, R.
25 E., MD., approx.

Metasediments, mostly

Roof pendant in granitic rocks. Lithology of the quartzite

Chesterman 42251

Hamilton

Peotc

quartzite, outcrop

(after Hamilton): white, gray, or pink, medium grained,

56:7, pi, 1,

3 mi. N. of Hunting-

dred 1 square mi.

contains minor clinopyroxene and plagioclase, biotite

ton Lake.

rare; (after Chesterman) 90% quartz with biotite, has
zircon, sphene, sericite, chlorite, hornblende, zoisite,
granoblaslic texture.

Quartzile near Nellie

Sees, 29, 32, T, 7 S,,

Outcrop area approx. 1

Roof pendant, mostly quartzite, in granitic rocks, Litho-

Hamilton 56:7, pi. 1.

Lake

R. 25 E., MD., 5 mi.
NW. o( Huntington
Lake.

square mi.

logy of the quartzite: white, gray, pink, medium grained.
Has minor feldspar, biotite, zircon.

Quartzite near Twin

Sees. 20, 29, T. 7 S.,

Quartzite body 8 ft.

Associated with limestone in roof pendant, Lithology of

Chesterman 42:252

Lakes

R. 26 E., MD., ap-

wide, strike length
100 f^t.

the quartzite: granoblastic texture. Quartz, 60%/ feld-

prox. 3 mi. N. of

spar, 30%; also sphene, biotite, zircon, epidote, mag-

Huntington Lake.

netite.

Quartzite m Western

E. partT. 11 S.^R. 23E.
to NE. part T. 12 S.,

Quartzite layers from

Numerous lenticular bodies of quartzite associated with a

Macdonald 41:220

Sierra Nevada

less than 1 in. to 40

great thickness of mica schist. Lithology of the quartzite:
light gray to dark bluish gray, granoblastic texture, av.

R. 24 E., MD, nr.

or 50 ft. thick. Beds

Watts Valley,

lens out within short
distance

grain size 0.1 mm. to 1 mm. No pure quartzite reported.
Contains feldspar, biotite. Some specimens contain
hornblende, diopside, augite, clinozoisite, epidote.

Triassic (?)

Strip From SE. partT. 15

Quartzite masses as much

Lies on Lemon Cove Schist. Overlain by Three Rivers

Durrelt 40:13, 32, map 1, 43:158,

Homer Quartzite of

S., R. 26 E., tocen, T.

as several hundred ft.

Schist. Quartzite occurs as a) lenticular masses consisting

pi. 3.

Kaweah Series

17 S., R. 28 E,, MD,,

thick, strike length 1-

of thin, alternating beds of quartzite and quartz schist

Dry Creek

N. and NE. of Lemon
Cove along Dry
Creek.

2 mi., in max. thick-
ness of 7,000 ft.

that are separated by masses of mica schist and phyllite;
b) masses composed of quartz-rich bands up to 3 in.
thick sepdrated by sharp partings of graphitic or qufrtz-
itic material. The quartzite: quartz, 85% or more; mus-
covite, biotite, graphite; other minerals infrequent-

Paleozoic

T, 1 N., R. 15E., toT. 3

Minor quartzite layers

Lithology of quartzite in SE. cor. T. 1 N., R. 15 E.. MD.:
Fine grained, quartz 90%, micaceous, not much feldspar.

Clark 54 6, Eric 55:8;

Hart 59:12.

Quartzite in Calaveras

N., R. 14 E., MD., in

in schist, locally form-

Fm.

Sierra Nevada foot-

ing units 3-25 ft. thick.

Angels Camp to

hills.

Sonora

Turnback Creek

E. part Sec 25, E. part
Sec. 36, T. 1 N., R.
15 E., NW. Vi See.

Quartzite-bearing units

Metachert associated with carbonate rocks and schist. Lith-

Hart 59:12, pL 2.

up to 150 ft. thick.

ology: crenulated beds 1-2 in. thick separated by phyl-

litic schist and forming thick units. Composed of finely

30 T. 1 N, R. 16 E.,
MD., approx. 10 mi.

crystalline quartz, 90%; mica, pyrite.

SE. of Sonora in bed

of Turnback Creek.

Quartzite in Kernville

T. 27 S,, R. 33 E,, MD.

Quartzite outcrops sev-

Roof pendant consisting of Kernville Series in tightly folded

Miller 40:350, pi. 2,

Series

and to SE., E. and SE.

eral hundred ft. wide,

anticline with thick axial zone of metavolcanic rocks

Bodfish

of Bodfish,

several tens of mi.
long.

flanked by small, thin-bedded layers of quartzite that
grades outward into marble.

Calienle Creek

Sees. 23, 26, 27, T. 30
S., R. 32 E., MD„ 12

Quartzite beds a few ft.

Subordinate quartzite beds in schist, total apparent thick-

Dibblee 53:15, pi. 1,

thick, outcrop length

ness, 6000 ft. Lithology of the quartzite: light-gray to

Mi.E. of BenainDevil

up to 1 mi

bluish-gray, fine-grained, granoblastic aggregate of

Canyon area of Cal-

quartz, albitc, zoisite, hornblende, muscovite, scheelite,

iente Creek.

graphite.

Dome Land

SW. part T. 22 S., R. 34
E., MD., approx. 30
mi. W. of Little Lake,
NW of Dome Land,

Steeply dipping quartz-
ite-bearing mctasedi-
ments 5000-7000 ft.

thick.

Phyllite in E. half of outcrop, quartzite in W. half. Poorly
bedded, white, "fishcyc" quartzite forming bold out-
crops.

Miller 40:351, pi. 2

Kernville

See. 28, T. 25 S., R. 33
E.,MD., 7'/2mi, N. of
Isabella (new loca.
lion).

Isolated outcrops up to
500 ft. long, 1 mi.
wide of quartzite as-
socialed \vith other
metamorphic rocks.

Roof pendant composed of quartzite, schist, phyllite, lime-
stone, that has been intruded by granodiorite, by alas-
kite, and faulted. Lithology of the quartzite: light yellow,
thin bedded, usually intcrbcddcd with phyllite. Medium
sized, rounded or angular grains cemented by botryoidal,
cryptocrystallinc chalcedony (?). Has feldspar crystals.

Prout 40:391.

1966

QUARTZITE

SIERRA NEVADA-Continued

Asc

M«p

Formation (group)

No.

Locality

Location

Size

Geology

Remarks and icfcrcnccs

Monolith

Sec. 14, T. 32 S., R. 33

Impure quartzite several

Roof penddnt containing limestone, quartzite and some

Material of 85% SiOi content

E., MD., approx. 2 mi.
NW of Monolith.

hundred ft. thick.

schist. Lithology of the quartzite: brown and dark gray,

quarried by Monolith Portland

strike length at least

shattered, iron-stained quartzite with schist inclusion

Cement Co. for use in mfg. of

Vq mi.

and cut by stringers of pegmatite and granitic material.
Contains 5-10% biolite; diso feldspar, chlorite, musco-
vitc.SiO!, 70-90%.

Portland cement, Herein.

Rockhouse Basin

T. 23S., R. 36E.,andT.
24 S., R. 36 E., MD.,
approx. 10 mi. W. of
Little Lake, E. and SE.
of Rockhouse Basin.

Phyllite, apparent thick-
ness 15,000 ft. with
subordinate quartzite.

White to gray, "fine-bedded" quartzite.

Miller 40:351.

Sirretta Peak

T. 22 S., R. 33 E., and

3 outcrops, total area

Seplal-like inclusions in granite "composed entirely of

Miller 40:351, pi. 2.

T. 23S.,R.33E.,MD.,

several square mi.

quartzite and its variants".

N. and W. of Sirretta
Peak.

Relief Quattzite of

a)Secs.10, 11,T. 18N.,

Scattered outcrops of

Lies on Kanaka Fm. Overlain by Cape Horn Slate. Mica

Carlson 56:241, pi. 8; Ferguson

Calaveras Group

R. IDE., MD., SW. of

siliceous sediments V4-

schist and schistose quartzite with muscovite partings.

32:12, pi. 1.

Allegfiany

Minnesota Flat. b)Sec.
3, T. 18 N, R. 10 E.,
MD., W. of Chips
Flat, c) Sec. 4, T. 18
N, R. lOE, Sec. 33,
T. 19 N., R. 10 E.,
MD., nr. French Ra-
vine, d)Secs. 29, 32,
T. 19 N., R. 10 E.,
MD., nr. Oreaon
Creek, e) Sees. 4, 5,
T. 18 N,, R. 10 E.,
MD., nr. Rapps Ra-
vine.

V2 mi. wide, up to 1
mi. long.

Quartzite is dark and fine grained

Dutch Flat to Relief

Strip from Sec. 34 T. 16
N., R. IDE. to Sec. 4,

Quartzite-bearing sedi-

Very fine grained quartzite alternating with streaks of

Lindgren 00:2.

ments, outcrop 1 mi.

siliceous clay slate.

T. 17 N., R. 10 E„

by 10 mi.

MD.

Quartzite in Shoo Fly

NW.-trendins strip

Quartzite-bearing sedi-

Lies on Taylor Fm. (metavolcanic). Overlain by Peale Fm.

Diller 08:23; Lydon 60.

Fm. of Calaveras

through Sees. 10, 15,

ments approx. 6800

Slate, lower part; quartzite, upper part. Thin beds of

Group

T. 25N,,R. 9E., MD.

ft. thick.

gray, somewhat slaty, indistinctly schistose quartzite with

Indian Falls

occasional lentils of limestone.

Quartzite in Grizzly Fm.

Sec. 13, T. 25N., R. 10

Shale (400 ft. thick out-
crop length 6 mi.; con-

Lies on metarhyolite. Overlain by Montgomery Limestone.

Dillcr 08:14-16; Lydon 60.

Grizzly Peak

E., to Sec. 34, T. 26

Gray, thtn-bedded quartzite interstratlfied with shale.

N, R. 10E.,MD., SE.

tains quartzite beds 5-

of Taylorsville on

20 ft. thick; strike

Grizzly Mtn.

length comparatively
short.

100

Silurian

NE. partT. 25N.,R. 10

Slate and thin-bedded

Lies unconformably on Montgomery Limestone; upper side

Diller08;17-19j Lydon 60.

Quartzite in Taylorsvillc

E., and adjoining part

sandstone 1800 ft.

is in contact with Taylor Fm. (metavolcanic) and granitic

Frr.

T. 26 N R. 10 E,,
MD. on Grizzly Peak

thick, outcrop length

rock. Has weW defined beds of light colored quartzite

Taylorsville

6 mi., with subordi-

near the middle.

nr. Taylorsvillc.

nate quartzite.

CASCADE RANGE

101

Paleozoic

Ouartzite-bearmg
metasediments
Yellow Butte

Sec. 34, T. 43 N., R. 4
W., MD., at Yellow
Butte.

Outcrop dr^a approx.
1/2 square mi.; mainly
quartzite.

Fault block forming bedrock island in Pleistocene and
Recent lavas. Lithology of the quartzite: pale bluish
white; in places, finely banded gray and black. Dense,
almost porcelaneous. Probably metachert in part.

Williams 49:14.

California Division' of Mines and Geology
KLAMATH MOUNTAINS

Bull. 187

Map
No.

Formation (group)
Locality

Location

Size

Geolosy

Remarks and references

102

Triassic and Paleozoic
Chanchelulla Fm.
Chanchelulla Peak

SW. partT. 31 N., R. 10
NX/.^MD., on slopes of
Chanchelulla Peak.

Recrystallized chert more
than 5,000 ft. thick.

Massive or platy recrystallized chert intcrbedded with
slate, quartzite, and other metasediments.

Hinds 32:392; 33:85; Irwin 60:
21.

103

Helena

T. 34 N., R. 11 W.; T.

34 N., R. 12 W.; T.

35 N., R. 12 W.; T.
36N.,R. 12W.,MD.,
north of Helena.

Recrystallized chert and
slate 2,000-4,000 ft.
thick.

Recrystallized chert makes up 80% of section. One small
outcrop of quartzite. Lithology of recrystallized chert;
microcrystalline quartz and mica. Lithology of quartzite;
gray, medium grained, composed of quartz grains with a
few % feldspar, a little chert.

Cox 56; Irwin 60:22, 23.

104

Qudrtzite-bearins
metasedi merits
Marble Mtns.

T. 43N., R. 12W., MD.,

in Marble Mtns.

Quartzite included in
section more than 10,-
000 ft. thick.

Quartzite and marble associated with amphibolite and
chloritic schists.

Irwin 60:24.

105

Klamath River

T. 46 N., R. 7 W., MD.,
along Klamath River.

Metasediments, includ-
ing quartzite.

Argillites, phyllites, quartzitic slates, graphitic slaty schists,
very fine-grained black schists, quartzites, talcose schists,
pyroxene-hornblende schists limestone, marble.

Avenll 31:9; Irwin 60:24.

106

Silurian

Quartzite-bearing
metasediments
Yreka

T. 44N„R.6W.,T. 44
N., R. 7W.,T. 45N.,
R. 7 W., MD., Yreka
to Grenada.

Alternating bands sev-
eral ft. wide of quartz-
ite and schist or slate.

Lithology of the quartzite: whjte, massive, apparently pure,
recrystallized, fine grained.

Averill 31:9; Irwin 60:16; Wil-
liams 49:14, 15.

107

Pre-Silurian

Quartzite in Abrams Fm.
CoFfec Creek

T. 37N., R. 9W., T. 38
N., R. 9 W., MD., in
upper Coffee Creek

Minor quartzite in sec-
tion 1,000 ft. thick.

Schist with a minor proportion of micaceous quartzite, pure
quartzite, meta-conglomerate, marble. In places quartzite
predominates and forms vein-like outcrops of very glassy
white or dark quartzite.

Gay 49; Irwin 60:19; Hershey
01:226.

108

Scott Valley

A) T. 41 N., R. 9 W.;
B)T. 43 N., R. 8 W.;
C)T. 43 N., R. 9W.;
D)T. 44 N., R. 8 W.,
MD,, in Scott Valley.

Quartzite layers up to 1
in. thick in a great
thickness of metasedi-
ments.

Schist with subordinate layers of white quartzite.

Averill 31:9; Irwin 60:18.

109

Seiad Creek

NW. part T. 46 N., R.
11 W.;SW. partT.47
N., R. 11 W., MD.,
near Seiad Creek.

Schist with subordinate
quartzite.

Thin bands of nearly pure quartzite.

Irwin 60:18; Wells 49:23.

110

Stewart Fork

T. 35N.,R. 9W.;T. 36
N., R. 9 W., MD.,
near Stewart Fork of
Trinity River.

Schist and subordinate
quartzite 2,500 ft.
thick.

Alternating layers of schist and quartzite.

Hinds 33:81; Irwin 60:19.

A 66134—650 3-66 3,500

printed in California office of state printing

BULLETIN 187
PLATE 1

BOOKS REQUESTED BY ANOTHER BORROWER
ARE SUBJECT TO IMMEDIATE RECALL

JUN 30 ^983

P^^SSCILIBRARV

JAN 07 1987 X \
DEC 29 ]986

'"'^^SSC/LIBRARv

GEO

scl

'JNIVEKSITY OF CALIFORNIA
DAV13

LIBRARY, UNIVERSITY OF CALIFORNIA, DAVIS

Book Slip-Series 458

1975

I C^'"-^ ""-f .(_-'

iC^V

STATE OF CALIFORNIA

THE RESOURCES AGENCV

DEPARTMENT OF CONSERVATION

# .4

GEOLOGIC MAP AND SECTIONS OF THE LAKEVIEW QUARTZITE DEPOSIT,

INYO COUNTY, CALIFORNIA

William E. Ver Planck

GEOLOGY ANO TOPOGRAPHY COMPILED BY WILLIAM E. VER PLANCK 1958-1959

100

!00

300 400

CONTOUR INTERVAL '0 FEET
ELEVATION OF STATION A ASSUMED TO BE 4200 F E E T

1966

CORRELATIVE EXPLANATION
Geologic Map and Section B-B' Section A-A

I I ' ""- —

A Dumps ond I

Alluv-um onO 1

I ] Wh.re dolomrle un,r. mclua^nQ pole gro, i.emol.lic

I uoat' mossive uml ot high-punly Quorriile

I ,; ■:■■'■;■] Medium-qfoy guorliilei guorime "ilh dorK sireoks,

1 : :l ood piQly, block, pynle- beoring quorliile

I : , : , ■-:-| Moss>ve quoiime *irh dissetninoled ifon o..de gtoms;

CD-

[Z]'

k quailiile *ilti pyi

SYMBOLS

Doihed wfieri

Vedicol lolioli

I and verticol

LOCATION MKP

Slr>ke and dip ol beds

STATE OF CALIFORNIA

THE RESOURCES AGENCY

DEPARTMENT OF COriSERVATIQN

BULLETIN 187
PLATE 3

gUAHTZlTK MOUNTAIN AND VICINITY SHOWING ORIKNTATION OF THE AREAS AND
MAJOR STRUCTURAL ELEMENTS DISCUSSED IN THE TEXT

M M M H H t

SCALE m FEET

Geology by Oliver E. Bowen and William E. Ver Planck

19:5

GO'ill

STATE OF CALIFORNIA

THE RESOURCES AGENCY

DEPARTMENT OF CONSERVATION

'..y\J

m^cz:i^ — "^^ —

. Cont&ct
OV'T. DOCS. - UEt ttfiXfttif t\ tu^ approximaUty heattd.
jlinffnfinnnf <*r inj'trred)

Fault
Da$h€d ivhtrt approximaUij/ located
U, uTtthnvm tidt; D, dowttthrotcn tidt

SYMBOLS

Strike and dip of deavage

Strike of vertical deavage

Striki! anil dip of bedding and deavage

Strike aod dip of beds

Strike and dip of overturned beds

Fault, showing relative
movement

Thrust fault

(Barbs on upper plate; dashed wher

approximately located)

Strike of vertical beds

Axis of aniidine

Axis of syndine

EXPLANATION

"1 AUutium. Locally include* artificial fill.

' '''I'-T alluvium, fanglomerale, loeallu cemnttrd to hard breccia bv
Ooat •niicke. Locally ituludet artificial fill.

STRUCTURE SECTIONS

t-4500'

EAST END
FAULT RAILROAD

' 6a GRADE FAULT

'^■'1 L 3500'

4000' -
3500'^

QUARRY 12
KLONDIKE 7 „, THRUST FAULT
FAULT ZONE ^-^-^-^^TT'^^^^^^'^J^lL

3000--
2500-

W-/^;|

QUARRY 12
IHRUST FAULT

("iiic rocks, chirflv medium- and coa'se-uramcd triolUt Quarti
"inzonUe; includu aplite and pegmalHe.

SIDEWINDER VOLCANIC SERIES

Black to dark-i/ray latilr, lighl-Qray rhyolile and docile.

4000- H SPABKHULE HILL

MACKS PEAK
THRUST FAULT

QUARTZITE MOUNTAIN

THRUST FAULT

SIDEWINDER VOLCANIC SERIES

lilatk to dark-gtay latiU, lighl-grav rhi/oUu and doeitt.

QUARTZITE MOUNTAIN

4000' H SPARRHULE MILL

ORO GRANDE SERIES
MAP AREAS I THROUGH VI

Dark-brovm to blaek'ictalhfring quarlsilt brteeia, dark qiuirli-mico
lehigt and Ihin^tddtd gnmiBh cak-»ilieaie Iwrnfth (9); hutr dark

?'uaTlt-miea »ehiat and hornfeU {93): bltit-gray, medium rri/glaUinf
imetlom (9t>] ; middU dark quarU-mieo *thiiiC andhomfrli (9c),'
toicer btur-grav to off-whilt. medium eryntallinr dolomite (9a). up-
ptr dark quarlt-mica tehitl and hornfeU (9e),' upjitr blur-gray lo
off-white medium- eryttalline datomitr with minor tchut (&ch) (91)-

Vnjier eommercial quarl:ilt~

', evtii-Draintd. mtdium-rryftal-

Prineipal »ehi»l— black, tevtrelj/ crumpled guarli-mica aehitt (6a);
blue-gray lo light-broum-uieathering Ihnatone and dolomtlie Ume-
Mtont, thin and commonly lenticular l6b);off-v)hiUquartiile (6c},

n-grained, medium'trryilal-

^^ """

i^uamite-sehigt tramition tinit— black, grtenish-black and dark-bro
-' «( and mieaeeout quartrtte; minor calo-silieale homftU.

^~.

nfipol carbonalt—bWe-gray. mtdxam-eryttalline HmenUmi (3a);
htown-wtatheting, off-whiU. medium-eryslaUint dolomite 1 3b);
acbUt (sch).

LoiceTMehial-hornfrU—grren.brnwn.and black, tbin-brddedfchUI, eale-
nlteaU homftU and micaceou* qitorlzUe.

GEOLOGIC MAP OF QUARTZITE MOUNTAIN AND VICINITY NEAR ORO GRANDE,

SAN BERNARDINO COUNTY, CALIFORNIA

Geology by Oliver E, Bowen and William E. Ver Planck

1000

I i-i M t-i \-n=

1960

2000 3000

5000 6000

SCALE IN FEEr

CONTOUR INTERVAL 20 FEET

DATUM IS MEAN SEA LEVEL

>^AP AREA Vll - MACKS PEAK VICINITY

QUARRY 12 PLATE

Dark-brown to black uMtt, thinly laminated.

Matiiee, blue-gray, mrdium-crytilalline t\

PLATE SOUTH OF MACKS PEAK

Dark-brouin to black tehisl, thinly laminalfd.

MACKS PEAK PLATE

fffi

::::

PLATE WEST OF QUARRY IZ

Upper commercial quartrile—maaaive, eten-grained, medtum-cryetal'
linf, off-white quarftite. Lithologtcally indiKlinguiihablf from the
lower quarliilc.

ASaMive to bricciated hluf-gray, medium-crystaltine limrslone, man-
negian in pari.

PLATE AT NORTH END OF CENTRAL RIDGE

Lowermont dolomite -vihiU. rmMriee, medium- to eoarae-eryslalUnf
dohmitr, locally serpenlinie.

NOTE LINE PATTERNS IDENTIFY MAP AREAS

MAP AREA VIII
LOWER ORO GRANDE CANYON

M,ueive, off-whilf. Qiiartsilr .

Blue-graij lo white, crgsialtint lime»tone, dolomilie in pari.

!:■ dark-brown guarii-mica oehitt with minor limestone, horn-
!, quartsile.

"^ Hlue-gray, medium-cryalallint timeatone.

iilack to dark-brouin quarti-miea schist ; few thin lentes of lime»tone 0%),
qaartzite, homfelx

Mauier, off-u>hile quariaU, joinii stained by iron oxide; utather*
rutl-colortd.

Dark-brown to black quarti-miea tchitt; frw thin len*e» of lime*tone,
quart titt, horn felt.

MAP AREA IX
SHAY - KLONDIKE BLOCK

Gttm calc-eitteou homftU and black quarlt'mica schitt urilh onr Ihin
lens of btue~gray erytlalline limetlone (Is).

/)<)rk<brou»i lo black euartfmica Kkiel teith thin ten* of grten horn-
fell and gray or lifhl-ttrovn doUmile (dol).

Btuf-graif to whiU erysiaUine dolomite (W. 8 l);lighlriiraveryilallitu

-_-H)H^_-£3 limetlone OX B 2); lensttof tchiflandquaruile IIKB 3).

\r^=;) Lijhi-grav to browniih-gray. mediunt-i/rainrd guattt-feldtpar-miea
gnei»» and schist probably derited by granititalion of ihaU.

MAP AREA X - SPARKHULE HILL

l/iMHiM, mfdium-crystalline limettone, light blue-groy grading to
block; off-white, broiott-aifalhering dolomite (dol).

° a

CO ;i °

BULLETIN 187
PLATE 1

THIS BOOK IS DUE ON THE LAST DATE
STAMPED BELOW

BOOKS REQUESTED BY ANOTHER BORROWER
ARE SUBJECT TO IMMEDIATE RECALL

JIJN 30 ^983

PHYSSCILIBRARV

JAN 07 1987
DfC 29 1986

P*^^S SCI LIBRARY

GEO

UNIVERSITY OF CALIFORNIA
DAV13

LIBRARY, UNIVERSITY OF CALIFORNIA, DAVIS

Book Slip-Scries 458

■ 1975