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FAIRBANKS, Alaska--New Federal Building, 101 

Twelfth Ave. 
Triple Divide Peak Quadrangle, 

Fresno and Tulare Counties, CaliforniaAnalytic Data 

By THOMAS W. SISSON 

Modal and chemical analyses of granitic rocks of the 

Triple Divide Peak quadrangle, California 

U.S. GEOLOGICAL SURVEY BULLETIN 2026 
U.S. DEPARTMENT OF THE INTERIOR 

MANUEL LUJAN, JR., Secretary 

U.S. GEOLOGICAL SURVEY 

Dallas L. Peck, Director 

Any use of trade, product, or firm names 

in this publication is for descriptive purposes only 

and does not imply endorsement by the U.S. Government 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1992 

For sale by 

Book and Open-File Report Sales 

U.S. Geological Survey 

Federal Center, Box 25286 

Denver, CO 80225 

Library of Congress Cataloging in Publication Data 

Sisson, Thomas W. 

Triple Divide Peak quadrangle, Fresno and Tulare counties, California : 

analytic data I by Thomas W. Sisson. 

p. cm.-(U.S. Geological Survey bulletin ; 2026) 

Includes bibliographical references. 

Supt. of Docs. no.: I 19.3:2026 

1. Granite-California-Fresno County-Composition. 2. GraniteCalifornia-Tulare County-Composition. I. Title. II. Series. 

QE75.B9 no. 2026 

[QE462.G7] 

557.3 s-dc20 

[552'.3] 92-23143 

CIP 
CONTENTS 

Abstract 1 

Introduction 1 

General geology 1 

Sampling and analytic methods 4 

Sequoia Intrusive Suite 4 

Mitchell Intrusive Suite 5 

Mount Whitney Intrusive Suite 5 

Other granitic rocks 5 

Average plutonic rock composition 6 

Fractionation modeling 7 

References cited 8 

FIGURES 

1. Index map showing location of Triple Divide Peak and other quadrangles cited in 

report 1 

2. Generalized geologic map of the Triple Divide Peak 15-minute quadrangle showing distribution of rock units 2 

3. Generalized geologic map of Triple Divide Peak 15-minute quadrangle showing 

locations of samples analyzed for chemistry, modal mineral abundances, or specific gravity 11 

4. Modal plots on Q-A-P diagrams of Triple Divide Peak quadrangle granitoids 

showing Mitchell Intrusive Suite, Mount Whitney Intrusive Suite, light-colored 

granitic rocks, mafic intrusive rocks, and miscellaneous granitic rocks 12 

5. Average modal abundances on Q-A-P diagram 13 

TABLES 

1-4. Chemical analyses and CIPVV norms of rocks from: 

1. Mitchell Intrusive Suite 14 

2. Sequoia Intrusive Suite 15 

3. Miscellaneous plutons 15 

4. Mafic intrusions near Hamilton Lake 16 

5. Areal size of geologic map units 16 

6. Modes of plutonic rocks H; 

7. Average chemical composition of plutonic rocks 18 

8. Mineral-liquid modeling parameters 18 

Contents Ill 

Triple Divide Peak Quadrangle, Fresno and Tulare 

Counties, California-Analytic Data 

By THOMAS W. SISSON 

ABSTRACT 

The Triple Divide Peak quadrangle encompasses 620 

km2 of the central Sierra Nevada, including the headwaters of 

the Kings, Kern, and Kaweah Rivers. Cretaceous granitic rocks 

make up most of the bedrock of the quadrangle. A total of 11 

percent of the quadrangle is composed of rocks belonging to 

the Sequoia Intrusive Suite, 40 percent by rocks of the Mitchell Intrusive Suite, and 27 percent by rocks of the Mount 

Whitney Intrusive Suite. 

The 80 modal and 42 chemical analyses in this report are 

of typical granitic rocks and indicate that the average plutonic 

rock in the quadrangle contains 66.5 wt. percent Si02 and 

3.4 wt. percent K20, estimates similar to those for the Earth's 

upper continental crust. Fractionation modeling indicates that 

der!vation of the average composition from the average mafic 

rock requires separation of 45-48 percent (by mass) of earlyforming crystals. If accumulated together, these minerals 

would produce a cumulate body recognizable by geophysical 

methods. The evidence for such a body is lacking, and it is 

concluded that significant crustal fusion has accompanied 

crystal fractionation to produce the granitic rocks of the quadrangle. This report supplements the geologic quadrangle map 

by documenting analyses and sample locations. 

INTRODUCTION 

The Triple Divide Peak quadrangle encompasses 

about 620 km2 of mountainous terrain of the central Sierra 

Nevada in Fresno and Tulare Counties, California. Elevations range from 975 m at the southwest comer of the 

quadrangle up to 4, 196 m at the summit of Black Kaweah 

in the southeast comer. The quadrangle is named for Triple Divide Peak, which lies in the eastern part, and separates the headwaters of the Kern, Kaweah, and southern 

Kings Rivers (fig. 1). The quadrangle also contains the 

Great Western Divide, a chain of high peaks lying well to 

the west of the Sierran crest, separating the south-flowing 

Manuscript approved for publication, March 13, 1992. 

Kern from the west-flowing Kaweah River. The quadrangle lies within Kings Canyon and Sequoia National Parks, 

except for a small area in the northwestern comer within 

Sequoia National Forest. 

Granitic rocks of the Sierra Nevada batholith comprise more than 98 percent of the quadrangle. This report 

supplements the geologic map of the Triple Divide Peak 

quadrangle (Moore and Sisson, 1987a), by providing modal and chemical analyses of granitic rock samples. 

GENERAL GEOLOGY 

The oldest rocks of the quadrangle (fig. 2) are 

metamorphosed sedimentary and volcanic rocks. Both are 

TEHIPITE 

DOME 

QUAD. 

118°45' 

South P- '"'--, :or.f. __ ........._ ______ . 

/- '-----f(ings River r-' 

MOUNT 

PINCHOT 

QUADRANGLE ',l MARION PEAK QUADRANGLE 

36°45' 1-----+---+-------;==;::;-;:;=~~------r-------:= - ~ .fRESNO SOUNTY _ ____r----

SEQUOIA j TULARE COUNTY 

NATIONAL j TRIPLE DIVIDE PEAK \ QUADRANGLE 

FOREST ,/ QUADRANGLE l 

________ _,--, __ J..:-, ' l __ /-~ ' . , ',\ Mount KINGS CANYON r 

KAWEAH 

QUAD. 

J(Sillim~n NATIONAL PARK ( 

..__ __ / \_.---"'- I 

Lodgepole SEQUOI:,;.\ ~«_- /Triple 

Campground NATIONAL--\ 0'~/ Divide ~ 

'f PARK . ',~--~- I Peak ~ Ham1lton;:: ; 

MINERAL KING 

QUADRANGLE 

Lake f5 /"' \ty~ 

!;; ( ',~ Black 1/ ~Kaweah 

/ "1!. ',()~ f- \ o<> '--..."~Ire 

~ (' 7?.0 "?;~ Ql ( :Po ~ 

Figure 1. Index map showing location of Triple Divide Peak and 

other quadrangles cited in report. 

General Geology 
118"45' 

36"45' 

J"Rms 

Kgf 

KJdc 

Kmf 

Kcc 

0 2 

Kp 

Ks 

' Kmc 

~ 

Kmf 

Kmc 

'P 

3 4 5 6 7 8 KILOMETERS 

Figure 2. Generalized geologic map of the Triple Divide Peak quadrangle (modified from Moore and Sisson, 1987a). 

2 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 

118"30' 
EXPLANATION 

GRANITIC ROCKS 

Dark-colored 

rocks 

Granodiorite of 

Sugarloaf 

Mitchell 

~ Peak 

Granodiorite, 

fine-grained facies 

~ 

~ 

Mitchell Peak 

Granodiorite, 

coarse-grained facies 

Granodiorite of 

Lookout Peak 

8 

Granodiorite of 

Castle Creek 

Diorite 

and gabbro 

~ Granodiorite of 

Lightning Creek 

Medium-colored 

rocks 

Granodiorite of 

Chagoopa 

Light-colored rocks 

EJ 

Po1h~? of Blac aweah 

0 

Granite of 

Tamarack Lake 

~ Granite of 

Eagle Scout Peak 

~ 

~~ 

Granites of 

Triple Divide Peak 

and Coyote Pass 

EJ 

Granite of 

Mount Kaweah 

//~G 

~ / Granite of 

/ ~~ Weaver Lake // ( 

/ Granodiorite of 1 

/ Clover Creek 1 

/ I 

/ // Bl ~ 

~ 

/ / Granite of 

/ Big Meadows 

Giant Forest 

Granodiorite 

Figure 2.-Continued 

GRANITIC ROCKS- continued 

I KJem I 

Quartz Diorite of 

Empire Mountain 

~ 

Sheared 

Granodiorite 

~ Diorite 

and gabbro 

0 

Granite of 

Lion Rock 

a 

Granite of 

Lodgepole 

Campground 

8 

Granite of 

Dome Creek 

MET AM ORPHIC ROCKS 

I JRms I 

Metasediments 

~ Mafic and 

intermediate 

metavolcanics 

Contact 

Fault 

I JRmr I 

Metarhyolite 

~ 

0 

IZlU 

:::::>- QIZl 

i:lliZl 

u~ <:::::> 

~ .... ~ 

u 

General Geology 3 
associated with small bodies of sheared, schistose intrusive rocks. The metamorphic rocks and schistose granites 

are cut by fine-grained dikes of hornblende gabbro and diorite that may be members of the Late Jurassic Independence dike swarm. 

Large masses of granodioritic and granitic magma intruded the region during the Cretaceous. These intrusive 

masses are present as discrete bodies (plutons) with sharp 

boundaries and are internally almost uniform in texture, 

mineralogy, and chemistry. Individual plutons form the 

principal map units of the quadrangle (fig. 2). Some plutons are nested one within another, with the inner plutons 

generally being younger and lighter colored than the outer 

plutons. Such an arrangement suggests a related, cogenetic 

origin for these plutons. Parts of three such intrusive suites 

are exposed in the Triple Divide Peak quadrangle (Moore 

and Sisson, 1987a). Eleven percent of the quadrangle is 

made up of rocks belonging to the Sequoia Intrusive Suite, 

40 percent by rocks of the Mitchell Intrusive Suite, and 27 

percent by rocks of the Mount Whitney Intrusive Suite. 

SAMPLING AND ANALYTIC METHODS 

Eighty samples of plutonic rocks were analyzed for 

their modal mineralogy and specific gravity (table 6). Forty-two samples were analyzed for their major-element 

chemistry (tables 1-4). Locations of chemically or modally 

analyzed samples are shown in figure 3. Modal analyses 

were performed by counting over 1 ,000 points on stained 

rock slabs (Norman, 1974). Data are· reported in terms of 

volume percent quartz, plagioclase, K-feldspar, and mafic 

minerals (chiefly biotite, hornblende, and magnetite) and 

are presented graphically in figure 4. The rocks are classified using the modal limits of Streckeisen and others 

(1973) and average or estimated modal abundances (fig. 

5). Older chemical analyses (with field numbers prefixed 

6-) were determined by the rapid method of Shapiro and 

Brannock (1962). All other analyses were made by standard X-ray fluorescence techniques, with Na20 and in some 

cases K20 determined by flame photometry. Ferrous iron, 

C02, H20+, and H20- were determined by standard wet 

chemical methods. Specific gravity was determined by 

beam balance weighing of hand samples in air and water. 

Representative samples were collected of most map 

units, but no rigorous attempt was made to establish a uniform sampling distribution (fig. 3). Instead, sampling was 

concentrated on plutons with distinctive and informative 

field relations and in areas with particularly unweathered 

rocks. 

SEQUOIA INTRUSIVE SUITE 

Ross (1958) recognized a sequence of intrusions starting with the Giant Forest Granodiorite, followed by the 

granite of Big Meadows and the granodiorite of Clover 

Creek, and ending with the granite of Weaver Lake. The 

inward-younging, grossly concentric arrangement of these 

plutons led him to propose that they were genetically related. Uranium-lead ages from zircon and sphene for samples from these plutons (Chen and Moore, 1982) fall in a 

narrow range from 97 to 102 Ma and support this interpretation. Modal mineral abundances were not measured on 

samples of the granite of Big Meadows and granodiorite 

of Clover Creek or the granite of Weaver Lake from within the Triple Divide Peak quadrangle. These plutons have 

been classified on the basis of measurements of samples 

from the adjacent Giant Forest quadrangle, as well as on 

modes reported in Ross (1958). 

The Giant Forest Granodiorite is dark, equigranular, 

and medium grained. It contains prominent, subhedral 

crystals of hornblende and biotite. A few hornblende 

grains contain resorbed cores of augite, commonly altered 

to actinolitic amphibole. Honey-brown sphene is an accessory in all samples. Dark mafic inclusions, generally 5-10 

em in size, are particularly abundant in the granodiorite 

and range from three to seven in a square meter. A zone 

up to 1 km thick along the outer border of the Giant Forest Granodiorite contains phenocrysts of K-feldspar. 

The granite of Big Meadows is lighter colored than 

the Giant Forest Granodiorite and, except locally, contains 

far fewer mafic inclusions. Biotite makes up a larger proportion of the mafic minerals, and allanite is present in 

some very light colored samples. The granite of Big 

Meadows contains phenocrysts of K-feldspar chiefly along 

its northeastern margin. A sharp contact has not been 

found separating the porphyritic and nonporphyritic facies. 

Samples of the granite of Big Meadows include both granite and light colored granodiorite in nearly equal proportions. 

The granodiorite of Clover Creek cuts the granite of 

Big Meadows. The granodiorite of Clover Creek is darker 

than the granite of Big Meadows and locally contains variably disaggregated blocks of the granite of Big Meadows. 

Chemical analyses of samples of the granodiorite of Clover Creek show straight-line trends on silica variation diagrams, with end-member compositions corresponding to 

the granite of Big Meadows and an unexposed tonalite. 

Diorite dikes also cut the granite of Big Meadows, but do 

not have compositions appropriate to have produced the 

granodiorite of Clover Creek by assimilation of granite of 

Big Meadows. 

The granite of Weaver Lake is the youngest member 

of the Sequoia Intrusive Suite. It forms a swarm of lightcolored, fine-grained sills that intrude both the granite of 

Big Meadows and of Clover Creek. These sills commonly 

contain small (1 em) phenocrysts of K-feldspar. The latest 

crystallizing areas of the granite of Weaver Lake are 

stocks or plugs of medium-grained, alaskitic granite containing vuggy pegmatitic pods and veins. 

4 Triple_ Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 
MITCHELL INTRUSIVE SUITE 

The rocks of the Mitchell Intrusive Suite dominate 

the geology of the Triple Divide Peak quadrangle. The 

suite lies centered in the middle of the quadrangle (fig. 2), 

covering 40 percent of the total area (250 km2, table 5). 

The suite stretches 60 km by 16 km in maximum length 

and breadth from the southern Marion Peak quadrangle 

(Moore, 1978) to the southern Mineral King quadrangle 

(Moore and Sisson, unpub. mapping). 

The oldest member of the suite is the granodiorite of 

Castle Creek. This intrusion is formed of dark rocks similar to those of the Giant Forest Granodiorite. Two facies 

have been mapped in the Triple Divide Peak quadrangle. 

The westernmost is poor in mafic inclusions and possesses 

a faint layering of the dark minerals. This facies is intruded by dark granodiorite containing abundant mafic inclusions and generally lacking modal layering. A sample of 

the inclusion-bearing facies from the Mineral King quadrangle was dated at 98±2 Ma by the uranium-lead zircon 

method (Busby-Spera, 1983). 

The next younger members of the suite are the 

coarse-grained facies of the Mitchell Peak Granodiorite 

and tlie correlative granodiorite of Lookout Peak. These 

rocks contain phenocrysts of K-feldspar as large as 4 em 

in size. The coarse-grained facies can be subdivided into 

lighter and darker colored members, the darker being similar to the granodiorite of Castle Creek but with K-feldspar 

phenocrysts. The lighter colored member is more voluminous and consists of coarse-grained, porphyritic biotite 

granite, with few mafic inclusions. A sample of the granodiorite of Lookout Peak from the Marion Peak quadrangle 

was dated at 97 Ma by the uranium-lead zircon technique 

(Chen and Moore, 1982). 

Following intrusion of the coarse-grained facies, the 

plutons of the Mitchell Intrusive Suite were arranged in a 

form typical of zoned intrusions and intrusive suites in the 

Sierra Nevada batholith: an outer equigranular dark granodiorite with abundant mafic inclusions intruded core-ward 

by progressively lighter colored porphyritic granodiorites 

and granites with few mafic inclusions. The later intrusion 

of the voluminous fine-grained facies of the Mitchell Peak 

Granodiorite disrupted this general form. 

The fine-grained facies of the Mitchell Peak Granodiorite consists of dark granodiorite with abundant large (10-

50 em) mafic inclusions (6-18/m2). Plagioclase forms the 

most prominent phenocrysts, reaching 4 em in length. 

Most of the hornblende and biotite are groundmass minerals, but some are scattered subhedral phenocrysts. The 

scattered dark phenocrysts in a fine-grained matrix give the 

rock a salt-and-pepper appearance. Augite forms ragged 

cores in some hornblende phenocrysts; most augite grains 

are variably altered to actinolite. Plagioclase phenocrysts 

with a distinctive boxwork or cellular microtexture are 

present in both the host granodiorite and in some mafic 

inclusions. This suggests that these inclusions were sufficiently fluid to mix with some of their host magma. Quartz 

and K-feldspar are found only as groundmass minerals. 

The fine-grained facies magma intruded into the center of the coarse-grained facies, following intrusion of a 

few small stocks of diorite and dikes of fine-grained granodiorite. Many areas of the fine-grained facies are crowded with blocks of the earlier coarse-grained facies. The 

blocks range from meters to hundreds of meters across. 

Many of the smaller blocks now have smooth fluidal outlines, elongate concordant with the foliation of the host 

fine-grained facies and suggesting that the blocks were incompletely solidified when they were engulfed. Ascent of 

the magma parental to the fine-grained facies was probably accompanied by venting of overlying silicic magma 

from the center of the intrusive suite in major volcanic 

eruptions. These could have been triggered by intrusion of 

fresh, primitive magma related to the growth of the adjacent Mount Whitney Intrusive Suite. The fine-grained facies of the Mitchell Peak Granodiorite was dated at 91 Ma 

by the uranium-lead zircon technique (Chen and Moore, 

1982). 

MOUNT WHITNEY INTRUSIVE SUITE 

Parts of two plutons of the giant Mount Whitney Intrusive Suite (Moore, 1987) make up the northeast comer 

of the Triple Divide Peak quadrangle (fig. 2). The older of 

these, the granodiorite of Sugarloaf, is a dark equigranular 

granodiorite with subhedral crystals of hornblende and biotite and abundant mafic inclusions (61m2). Hirt (1989) reports augite cores in some hornblende crystals in samples 

of the granodiorite of Sugarloaf and provides several 

whole-rock chemical and modal analyses. Two uraniumlead zircon analyses of a sample of the granodiorite of 

Sugarloaf from the Marion Peak quadrangle indicate inherited old zircon, but nevertheless constrain the pluton to 

be younger than 88 Ma (Chen and Moore, 1982). The 

granodiorite of Sugarloaf was followed by the Paradise 

Granodiorite, a medium-colored granodiorite with K-feldspar phenocrysts masked by abundant inclusions of hornblende and biotite. Mafic inclusions are rare (<21m2

). 

Uranium-lead zircon ages for samples of the Paradise 

Granodiorite from the Marion Peak quadrangle range from 

83 to 88 Ma (Chen and Moore, 1982). 

. OTHER GRANITIC ROCKS 

Numerous intrusive masses are present that cannot be 

assigned to larger intrusive suites. These generally form 

small to medium-sized plutons either much poorer or 

moderately richer in silica than the large granodiorite 

plutons. 

Other Granitic Rocks 5 
The granite of Lodgepole Campground is sandwiched 

between the Sequoia and Mitchell Intrusive Suites and locally forms a roof over the top of the granodiorite of Castle Creek. Pyrite is present on the surfaces of many joints 

in the granite and has weathered to produce iron oxides 

and, apparently, sulfuric acid. The iron oxides have stained 

the jointed areas red, whereas the sulfuric acid has etched 

minerals in the rock. In extreme cases, the resulting rock 

is cavernously weathered, red, and soft. An analysis of 

such rock (table 3) from the Emerald Lake area shows enrichment in total iron oxide and K20 and strong depletion 

in silica compared to nearby unaltered granite. 

The granite of Lodgepole Campground contains latecrystallizing pegmatitic areas with open cavities. Pegmatitic areas contain the minerals quartz, albitic plagioclase, 

and K-feldspar. Some contain massive magnetite and ironrich biotite, others contain magnetite without biotite. If a 

total pressure of 2 kbar is assumed, conditions near or 

more oxidizing than the nickle-nickle oxide buffer were 

reached at the final stages of consolidation (following calculations in Czamanske and Wones, 1973). Chen and 

Moore (1982) report a discordant U-Pb zircon analysis 

that constrains the granite of Lodgepole Campground as 

older than 115 Ma. 

The granites of Triple Divide Peak and Tamarack 

Lake consist of light-colored granite generally with no 

mafic inclusions. Both of these plutons are only shallowly 

unroofed, with either gently dipping upper contacts or isolated remnants of their former roofs. Both granites are 

poor to very poor in MgO and rich 1n silica (table 3). 

The granites of Coyote Pass and Eagle Scout Peak 

are darker colored than either the granite of Triple Divide 

Peak or Tamarack Lake. Mafic inclusions are present and 

occur in swarms in some areas, but their abundance usually does not exceed 21m2. The granite of Eagle Scout Peak 

contains areas with small (1-2 em) K-feldspar phenocrysts. 

Dark -colored rocks form the slopes rising from 

Hamilton Lakes up to Kaweah Gap, and dark dikes lace 

the granite cliffs both north and south of the lakes (figs. 1, 

2). The dark rocks are rich in hornblende, and the presence of hornblende-plagioclase pegmatites and tiny open 

cavities indicate crystallization with abundant water. The 

fine-grained dikes, sills, and medium-grained stocks have 

the composition of silica-poor andesites, some containing 

olivine in their norms (table 4). Rocks that formed from 

accumulated early crystals are also present. 

The granodiorite of Chagoopa extends into the quadrangle from the southeast (fig. 2) and is the source of thick 

dikes and sills that intrude the granite of Mount Kaweah 

and the metamorphic rocks of the Kaweah Peaks Ridge. A 

few mafic inclusions from this intrusive mass have a distinct and unusual habit. They are very fine grained and 

have bulbous shapes similar to magmatic inclusions in 

volcanic rocks (Bacon, 1986). Altered ferromagnesian 

phenocrysts (augite?) have skeletal forms, suggestive of 

quenching. An analysis of such an inclusion is presented 

in table 3. Most of the mafic inclusions in the granodiorite 

of Chagoopa resemble common Sierran mafic inclusions, 

such as those described by Pabst (1928). 

AVERAGE PLUTONIC ROCK COMPOSITION 

An attempt is here made to estimate the average 

chemical composition of the intrusive rocks in the Triple 

Divide Peak quadrangle. This is done by assigning compositions to the various plutons and then weighting the compositions by the areas of their plutons (table 5). A 

similarly calculated average chemical composition is presented by Moore (1987) for the adjacent Mount Whitney 

quadrangle. 

The assignment of compositions was performed as 

follows: the fine-grained facies of the Mitchell Peak Granodiorite is the average of seven analyses (table 1), the 

coarse-grained facies and the granodiorite of Lookout 

Point are the average of three analyses (table 1), the granodiorite of Castle Creek is the average of two analyses 

(table 1), the Giant Forest Granodiorite and the similar 

granodiorite of Lightning Creek and the Jurassic or Triassic granodiorite are given the average of four Giant Forest 

Granodiorite analyses (table 2), the granodiorite of Clover 

Creek is the average of two analyses (table 2), the granite 

of Big Meadows is given a single analysis (table 2), the 

granite of Weaver Lake is· given the average of two unpublished analyses of samples from the Giant Forest quadrangle, the granite of Tamarack Lake is the average of 

three analyses (table 3), the granites of Eagle Scout Peak 

and Triple Divide Peak and the granodiorite of Chagoopa 

are their single analyses (table 3), the granite of Lodgepole 

Campground is given by the average of three analyses of 

unaltered granite, the mafic plutonic rocks and the Jurassic 

or Triassic diorites and the quartz diorite of Empire Mountain are given the average of six analyses (table 4), the 

granodiorite of Sugarloaf is given by the average of three 

analyses presented by Hirt (1989) and sample 7-27 of 

Moore (1987) with Fe0/Fe0+Fe20 3 in Hirt's samples set 

to the value in sample 7-27, the Paradise Granodiorite is 

given by the average of nine samples from the west side 

of the pluton presented by Hirt (1989) with FeO/FeO+ 

Fe20 3 in Hirt's samples set to the mean of three Paradise 

Granodiorite analyses given by Moore (1987), the granites 

of Lion Rock and Dome Creek are given the analysis of 

the granite of Eagle Scout Peak (table 3), the granite of 

Mount Kaweah is given the analysis presented by Moore 

( 1987) for a sample from the Mount Whitney quadrangle, 

and the granite of Coyote Pass is given the average of 

three unpublished analyses from the adjacent Mineral 

King quadrangle. 

The average granitoid rock for the Triple Divide Peak 

quadrangle is given in table 7. The quadrangle average of 

6 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 
66.5 wt. percent Si02 is markedly lower than that for the 

adjacent Mount Whitney quadrangle on the east (70.6 wt. 

pet. Si02, Moore, 1987) and illustrates the general increase in Si02 content from west to east across the Sierra 

Nevada batholith. The average Triple Divide Peak composition is that of a typical granodiorite. For comparison, an 

estimate of the composition of the bulk upper continental 

crust (Taylor and McLennan, 1985) and the average of 

two estimates of the bulk composition of the Precambrian 

Canadian Shield (in Taylor and McLennan, 1985) are also 

presented. The average Triple Divide Peak granitoid and 

these estimates are similar, indicating that the average upper continental crust is and has been a product of igneous 

processes similar to those that have produced the Sierra 

Nevada batholith. 

FRACTIONATION MODELING 

The rocks of the Triple Divide Peak quadrangle vary 

in chemical composition in a fashion typical of granitoid 

batholiths formed along the margins of continents. As noted above, the average composition is also close to estimates of the bulk composition of the upper continental 

crust. The origin of granitoid batholiths and the upper continental crust are questions of profound importance in geochemistry and igneous petrology. Although addressing 

these questions is well beyond the scope of this report, the 

simple model of fractional crystallization can be examined 

and the implications tested against independent observations. 

Modeling has been performed through the use of a 

computer program developed by T. Juster (1988, written 

commun.) for general crystal-fractionation calculations. 

The procedure began by plotting the average pluton compositions, used above, as oxide variation diagrams against 

MgO. The trends on the variation diagrams were then fit 

by multiple regression of MgO polynomials until equations were obtained that closely matched the oxide-MgO 

trends. In this way, weight percents of all oxides could be 

calculated for any specified MgO content. The calculated 

oxide concentrations are defined by the trends regressed 

through the natural data. For the purposes of fractionation 

modeling, it was assumed that the observed trends represent a spectrum of (now crystallized) liquid compositions. 

The range of observed MgO contents was divided into 10 

or more equally sized intervals, and bulk compositions 

were calculated for the end points of each interval. Synthetic mineral compositions were calculated for each synthetic liquid composition using known or estimated 

mineral-liquid exchange distribution coefficients (table 8). 

Each liquid composition interval was then regressed using 

a variety of petrologically reasonable mineral assemblages 

plus the low-MgO liquid for that interval until an acceptable combination was obtained that matched the highMgO liquid for that interval. The following restnctmns 

were applied: ( 1) the modes of liquid plus crystals must 

sum to 1.000, (2) no assimilation of minerals was allowed, 

(3) no more than two ferro-magnesian silicate minerals 

were allowed in modeling each interval, ( 4) in keeping 

with petrographic evidence, K-feldspar, quartz, and biotite 

were not allowed in any interval in which clinopyroxene 

was employed, and (5) solutions are acceptable if their Q 

statistic equals or exceeds 0.01 and their Chi-squared statistic equals or lies below 11.000. The coarse-grained cumulate rock sample 85S69 (table 4) was excluded from 

the average mafic rock starting composition because it 

clearly does not represent a crystallized liquid. 

Acceptable solutions were obtained for compositions 

ranging from 55 to 66.5 wt. percent Si02 using the assemblage plagioclase+homblende+apatite+titanomagnetite. 

Modeling was continued from 66.5 wt. percent Si02 to 

70.5 wt. percent Si02, after adding biotite and sphene. 

Sixty-six percent Si02 is close to the calculated average 

composition for the quadrangle, and modeling results are 

not reported for more silicic compositions. 

Derivation of the most common plutonic rock composition from the mean mafic rock (-55 wt. pet. Si02 andesite) by fractional crystallization requires separation of 45-

48 percent of the original mass of liquid as cumulate minerals. If these cumulate minerals were entirely separated 

from liquid, the cumulate material would have an aggregate density of -3.09 g/cm3. The approximate density of a 

66 wt. percent Si02 plutonic rock can be estimated as 2. 72 

g/cm3 (Moore and Sisson, 1987b), and from this it is seen 

that the volume of cumulate minerals is approximately 0.7 

of the volume of (now crystallized) derivative 66 wt. percent Si02 liquid. 

A regional gravity and· density study by Oliver and 

others ( 1986) concludes that the exposed plutons of the 

Sierra Nevada maintain their individual density contrasts 

to depths between 8 and 12 km depending on location. If 

the average pluton from the Triple Divide Peak quadrangle 

is uniform in density to a depth of approximately 10 km, 

the fractionation model presented above would require an 

additional 7 km of cumulate material. Bateman and Eaton 

( 1967) present a model cross section for the Sierra Nevada 

in which the crust in the central region is 40 to 55 km 

thick and in which the lower 30 km consists of material 

with compression wave velocity of 6.9 km/s and a bulk 

density of 3.03. The fractionation model would require 

that approximately one-quarter of the crust below the 

batholith consists of cumulates. If the modeling was continued to more silicic compositions, as would be appropriate in the adjacent Mount Whitney quadrangle (Moore, 

1987), the volume of cumulates would be even greater. 

Using a volume fraction of cumulate rocks of 0.25, a cumulate density of 3.09, and a bulk density of 3.03, the 

calculated country rock density of the sub-batholithic crust 

is 3.01 g/cm3. 

Fractionation Modeling 7 
Chen and Moore (1982) calculate that Cretaceous 

plutonism migrated at a rate of 2. 7 mm/yr eastward across 

the batholith. For the combined volumes of cumulate and 

fractionated liquid calculated above, this leads to a magma production rate of 4.6xlo-5 km3

/yrlkm (neglecting the 

density difference between granodiorite liquid and crystalline granodiorite). Integration over the length of the entire 

batholith ( -800 km) would imply a production rate of 

3.7xlo-2 km3/yr. These numbers only apply to the model 

outlined above. 

Peterson and others (1974) present compression wave 

velocity measurements of unweathered cumulate gabbros 

with densities from 2.9 to 3.2 g/cm3. They find that most 

of their measurements lie above 6.9 km/s, in the range 7.4 

to 7.5 km/s. The gabbros that they measured have density 

similar to the model cumulates, so it is likely that any 

pure, sub-batholithic cumulates would have compression 

wave velocities in excess of 7.0 km/s and perhaps as high 

as 7.5 krnls. Bateman and Eaton (1967) found no evidence 

to suggest the presence of a layer with this high seismic 

velocity flooring the batholith. If the fractionation model 

outlined above is correct, then the cumulate rocks must 

occur as small masses heterogeneously dispersed within 

less dense, seismically lower velocity country rocks. 

The absence of large volumes of suitable unfractionated parents and the apparent lack of (geophysically recognized) cumulates are evidence against interpretations 

favoring the production of the common plutonic rocks 

through simple crystal fractionation from the average mafic rocks (-andesite). Considerable crustal fusion must 

have accompanied fractionation of mafic magmas. Major 

element models involving combined crystal fractionation, 

assimilation, and crustal fusion have proven notoriously 

non-unique, and they are not reported here. 

REFERENCES CITED 

Bacon, C.R., 1986, Magmatic inclusions in silicic and intermediate volcanic rocks: Journal of Geophysical Research, v. 91, 

no. B6, p. 6091-6112. 

Bateman, P.C., and Eaton, J.P., 1967, Sierra Nevada batholith: 

Science, v. 158, p. 1407-1417. 

Busby-Spera, C.J., 1983, Paleogeographic reconstruction of a 

submarine volcanic center: geochronology, volcanology, and 

sedimentology of the Mineral King roof pendant, Sierra Nevada, California: Princeton, N.J., Princeton University, 

Ph.D. dissertation, 290 p. 

Chen, J.H., and Moore, J.G., 1982, Uranium-lead isotopic ages 

from the Sierra Nevada batholith, California: Journal of Geophysical Research, v. 87, p. 4761-4784. 

Czamanske, G.K., and Wones, D.R., 1973, Oxidation during 

magmatic differentiation, Finnmarka complex, Oslo area, 

Norway: part 2, the mafic silicates: Journal of Petrology, v. 

14, p. 349-380. 

Hirt, W.R., 1989, The petrological and mineralogical zonation of 

the Mount Whitney Intrusive Suite, eastern Sierra Nevada, 

California. University of California, Santa Barbara, Ph.D. 

thesis. 278 p. 

Moore, J.G., 1978, Geologic map of the Marion Peak quadrangle, Fresno County, California: U.S. Geological Survey Geologic Quadrangle Map GQ-1399. 

__ 1987, Mount Whitney quadrangle, In yo and Tulare Counties, California-analytic data: U.S. Geological Survey Bulletin 1760, 15 p. 

Moore, J.G., and Sisson, T.W., 1987a, Geologic map of the Triple Divide Peak quadrangle, Tulare County, California: U.S. 

Geological Survey Geologic Quadrangle Map GQ-1636. 

__ 1987b, Preliminary geologic map of Sequoia and Kings 

Canyon National Parks, California: U.S. Geological Survey 

Open-File Report 87-651, 14p. 

Norman M.B., 1974, Improved techniques for selective staining 

of feldspar and other minerals using amaranth: U.S. Geological Survey Journal of Research, v. 2, no. 1, p. 73-79. 

Oliver, H.W., Moore, J.G., and Sikora, R.F., 1986, Specific gravity vs. gravity--central Sierra Nevada, California: Eos, v. 67, 

no. 44, p. 1212. 

Pabst, A., 1928, Observations on the inclusions in the granitic 

rocks of the central Sierra Nevada: University of California 

Publications Bulletin of the Department of Geological Sciences, v. 17, p. 325-387. 

Peterson, J.J., Fox, P.J., and Schreiber, E., 1974, Newfoundland 

ophiolites and the geology of the oceanic layer: Nature, v. 

247, p. 194-196. 

Ross, D.C., 1958, Igneous and metamorphic rocks of parts of 

Sequoia and Kings Canyon National Parks, California: California Division of Mines and Geology Special Report 53, 

24p. 

Shapiro, L., and Brannock, W.W., 1962, Rapid analyses of silicate, carbonate, and phosphate rocks: U.S. Geological Survey Bulletin 1144-A, 56 p. 

Streckeisen, A.L., chairman, and others, 1973, Plutonic rocks: 

classification and nomenclature recommended by the International Union of Geological Sciences Subcommission on 

the Systematics of Igneous Rocks: Geotimes, v. 18, no. 10, 

p. 26-30. 

Taylor, S.R., and McLennan, S.M., 1985, The continental crust: 

its composition and evolution: Palo Alto, California, Blackwell Scientific Publications, 312 p. 

8 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 
FIGURES 3-5; TABLES 1-8 

118"30' 

S-6 

' S-3 "11 S-1 "'I P-1~' 

G-4 

\ 

G-1 

M-41~ 

.__ M-37 

M-36? 

0 2 3 4 5 6 7 8 KILOMETERS 

Figure 3. Map showing location of modally and (or) chemically analyzed grani· ic rock samples. Location numbers correspond 

to those in tables 1 to 4 and 6. See figure 2 for geologic units and explanation. 

Figures 3-5; Tables 1-8 11 
-A 65 90 p 35 35 -A 65 90 p 

35 65 90 p 

-A 35 -A 65 90 p 

12 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 
0 

Quartz monzonite 

Monzonite 

35 -A 65 90 p 

Figure 5. Plot of average modpl compositions for analyzed 

plutons of the Triple Divide Peak quadrangle. Q, quartz, P, 

plagioclase, A, alkali feldspar: Filled· star, granite of Triple Divide Peak; open star, granite of Lodgepole Campground; star 

in circle, granite of Coyote Pass; circle and vertical bar, granite of Tamarack Lake; open circle, granite of Lion Rock; open 

square, granite of Eagle Scout Peak; filled inverted triangle, 

granodiorite of Castle Creek; small dot, Mitchell Peak Granodiorite, light-colored facies; open diamond, Mitchell Peak 

Granodiorite, coarse-grained dark-colored facies; inverted 

open triangle, Mitchell Peak Granodiorite, fine-grained facies; 

filled diamond, granodiorite of Chagoopa; filled square, granodiorite of Sugarloaf; filled triangle, Paradise Granodiorite; triangle in square, Giant Forest Granodiorite; large dot, mafic 

intrusives. Classification from Streckeisen and others (1973). 

..... Figure 4. Plots of modes of granitic rocks from the Triple 

Divide Peak quadrangle. Classification scheme for granitic 

rocks from Streckeisen and others (1973). Q, quartz, P, plagioclase, A, alkali feldspar. A, Mitchell Intrusive Suite: squares, 

granodiorite of Castle Creek; dots, Mitchell Peak Granodiorite, coarse-grained, dark-colored facies; star, Mitchell Peak 

Granodiorite, coarse-grained, light-colored facies; triangles, 

Mitchell Peak Granodiorite, fine-grained facies. B, Mount 

Whitney Intrusive Suite: dots, granodiorite of Sugarloaf; 

squares, Paradise Granodiorite. C, Very light colored granitic 

rocks: diamonds, Granite of Tamarack Lake; squares, granite 

of Lodgepole Campground; dots, granite of Triple Divide 

Peak; triangles, granite of Coyote Pass. 0, Mafic intrusive 

rocks, undifferentiated. £, Dots, granodiorite of Chagoopa; 

triangles, granite of Eagle Scout Peak. F, Miscellaneous granitic rocks: diamond, granodiorite of Lightning Creek; 

squares, sheared granodiorites; triangles, granite of Lion 

Rock; dot, Giant Forest Granodiorite. 

Figures 3-5; Tables 1-8 13 
... 

~ Table 1. Chemical analyses and CIPW norms of rocks from Mitchell Intrusive Suite 

[Analyses performed by staff of the u.s. Geological Survey, L. Shapiro, J. Taggart, P. Lamothe, supervisors] 

~ Mitchell Peak Granodiorite, Mitchell Peak Granodiorite, Mitchell Peak Granodiorite Mitchell Peak Granodiorite, Granodiorite of 

-s· fine-grained facies fine-grained facies (cont.) coarse-grained facies miscellaneous rocks Castle Creek 

ii" Map No. (fig. 3) M-1 M-2 M-3 M-4 M-5 M-6 M-7 M-8 M-9 M-10 M-11 M-12 M-13 M-14 M-15 

c Field No.------- 84Ml 84Sl 84S3 6-340 83S296b 83S293a 83S298 84M2 83S293b 83s236 84S2 84S4a 83S201 83S243 83S244a 

:r (qabbro Pluql Cdikel 

a: 

til Chemical analyses 

"V 

m 

~ Si02------------ 60.2 63.8 57.3 63.1 61.1 62.3 63.8 70.0 71.6 63.4 50.4 62.0 67.5 67.1 73.3 

1:) Al203----------- 17.0 16.1 17.6 16.2 16.4 16.8 16.4 14.6 14.1 16.2 18.8 17.3 15.8 15.3 12.4 

c Fe2o 3----------- 2.54 2.10 2.85 1.9 2.31 2.21 1.94 1. 34 1.15 2.11 3. 34 2.26 0.04 1. 52 2.12 

Dol Feo------------- 3.27 2.63 4.14 2.9 3. 05 2.82 2.44 1. 30 1. 20 2.46 5.69 3.00 2.78 2.00 1. 32 ca. MgO------------- 2.84 2.16 3.39 2.3 2.55 2.29 1.98 1.04 0. 87 2.04 4.75 2.01 1.36 1. 51 0.53 

~ cao------------- 5. 75 5.11 6. 63 4.5 4.82 5. 38 4.41 2.92 2.63 4.43 8.95 4.76 4.09 3.37 1.47 :I Na2o------------ 3.97 3.59 3.76 3.6 3.48 3.80 3.73 3.42 3.18 3.77 3.36 4.49 3.27 3.56 2.45 OQ K20------------- 2.20 2.95 2.31 2.8 3.34 2.73 3. 52 4.02 4.36 2.97 1.57 1.67 3.43 3.59 5.30 F H20+------------ o. 77 0.48 0.76 0.66 0.69 0.62 0.58 0.33 0.34 0. 63 1.10 0.68 0.45 0.67 0.29 ., H20- ----------- 0.06 0.07 0.05 0.15 0.15 0.02 0. 03 0.09 <0.01 0.06 0.05 0.02 0. 03 <0.01 0. 01 ii Ti02------------ 0.76 0.59 0.90 0.71 0.76 0.65 0.59 o. 37 0.32 0. 63 1. 38 0.98 0.43 0.52 0.34 

:I P2o5------------ 0.24 0.20 0.29 0.19 0.25 0. 22 0.19 0.12 0.10 0.20 0.44 o. 34 0.12 0.16 0.12 

0 Mno------------- 0.12 0.08 0.11 0.09 0.10 0.09 0.09 0.04 0.03 0.07 0.11 0.08 0.04 0.06 o. 03 

:I 

Dol C02-------------

Total----- 99.8 99.9 

0.07 ~ ___Q_,_Q! 

100.1 99.1 99.1 

0.01 __Q_,_Q2 ___Q_,_Q! 

100.0 99.8 

0.07 

99.6 

0.03 ~ 

99.9 

___Q_,_Q.2 

99.0 

___Q_,_Q.§_ 

100.0 

__Q_,_Q_!l_ 

99.7 99.4 

___Q_,_QZ 

99.4 

0.05 ~ 

99.7 ca. 

ct 

r CIPW norms 

til 

n Q-------------- 12.7 18.1 7.84 18.0 14.2 15.4 16.6 27.2 29.7 17.8 -- 16.5 23.2 23.1 35.2 0 c-------------- -- -- -- -- -- -- -- -- -- -- -- 0. 45 -- -- 0.29 c 

:I or------------- 13.0 17.4 13.7 16.6 19.7 16.1 20.8 23.8 25.8 17.6 9.28 9.87 20.3 21.2 31.3 ... ab------------- 33.6 30.4 31.8 30.5 29.5 32.2 31.6 28.9 26.9 31.9 28.4 38.0 27.7 30.1 20.7 ;· an------------- 22.1 19.1 24.3 19.8 19.3 20.7 17.6 12.6 11.3 18.5 31.6 21.0 18.3 15.1 6.38 ~ di------------- 2. 64 2.84 3. 68 0.71 1. 60 2.51 1. 52 0.57 0.54 1. 08 5.47 -- 0.30 0.11 n he------------- 0.94 1.04 1. 51 0.30 0.58 0.94 o. 56 0.14 0.17 0.35 2.26 -- 0.34 0.04 !. en------------- 5.85 4. 07 6. 74 5.40 5.61 4.54 4.23 2.32 1. 92 4.58 8.09 5. 01 3.25 3.71 1. 32 ;: fs------------- 2. 38 1. 71 3.16 2.59 2.32 1.95 1. 77 0.67 0.69 1. 68 3. 84 2.17 4.26 1.65 0.17 ... mt------------- 3.68 3.04 4.13 2.75 3.35 3.20 2.81 1.94 1. 67 3.06 4.84 3. 28 0.06 2.20 3.07 :I il------------- 1. 44 1.12 1.71 1. 35 1. 44 1.23 1.12 0.70 0.61 1. 20 2.62 1.86 0.82 0.99 0.65 Di' ap------------- 0.56 0.46 0.67 0.44 0.58 0.51 0.44 0.28 0.23 0.46 1. 02 0. 79 0.28 0.37 0.28 

~ fo------------- -- -- -- -- -- -- -- -- -- -- 0.85 fa------------- -- -- -- -- -- -- -- -- -- -- 0.44 :I cc------------- 0.16 0.05 0.09 0.02 0.11 0.09 0.16 0. 07 0.07 0.14 0.14 0.18 0.16 0.11 0. 05 Dol 

'i' H2o------------ _Q..JU 0.55 ____Q_,JU_ ___Q_,JlJ,_ ___Q_,__§_i ~ 0.61 __Q_,_U ___Q_,__li ~ _____l_,__l_2_ _Q_,_1Q 0.48 _Q_._§_]_ _Q_,_]_Q 

Total---- 99.9 99.9 100.1 99.3 99.1 100.0 99.8 99.6 99.9 99.0 100.0 99.8 99.5 99.4 99.7 ;:;-

c 

Dol 

S' 
Table 2. Chemical analyses and CIPW norms of rocks from Sequoia Intrusive Suite 

[Analyses performed by staff of the U.s. Geological survey, L. Shapiro, J. Taggart, P. Lamothe, supervisors) 

Giant Forest Granodiorite 

Map No. (fig. 3) G-1 G-2 

Field No.------- 83S210 835213 

Si02------------

Al203-----------

Fe20J-----------

Feo-------------

Mgo-------------

cao-------------

Na2o------------ K2o-------------

H20+------------

H20- ----------- Ti02------------

P2o5------------

Mno-------------

co2------------- Total-----

Q--------------

c--------------

cr-------------

ab-------------

an-------------

di-------------

he-------------

en-------------

fs-------------

mt-------------

i1-------------

ap-------------

fo-------------

fa-------------

cc-------------

H20------------

Total----

65.6 

15.4 

1.26 

3. 06 

1. 73 

4. 02 

3. 53 

3.11 

0. 76 

0.17 

0.56 

0.12 

0.08 

.....Q_,_],Q 

99.5 

21.2 

18.4 

29.9 

17.0 

0. 72 

0.55 

3.98 

3.51 

1. 83 

1. 06 

0. 28 

0.23 

.....Q....21. 

99.6 

66.7 

15.5 

1. 37 

2.58 

1. 31 

3.58 

3. 72 

2.88 

0.46 

0.08 

0.48 

0.17 

o. 07 

0.06 

99.0 

23.7 

0. 30 

17.0 

31.5 

16.3 

3.26 

2.94 

1.99 

0.93 

0. 40 

0.14 

~ 

99.0 

G-3 

835245 

67.1 

15.3 

1.82 

2. 23 

1. 26 

3.36 

3. 77 

2.96 

0. 54 

0.04 

0.49 

0.13 

0. 08 

.....Q_,_],Q 

99.2 

24.5 

0. 33 

17.5 

31.9 

15.2 

3.14 

1. 93 

2. 64 

0.93 

0. 30 

0. 23 

_Q..2!! 

99.2 

G-4 

6-325 

Granodiorite 

of Clover Creek 

G-5 G-6 

83S225 835288 

Chemical analyses 

64.8 

15.9 

1.4 

3.1 

1.6 

4.0 

3.5 

2.9 

1.0 

0. 04 

0. 61 

0.13 

0.07 

_Q....Ql 

99.1 

67.4 

14.9 

0.92 

2.93 

1. 07 

3.01 

3.46 

3.94 

0. 38 

0.05 

0.55 

0.16 

0. 07 

_Q_._Q2 

98.9 

CIPW norms 

21.1 

0. 07 

17.1 

29.6 

18.9 

3. 99 

3. 66 

2.03 

1.16 

0. 30 

o. 02 

-l....M 

99.0 

23.1 

0.02 

23.3 

29.3 

13.4 

2. 67 

3.84 

1. 33 

1.04 

0.37 

0.16 

.-!l......il 

99.0 

65.8 

15.5 

1.81 

2. 49 

1. 50 

3.95 

3. 71 

3. 07 

0. 73 

0.06 

o. 70 

0. 21 

o. 09 

~ 

99.7 

21.9 

18.1 

31.4 

16.6 

0.59 

0.29 

3.46 

1.94 

2.62 

1. 33 

0.49 

0.20 

o. 79 

99.7 

Granite of Big 

Meadows 

G-7 

83S246 

69.2 

14.7 

1. 24 

1.66 

0.90 

2.28 

3. 66 

4.30" 

0. 34 

0.09 

0.43 

0.13 

0.07 

__Q_,_Q§ 

99.1 

25.1 

6.33 

25.4 

31.0 

10.1 

2.24 

1.44 

1.80 

0.82 

o. 30 

0.14 

.-!l......il 

99.1 

Diorite 

dikes 

G-8 G-9 

83S299b 83S300a 

58.1 

16.5 

2.16 

4.81 

3.90 

7. 09 

2.66 

1. 83 

1.16 

0.05 

1.19 

0.18 

0.12 

~ 

99.8 

14.1 

10.8 

22.5 

27.7 

3.34 

1.59 

8.17 

4.46 

3.13 

2.26 

0. 42 

0.09 

.....L..ll 

99.8 

56.0 

18.4 

2.65 

5. 05 

2. 49 

6.65 

3.61 

1. 79 

o. 99 

0.11 

1.12 

0.40 

0.14 

__Q_,_Ql 

99.4 

9. 22 

10.6 

30.6 

28.7 

0. 68 

o. 53 

5. 89 

5.21 

3.84 

2.13 

0.93 

o. 07 

__L_1Q 

99.5 

Table 3. Chemical analyses and CIPW norms of rocks from miscellaneous plutons 

(Analyses performed by staff of the U.S.Ge~1ogical Survey, L. Shapiro, J. Taggart, P. Lamothe, supervisors] 

Granite of Lodgepole Granite of Granite of Triple Granite of Eagle 

Campground Tamarack Lake Divide Peak scout Peak 

Map No. (fig. 3) L-1 L-2 L-3 L-4 T-1 T-2 T-3 TD-1 Es:l Field No.------- 83s200 87TD6 87TD7 87TD2 6-130 85S74 85S76b 6-109 6-332 

(altered} 

Chemical analyses 

Si02------------ 68.2 75.4 71.2 57.0 75.6 74.3 75.3 77.1 71.4 

Al203----------- 15.3 13.0 15.5 15.4 13.0 13.5 13.0 12.3 14.4 

Fe2o 3----------- 1. 04 0.71 0.45 9.9 0.42 0.88 0. 79 0.66 1.1 

FeO------------- 2.04 0. 54 0.86 1.80 0. 76 0. 64 0.53 o. 40 1.0 MgO------------- 0.82 0. 20 0. 29 0.13 0.16 0. 35 0.24 0.12 0. 57 cao------------- 2. 63 1.13 1. 58 1.45 0.84 1. 23 1.15 o. 76 1. 80 Na2o------------ 3 ,'91 3.12 4.16 3. 23 3.4 3.30 3.11 3.8 3.8 K2o------------- 3.95 5.13 5.21 7.09 4.4 4.97 5.28 4.4 4.2 

H20+------------ 0.31 0.15 0.13 1. 62 o. 42 0. 43 0.22 o. 20 0.44 

H20- ----------- 0.05 0.07 0.06 0. 30 0. 02 0.02 0. 04 0.02 0.11 Ti02------------ 0.45 0.11 0.14 0. 39 0.13 0.19 0.21 0.08 0. 32 

P2o5------------ 0.16 0.05 0.06 0. 08 0. 05 0. 05 <0.05 0.02 0.08 

Mno------------- 0.05 0. 03 0.04 0.05 0. 04 0. 04 0. 03 0.05 0.06 

C02------------- 0. 08 ~ <0.01 <0.01 _Q....Ql <0. 01 <0.01 ~ _Q....Ql 

Total----- 99.0 99.6 99.7 98.4 99.3 99.9 99.9 99.9 99.3 

CIPW norms 

Q-------------- 23.1 34.9 22.9 8.03 36.7 33.0 34.2 36.4 28.5 

c-------------- 0.38 o. 38 0. 29 1. 26 0.58 0.08 0.55 

or------------- 23.3 30.3 30.8 41.9 26.0 29.4 31.2 26.0 24.8 

ab------------- 33.1 26.4 35.2 27.3 28.8 27.9 26.3 32.2 32.2 

an------------- 11.5 5. 28 7.45 6.58 3. 78 5. 78 5.70 3.51 8. 34 

di------------- 0. 07 o.o he------------- o.o en------------- 2.04 0.50 0. 72 o. 29 o. 40 o. 87 0.60 0.30 1.42 

fs------------- 2.24 0. 28 1. 05 0. 91 0.21 o. 03 0.15 o. 51 

mt------------- 1. 51 1. 03 0.65 4.83 0.61 1. 28 1.15 0.96 1. 59 

i1------------- 0. 85 0.21 0. 27 o. 74 0.25 0. 36 0.40 0.15 0.61 

ap------------- 0. 37 0.12 0.14 0.19 0.12 0.12 <0.1 0. 05 0.19 

fo-------------

fa-------------

cc------------- 0.18 0. 02 0. 05 0. 02 H2o------------ 0.36 0.22 0.19 1. 92 0.44 0.45 0.26 0.22 0. 55 

hm------------- 6. 57 

Total---- 98.9 99.6 99.7 98.4 99.3 100.0 99.9 100.0 99.3 

Granodiorite 

of Chagoopa 

C-1 C-2 

6-138 85S13d 

(mafic inclusion) 

66.0 57.4 

15.9 16.8 

1.4 1. 56 

2.4 5.18 

0.93 3.25 

2.3 5. 62 

4. 7 5.00 

3.4 2.19 

0.86 0.91 

0.15 0.15 

0.66 0.95 

0.17 0. 24 

0.11 0.17 

0.01 0.08 

99.0 99.5 

18.8 2.69 

0. 74 

20.1 12.9 

39.8 42.3 

10.2 16.9 

4.17 

3.13 

2. 32 6.16 

2.37 5.30 

2.03 2.26 

1. 25 1. 80 

0.40 0.56 

o. 02 0.18 

1.01 1. 06 

-- 99.0 99.4 

Figures 3-5; Tables 1-8 15 
Table 4. Chemical analyses and CIPW norms of rocks from 

mafic intrusions near Hamilton Lake 

[Analyses performed by staff of the U.S. Geological Survey, L. 

Shapiro, J. Taggart, P. Lamothe, supervisors] 

Dike 

cutting 

granite 

Sills and stocks Coarse 

cumulate 

Map No. (fig. 3) 

Field No.------- H-1 

85S76a H-2 H-3 H-4 H-5 H-6 6-117 85S72a 85S73c 85S70a 85S69 

Si02------------

Al203-----------

Fe203-----------

Fe0-------------

Mgo-------------

cao-------------

Na 2 o------------ K2o-------------

H20+------------

H20- ----------- Ti02------------

P2o5------------

Mno-------------

co2 ------------- Total-----

Q--------------

c--------------

or-------------

ab-------------

an-------------

di-------------

he-------------

en-------------

fs-------------

mt-------------

il-------------

ap-------------

fo-------------

fa-------------

cc-------------

H20------------

Total----

57.6 

17.4 

3.14 

3.80 

2.83 

6.50 

3. 93 

2. 22 

0.80 

0.08 

1.16 

0.38 

0.12 

<0.01 

100.0 

9.35 

13.1 

33.3 

23.3 

3.91 

1. 30 

5.24 

2.00 

4.55 

2.20 

0. 88 

~ 

100.0 

Chemical analyses 

58. 0 55. 6 52. 8 

17.0 18.1 18.8 

3.0 3.84 4.28 

4.2 4.16 4.53 

3.0 3.18 3.77 

6.2 7.22 8.73 

3.6 3.73 3.45 

2.3 1.39 1.38 0.74 1.25 1.01 

0.11 0.12 0.10 

1.1 1.05 1.29 

0.31 0.37 0.40 

0.11 0.20 0.19 

__Q_,_Q£ <0.01 <0.01 99.7 100.2 100.7 

CIPW norms 

10.9 

13.6 

30.5 

23.4 

2. 94 

1. 24 

6.11 

2.96 

4.35 

2. 09 

0. 72 

0. 05 

9.06 

8.21 

31.6 

28.5 

2.91 

1. 00 

6. 57 

2. 57 

5. 57 

1. 99 

0. 86 

4.82 

8.16 

29.2 

31.7 

5. 61 

1. 56 

6.79 

2.17 

6.21 

2.45 

0. 93 

0.85 __L_ll _____l__,__ll 

99.7 100.2 100.7 

Table 5. Areal size of geologic map units 

Unit (fig. 2) Area (km2 ) 

Giant Forest Granodiorite -------------- 42.9 

Granite of Big Meadows ----------------- 19.0 

Granodiorite of Clover Creek ----------- 5.1 Granite of Weaver Lake----------------- 3.1 

Granite of Lodgepole Campground -------- 28.8 

Granite of Dome Creek ------------------ 8.4 

Granodiorite of Castle Creek ----------- 68.5 Mitchell Peak Granodiorite, 

coarse facies --------------------- 50.9 Mitchell Peak Granodiorite, 

fine facies ---------------------- 125.8 

Granodiorite of Lightning 

creek ----------------------------- 3. 1 

Granodiorite of Lookout 

Peak ------------------------------ <0. 1 

Granodiorite of Sugarloaf ------------- 117.5 

Paradise Granodiorite ------------------ 51.8 

Granite of Tamarack Lake --------------- 4.6 

Granite of Eagle Scout Peak ------------ 34.9 Granite of Coyote Pass ----------------- 7. 4 

Granodiorite of Chagoopa --------------- 13.5 

Granite of Mount Kaweah ---------------- 5.5 

Granite of Lion Rock ------------------- 1.8 Granite of Triple Divide Peak ---------- 6.2 

Porphyry of Black Kaweah --------------- 0.2 

Mafic plutonic rocks ------------------- 6.5 

Sheared granodiorite ------------------- 6.3 Metamorphic rocks ----------------------~ 

Total ---------------------------- 620.1 

53.3 

17.1 

3.65 

4.56 

4. 48 

9. 04 

3.39 

1. 35 1. 03 

0. 25 

1. 26 

0.30 

0. 10 

__Q__,_Q2 

99.9 

5.04 

7.98 

28.7 

27.5 

9.52 

2.58 

6.75 

2.09 

5. 29 

2.39 

0.70 

0.11 

~ 

99.9 

48.2 

13.8 

3.41 

7.82 

12. 1 

6.55 

2. 18 

2.99 

2.08 

0.12 

0.95 

0.20 

0.36 

<0.01 

100.8 

17.7 

18.5 

19.0 

7.45 

2.29 

1. 27 

0.45 

4.94 

1. 80 

0.46 

17.8 

6. 93 

Percentage of 

total area 

6.9 

3.1 

0.8 

0.5 

4.6 

1.4 

11.1 

8.2 

20.3 

0.5 

<0.1 

19.0 

8.4 

0. 7 

5.6 

1.2 

2. 2 

0. 9 

0.3 

1.0 

<0.1 

1.0 

1.0 

1.3 

~0 

Table 6. Modes of plutonic rocks 

[0. Polovtzoff and T. Sisson, analysts] 

Map No. 

(fig. 3) 

Field Mafic Specific 

No. Quartz K-feldspar Plagioclase minerals gravity 

Dioritic rocks near Hamilton Lake 

H-2 6-117 

H-7 6-112 

H-8 6-113 

H-9 6-114 

H-10 6-115 

H-11 6-116 

H-12 6-118 

Average 

standard deviation 

S-1 68ml8 

S-2 68m23 

S-3 68m17 S-4 8-17 

S-5 68m27 

s-6 68rn13 

14.7 

6. 4 

o. 8 

7.9 

0.0 

13.8 

3.8 

6. 8 

5. 8 

20.4 

20.0 

22.8 

24.5 

14.8 

23.2 

Average 21.0 

Standard deviation 3. 5 

6.3 63.3 

0. 0 56.8 

o.o 65.3 

0.1 63.8 

0.0 64.6 

1.8 61.6 

0.0 39.6 

1. 2 59.3 

2.4 9.1 

Granodiorite of Sugarloaf 

25.1 41.0 

27.3 41.8 

18.7 45.8 21.7 43.0 

16.4 48.0 

19.7 45.4 

21.5 

4.1 

44.2 

2.7 

Granite of Eagle Scout Peak 

ES-1 

ES-2 

ES-3 

ES-4 

ES-5 

ES-6 

ES-7 

ES-8 

ES-9 

ES-10 

ES-11 

ES-12 

ES-13 

6-332 

6-329 

6-111 

6-110 

3-19 

6-331 

8-52 

8-51 

75m27 

6-338 

6-129 

6-328 

6-339 

26.8 

29.4 

25.6 

27.6 

32.1 

26.7 

31.0 

30.1 

30.0 

27.7 

28.7 

27.1 

26.4 

Average 28.4 

Standard deviation 2.0 

C-1 6-138 17.6 

C-3 6-135 17.9 

C-4 6-136 25.2 

C-5 6-345 20.2 

C-6 6-145 9.4 

C-7 6-143 13.0 

Average 17.2 

Standard deviation 5.5 

30.0 

28.6 

29.9 

24.5 

31.7 

26.0 

30.2 

26.0 

35.0 

27.1 

31.8 

32.9 

25.5 

29.2 

3. 2 

38 .'2 37.5 

39.6 

43.4 

34.3 

41.1 

32.8 

38.7 

31.0 

39.0 

33.0 

34.9 

39.0 

37.1 

3.6 

Granodiorite of Chagoopa 

22.4 53.5 

21.2 50.4 

24.0 40.0 

18.6 49.7 

45.3 38.4 

25.3 40.0 

26.1 45.3 

9.7 6.6 

15.7 

36.7 

33.9 

28.2 

35.4 

22.8 

56.6 

32.8 

12.9 

13.4 

10.9 

12.7 

10.8 

20.8 

11.7 

13.4 

3.8 

5.0 

4.5 

4.9 

4.5 

1.9 

6.2 

6.0 

5. 2 

4.0 

6.2 

6.5 

5.1 

9.2 

5.3 

1.7 

6.5 

10.5 

10.8 

11.5 

6. 9 

21.7 

11.3 

5.5 

2.770 

2.945 

2.938 

2.849 

2.930 

2.766 

2.950 

2.878 

0.083 

2.698 

2.643 

2.702 

2.675 

2.736 

2.660 

2.686 

0.033 

2.630 

2. 625 

2.636 

2.650 

2.635 

2.635 

2.650 

2.640 

2.630 

2.615 

2.634 

2.613 

2.637 

2.633 

0.011 

2. 667 

2.665 

2.665 

2.690 

2.650 

2.675 

2.669 

0.013 

16 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 
Table 6. Modes of plutonic rocks-Continued· Table 6. Modes of plutonic rocks-Continued 

Map No. Field Mafic Specific Map No. Field Mafic Specific (fig. 3) No. Quartz K-feldspar Plagioclase minerals gravity (fig. 3) No. Quartz K-feldspar Plagioclase minerals gravity 

Granite of Triple Divide Peak Granodiorite of Castle Creek 

TD-1 6-109 31.0 34.7 33.0 1.3 2.610 M-36 8-47 20.3 16.8 48.0 14.9 2.695 TD-2 6-128 27.6 37.5 33.5 1.4 2.600 M-37 8-48 19.8 7.9 46.7 25.6 2.760 TD-3 9-13 31.2 40.5 27.6 <0.1 2.610 M-38 8-39 23.0 16.3 44.3 16.4 2.705 TD-4 8-18 35.4 35.3 24.4 4.9 2.625 M-39 8-42 13.6 8. 7 50.7 27.0 2.745 

M-40 8-41 23.4 22.7 42.7 11.2 

M-41 8-49 10.5 13.2 52.9 23.6 Average 31.3 37.0 29.6 1.9 2.611 M-42 8-50 20.0 20.0 47.4 12.8 Standard deviation 3.2 2.6 4.4 2.1 0.010 

Average 18.7 15.1 47.5 18.8 2.726 

Granite of Tamarack Lake Standard deviation 4.8 5.5 3.5 6.5 0.031 

T-1 6-130 27.4 35.5 33.1 4.0 2.595 Paradise Granodiorite T-4 6-337 33.1 36.9 26.3 3.7 2.615 

P-1 75m15 23.3 22.6 45.5 8.6 2.685 Average 30.3 36.2 29.7 3.9 2.605 P-2 75m17 24.0 21.1 46.9 8.0 2. 690 Standard deviation 4.0 1.0 4.8 0.2 0.014 

Average 23,7 21.9 46.2 8.3 2.688 

Standard deviation 0.5 1.1 1.0 0.4 0.004 Granite of coyote Pass 

CP-1 6-131 23.8 56.3 17.6 2.3 2.622 Giant Forest Granodiorite CP-2 8-43 32.9 42.0 22.1 3.0 2.620 

G-4 6-324 23.3 10.8 46.9 19.0 2. 708 Average 28.4 49.2 19.9 2.7 2.621 Standard deviation 6.4 10.1 3.2 0.5 0.001 

Granite of Lodgepole campground 

Mitchell Peak Granodiorite, fine-grained facies 

L-5 3-15 41.2 41.2 17.0 0.6 2.610 

L-6 6-326 22.5 23.9 44.8 8.8 2.645 M-4 6-340 21.6 18.4 45.4 14.6 2. 715 L-7 75m34 27.2 43.1 28.1 1.6 2.605 M-16 8-45 18.2 15.1 51.9 14.9 M-17 9-14 22.2 18.5 41.6 17.7 2.760 

M-18 6-330 17.7 19.2 49.1 14.0 2.692 Average 30.3 36.1 30.0 3. 7 2.620 M-19 3-16 19.7 14.1 48.8 17.4 2.735 Standard deviation 9.7 10.6 14.0 4.5 0.022 M-20 75m23 15.3 15.9 51.0 17.8 2.740 

M-21 75m24 15.6 10.2 53.8 20.4 2.765 M-22 75m25 18.8 19.6 49.7 11.9 2.715 

M-23 75m29 19.4 15.1 49.5 16.0 2.740 Granite of Lion Rock M-24 75m30 18.1 11.8 50.1 20.0 2.760 

M-25 75m32 15.1 9.2 56.6 19.1 2.725 

M-26 75m33 19.5 10.6 52.5 17.4 2.738 LR-1 6-139 28.9 28.6 38.5 4.0 2.633 M-27 75m35 20.8 21.8 43.9 13.5 2.700 LR-2 6-341 28.7 30.8 35.3 5.2 2.650 M-28 68m24 16.5 12.1 43.2 28.2 2.735 LR-3 9-12 31.8 33.9 28.2 6.1 2.650 M-29 3-17 16.4 9.6 55.1 18.9 2. 765 

Average 29.8 31.1 34.0 5.1 2.644 Average 18.3 14.7 49.5 17.5 2.735 Standard deviation 1.7 2. 7 5.3 1.1 0.010 Standard deviation 2.3 4.1 4.4 3.9 0.023 

Granodiorite of Lightning Creek Mitchell Peak Granodiorite, coarse-grained facies 

LC-1 2-59 24.8 13.4 46.3 15.5 2.690 M-30 75m28 24.9 8.6 51.3 15.2 2.730 M-31 3-18 28.6 29.6 34.5 7.3 2.660 M-32 3-20 24.7 19.0 46.2 10.1 2.675 M-33 8-38 17.9 14.6 52.2 .15.3 2.695 Map No. Field Mafic Specific M-34 8-46 21.3 23.0 38.6 17.1 2.700 (fig. 3) No. Quartz K-feldspar Plagioclase .minerals gravity M-35 9-10 18.2 20.7 51.1 10.0 2.730 

Average 22.6 19.3 45.7 12.5 Quartz Diorite of Empire Mountain 2. 698 Standard deviation 4.2 7.2 7.5 3.9 0.028 

EM-1 8-44 12.9 12.6 55.1 19.4 2.730 

Sheared Granodiorite 

SG-1 6-133 24.2 12.3 40.9 22.6 2.700 

SG-2 9-11 21.9 21.6 41.4 15.1 2.735 

Average 23.1 17.0 41.2 18.9 2. 718 

standard deviation 1.6 6.6 0.4 5.3 0.025 

Figures 3-5; Tables 1-8 17 
Table 7. Average chemical composition, in weight percent, of plutonic rocks, with estimates of the average upper continental crust and Precambrian Candian Shield 

(Taylor and Mclennan, 1985) 

[*, indicates all iron expressed as FeO] 

Triple Divide Peak Upper continental Canadian 

quadrangle crust Shield 

SiO 66.5 66.0 65.1 

Al 263 15. 5" 15.2 15.5 

~=t3 1. 70 

2.21 4.5* 4.21* 

MgO 1. 60 2. 2 2.22 

cao 3. 75 4.2 3.76 

Nat 3. 64 3.9 3. 68 

K;a 3.41 3.4 2.99 

T102 0.54 0.5 o. 53 

P205 0.17 0.16 

MnO 0. 07 0.08 0.07 

Table 8. Mineral-liquid modeling parameters 

[K0 , mineral-liquid exchange distribution coefficients; calculated as the ratio 

of a pair of cations in a mineral divided by the corresponding ratio in the 

coexisting liquid. For example, for equilibrium between hornblende and liquid 

the Fe-Mg K0 is ( (FejMg)hbl.l (Fe/Mg) lig.). Thus, equilibrium mineral compositions 

can be calculated from liquid composit.ion, exchange K0 , and mineral stoichiometry] 

Mineral compositions calculated as follows: 

Plagioclase: 

Hornblende: 

Apatite (wt. 

~:~a 

Ca-Na K0 (min.jliq.) 

1.800 

Fe-Mg K0 . 

0. 250 Al-Si K0 1. 000 

percent): 

~:~a ~~a~3 FeO MgO MnO 

0. 00 0.00 0.00 

Magnetite (wt. percent) 

~~~a ~:~a Al 2o 3 FeO MgO MnO 2.40 49.87 1. 20 1. 00 

Mineral densities: 

Plagioclase: linear function of An content 

cao 

55.82 

cao 

0.10 

cations Fe 

0. 030 

cations Ti: 

function of 

Al/Si 

;~a~3 ~~~~9 

;~~~1 ~~~8 

(An percent: 68.5-52.6; sp. gr.: 2.72-2.69) 

Hornblende: linear function of Mg/Mg+Fe (sp. gr.: 3.24-3.08). 

Apatite: fixed 3.17 

Magnetite: fixed 5.16 

18 Triple Divide Peak Quadrangle, Fresno and Tulare Counties, California-Analytic Data 

cations Mg 

0.030 

cations Na: 

function of 

Al/Si 


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