Batholithic Rocks of 

Southern California A Model for 

the Petrochemical Nature of 

their Source Materials

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1284

Batholithic Rocks of 

Southern California A Model for 

the Petrochemical Nature of 

their Source Materials

By A. K. BAIRD and A. T. MIESCH

U.S. GEOLOGICAL SURVEY PROFESSIONAL PAPER 1284

A mathematical model is used to remove 

the effects ofmagmatic differentiation 

from the chemical data on 480 samples

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1984
UNITED STATES DEPARTMENT OF THE INTERIOR 

WILLIAM P. CLARK, Secretary

GEOLOGICAL SURVEY 

Dallas L. Peck, Director

Library of Congress Cataloging in Publication Data

Baird, Alexander K.

Batholithic rocks of southern California.

(Geological Survey Professional Paper ; 1284)

Bibliography: 42 p.

1. Batholiths California, Southern. I. Miesch, A. T. (Alfred T.) II. Geological Survey (U.S.) III.

Title. IV. Series. 

QE461.B24 1983 552'.3 82-21048

For sale by the Branch of Distribution

U.S. Geological Survey

604 South Pickett Street

Alexandria, VA 22304
CONTENTS

Abstract ............................. 1

Introduction ........................... 1

Regional geologic setting ................... 1

Previous geochemical studies .................. 4

Petrologic nomenclature ..................... 4

Acknowledgments ........................ 5

Development of the model ................... 5

Number of end members ................. 5

Compositional structure .................. 8

Derivation of the differentiate end-members D-l and

D-2 ......................... 10

Derivation of the magma end-members M-l and M-2 . 11

Page

Characteristics of the model .................. 12

Petrology of the magma end-members M-l and M-2 . 12

Mixing proportions ................... 14

Regional variation in the compositions of the magmas

and differentiates .................. 16

Anomalous samples ..................... 18

Relations to other geologic features ........... 19

Discussion ............................ 21

Summary and conclusions .................... 22

References cited ......................... 23

Appendixes 1 and 2 ....................... 35

ILLUSTRATIONS

Page

FIGURE 1. Map showing geologic provinces and major fault patterns of southern and central California and northern Baja California,

Mexico ............................................................ 2

2. Generalized map of the Mesozoic plutonic rocks of the northern Peninsular and Transverse Ranges Provinces, Calif. . . 3

3. Map of sampling localities in Mesozoic plutonic rocks of the northern Peninsular and Transverse Ranges, California . . 6

4. Factor-variance diagram for the bathlolithic rocks of southern California ........................ 9

5. Factor-variance diagram for the Santa Ana block ..................................... 12

6. Factor-variance diagram for the San Bernardino block ................................... 13

7. Stereogram for the Santa Ana block ............................................. 14

8. Stereogram for the San Bernardino block .......................................... 15

9-12. Maps showing:

9. Relative amounts of magma required for formation of batholithic rocks .................... 18

10. Percentages of end-member M-2 .......................................... 19

11. Percentages of end-member D-2 .......................................... 20

12. Variability of Si02, A1203, FeO, MgO, CaO, Na^O, K20, and Ti02 in the batholithic rocks of southern California

and in the magmas and differentiates as interpreted from the model .................. 25

TABLES

TABLE 1. Average compositions of the batholithic rocks ......................................... 8

2. Chemical variances in the batholithic rocks ........................................... 9

3. Biotite and hornblende compositions ............................................... 10

4. Compositions of two mineral assemblages and end members D-l and D-2 ......................... 10

5. Compositions represented by some points on figure 7 .................................... 14

6. Compositions represented by some points on figure 8 .................................... 15

7. Chemical and normative compositions of the end members .................................. 16

8. Compositions of two samples of gabbros ............................................ 16

9. Analyses from the U.S. Geological Survey RASS file .................................... 17

10. Statistical summary of mixing proportions ........................................... 17

11. Mean values of parameters .................................................... 17

12. Average compositions of the magmas .............................................. 21

13. Average compositions of the differentiates ........................................... 21

m

BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA A MODEL 

FOR THE PETROCHEMICAL NATURE OF THEIR SOURCE MATERIALS

By A. K. BAIRD 1 and A. T. MlESCH

ABSTRACT

Major-element analyses of 497 composite samples of batholithic 

rocks (quartz diorites, granodiorites, and quartz monzonites) from the 

northern Peninsular Ranges and Transverse Ranges Provinces, 

southern California, form the basis for a mixing model that accounts 

for most of the compositional variation in the rocks. The compositional 

structure in the batholithic rocks as a group was found to be similar 

to that in the Sierra Nevada batholith, and indicates that four end 

members are sufficient to account for 85-97 percent of the variability 

in each of the eight major oxides. According to the model, the 

batholithic rocks formed from the mixing of basaltic and quartzofeldspathic end-member magmas, and the removal of variable proportions of plagioclase and mafic minerals, principally hornblende. Gabbroic rocks, common only in the western part of the region, could 

have formed from nearly uncontaminated magmas of the basaltic end 

member. Variations in the mixtures of basaltic and quartzofeldspathic magmas are presumed to reflect variations in their source 

materials at depth. According to the model, the compositions of the 

source materials do not vary smoothly over the region, but display 

a discontinuity along a line approximately coincident with the present 

San Jacinto fault zone. The discontinuity is roughly coincident with 

previously noted petrologic and isotopic discontinuities in the northern Peninsular Ranges and is interpreted as the western limit of 

significant contribution of continental materials to the batholithic 

rocks. The model gives no evidence of a discontinuity in the vicinity 

of the San Andreas fault zone.

INTRODUCTION

The batholithic rocks of late Mesozoic age in southern 

California are exposed over 18,000 km2 (square kilometers) in parts of two geologic provinces, the Peninsular 

Ranges Province and the Transverse Ranges Province 

(fig. 1), and range in composition from gabbro to quartz 

monzonite. Composite samples from 548 localities were 

analyzed for eight major elements (Baird and others, 

1979) and these data form the basis for compositional 

modeling with an extended method of Q-mode factor 

analysis (Miesch, 1976b). The method was used to determine the number and nature of end members required to adequately explain the observed chemical variations. Areal variations in the corresponding mixing 

proportions and in the derived compositions of the endmember magmas, or magma-source materials, display 

a distinct discontinuity in the eastern part of the Peninsular Ranges Province.

'Present address: Pomona College, Claremont, CA 91711

REGIONAL GEOLOGIC SETTING

The northern Peninsular Ranges lie at the northern 

end of a narrow (120 km) belt of batholithic rocks of 

Mesozoic age that can be traced southward for hundreds of kilometers into Baja California, Mexico. The 

eastern limit of this belt, over all its length, is in the 

flooded depression of the Gulf of California and its 

northward extension, the Salton Trough. The Gulf is 

interpreted to have formed in latest Tertiary time by 

oceanic spreading on the East Pacific Rise; the Salton 

Trough is believed to have formed by a series of rhombochasms developed along the San Andreas fault zone 

(fig. 2). The northern terminus of the Peninsular 

Ranges Province, and the southern boundary of the 

Transverse Ranges Province, is at the east-striking 

Malibu Coast-Cucamonga fault zone and its possible 

eastward continuation, the Banning fault (fig. 2). The 

San Andreas fault zone continues northwestward from 

the northern margin of the Peninsular Ranges diagonally across the Transverse Ranges Province. Other 

fault zones, especially the San Jacinto and Elsinore 

(both subparallel to the San Andreas) and the eaststriking Pinto Mountain fault, provide boundaries for 

further subdivisions of the provinces. We recognize six 

structurally-bounded units or blocks (fig. 2): San Gabriel, San Bernardino, and Little San Bernardino (Transverse Ranges), and San Jacinto, Perris, and Santa Ana 

(Peninsular Ranges).

To claim that this region is the most geologically enigmatic part of California is an understatement. Certain 

petrologic-structural aspects have been agreed to by 

most workers, but other aspects have received diverse 

interpretations. General, if not universal, agreement 

exists on the following aspects:

1. Plutonic igneous rocks are mostly late Mesozoic 

in age and are intrusive into metamorphic rocks apparently no older than Triassic in the Peninsular Ranges 

but as old as late Precambrian in the Transverse 

Ranges.

2. Plutonic igneous rocks vary compositionally from 

southwest to northeast, from mafic to felsic. Gabbroic 

rocks are found only in the Peninsular Ranges and most 

are southwest of the San Jacinto fault.

3. Plutonic igneous rocks are dominantly the product
BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

PACIFIC OCEAN ^ O ^^ 34° -

32° -

FIGURE 1. Geologic provinces of southern and central California and northern Baja California, Mexico (dotted lines). Heavy lines delineate 

major fault patterns, dashed where inferred. Shaded rectangle outlines area of figures 2 and 3.

of magmatic activity; that is, they form numerous individual plutons that have internal structures characteristic of flow.

4. At least some, if not most, of the faults that bound 

structural blocks postdate the emplacements of the 

plutonic rocks, and movements on the faults have continued to Holocene times.

The nature and magnitude of separation on the San 

Andreas fault in southern California remain subjects of 

major disagreement. (The total separations on the Elsinore and San Jacinto faults have been relatively small 

15 km or less by most interpretations.) The San Andreas fault has been judged (1) a major strike-slip fault 

in California with hundreds of kilometers of movement 

dating back to (perhaps) early Mesozoic time (Hill and 

Dibblee, 1953), (2) a major continental transform and

plate boundary also with hundreds of kilometers of 

movement (Atwater, 1970), (3) a boundary of minor importance in the Transverse Ranges (Hadley and 

Kanamori, 1977; Yeats, 1981), (4) an important strikeslip fault in southern California that has 250 km of separation (Crowell, 1979), (5) a relatively minor strike-slip 

fault in southern California that has 35-70 km of right 

separation at the Transverse Ranges (Baird, Morton, 

Woodford, and Baird, 1974), (6) a minor structure that 

does not significantly offset bedrock patterns in southern California (Woodford, 1960), and, finally, (7) a 

minor participant in large-scale rotational tectonics of 

southern California that does not cut the Transverse 

Ranges (Luyendyk and others, 1979). Thus, depending 

upon the interpretation, the San Andreas fault in this 

part of California may be young, may be old, or may
INTRODUCTION
BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

have only a few kilometers or more than 1000 km of 

separation. If the separation since Mesozoic time has 

been large then, obviously, it is fortuitous that the 

plutonic rocks east of the San Andreas (San Bernardino 

and Little San Bernardino blocks) are presently adjacent to similar rocks west of the fault, it is accidental 

that apparently continuous areal patterns of petrologic 

variation occur across the region, and a happenstance 

that distinct, internally consistent patterns of chemical 

variations in all these rocks suggest a common origin 

and evolution that are different from those of other Cordilleran batholithic masses (Baird and others, 1979).

PREVIOUS GEOCHEMICAL STUDIES

The first extensive and the definitive work on the 

batholithic rocks of the area was by E. S. Larsen, Jr. 

(1948) who described a number of plutonic units in the 

northern Peninsular Ranges and published dozens of 

chemical and modal analyses. Through his work, these 

rocks became known as the "southern California 

batholith," although Larsen clearly recognized that the 

same batholithic mass extends great distances into 

Mexico. The area he studied and mapped is essentially 

that of the Perris and Santa Ana blocks of the present 

paper (fig. 2). The name "southern California batholith" 

has been restricted to the Peninsular Ranges Province 

and has not been extended to include the Transverse 

Ranges, perhaps mainly because of Larsen's work.

Within and southeast of the area described by Larsen, a number of more detailed studies bearing on the 

geochemistry of plutonic rocks have been made (for example, Morton and others, 1969; Miesch and Morton, 

1977; Morton and Baird, 1976; Nishimori, 1976; Todd 

and Shaw, 1979; Taylor and Silver, 1978; Walawender, 

1979). Reconnaissance work in Mexico by Gastil and 

others (1975) has established the general geology of the 

batholithic rocks there. Isotope, trace-element and 

radiometric-dating studies have been pursued by Silver 

and colleagues (for example, Silver and others, 1975; 

Taylor and Silver, 1978; Gromet and Silver, 1979), by 

Krummenacher and others (1975), and by DePaolo 

(1980). Much of this work, especially as it pertains to 

the southern Peninsular Ranges within California, has 

been carefully summarized by Abbott and Todd (1979).

To the north, in the Transverse Ranges, considerably 

less work bearing on the geochemistry of batholithic 

rocks has been done. However, individual plutons have 

been studied (for example, Baird and others, 1967; 

Richmond, 1965), problems of the older Mesozoic syenitic rocks have been described (Miller, 1977), and 

radiometric dates for both wallrock and some intrusives 

have been reported (Silver, 1971).

The basis for the present report is the group of 548 

composite samples collected by Baird and his colleagues

(fig. 3). The purpose of the sampling was to provide 

unbiased representative samples of the batholithic rocks 

that could be used to determime areal distributions of 

the major and minor elements. Details of the methods, 

analyses, and discussions of elemental distributions are 

given elsewhere (Baird, 1975; Baird, Morton, Woodford, and Baird, 1974; and Baird, Baird, and Welday, 

1974, 1979). In summary, the principal findings from 

these prior studies are:

1. All elements, except aluminum and titanium, have 

statistically significant regional trends that increase or 

decrease to the northeast.

2. Silicon, potassium, and to a lesser extent sodium, 

increase markedly toward the northeast in a fashion 

directly predictable from areal distributions of rock 

types (gabbro to quartz monzonite) and from position 

with respect to the continental margin.

3. Within individual quartz-rich rock types (quartz 

monzonite, granodiorite and quartz diorite), however, 

silicon varies antipathetically with potassium.

4. Potassium, the element that exhibits the strongest 

trend, seems to vary independently of the other elements within the quartz-rich rock types, but dependently in gabbroic rocks.

5. Chemical variations are continuous, without the 

stepwise sequences thought to characterize the Sierra 

Nevada trends (Bateman and Dodge, 1970).

6. Monzo-syenitic rocks in the Transverse Ranges are 

genetically unrelated to the quartz plutonites.

7. Gabbroic rocks have patterns of geochemical behavior different from the quartz plutonites and probably 

had different sources.

For the present investigation, we have eliminated 

from consideration 23 samples from localities underlain 

by monzo-syenites, and an additional 26 samples from 

localities at which the rocks are gabbroic, for the 

reasons cited and because attempts to develop a model 

with these analyses included in the data gave evidence 

of the petrogenetic differences. A final two samples 

were removed from the San Gabriel block because the 

rocks are probably Miocene in age and genetically are 

unrelated to the batholith (D. M. Morton, oral commun. 

1980). Thus, a total of 497 composite samples from the 

studies summarized have been considered in this investigation.

PETROLOGIC NOMENCLATURE

This report uses the terminology of Bateman and 

others (1963, fig. 2), rather than that of the IUGS (International Union of Geological Sciences) Commission 

(Streckeisen, 1973) for several reasons: (1) for consistency with prior discussions of the same chemical data; 

(2) for consistency with studies in the Sierra Nevada; 

and (3) for flexibility because the Bateman classification
DEVELOPMENT OF THE MODEL

provides five divisions of quartz plutonites whereas the 

IUGS scheme uses only four (effectively three because 

no rocks in southern California fall in the alkali granite 

category).

ACKNOWLEDGMENTS

We are indebted to T. H. McCulloh and V. R. Todd 

of the U.S. Geological Survey and to W. B. Wadsworth 

of Whittier College for helpful criticism of the manuscript.

DEVELOPMENT OF THE MODEL

Chemical variation in nearly all rock bodies has resulted from processes of mixing and unmixing (for example, differentiation), and appropriate petrogenetic 

models are comprised of end-member compositions and 

estimated mixing proportions for representative rock 

samples. The observed compositions of the rock samples 

can be approximated by combining (forming linear combinations of) the end-member compositions according to 

the derived mixing proportions. The first task in the 

development of such a model is to determine the 

number of end members required; the next is to derive 

the end-member compositions. The first task can be accomplished rather objectively by mathematical analysis, 

but the second requires geologic reasoning and speculation as well as mathematics. Once the number of end 

members and their compositions have been determined, 

each individual sample composition can be examined to 

see if it can be approximated by reasonable combinations of the end members. If most or all the samples 

can be explained, the model is said to be mathematically 

adequate. Whether the model is valid or not depends 

on whether the end-member compositions are those of 

the materials that were actually involved in the mixing 

or unmixing processes that caused the compositional 

variations in the rocks. The methods used here serve 

to reject some selected end-member compositions as 

mathematically impossible, but the final selections are 

not unique.

The modeling methods used here have been described 

elsewhere (Miesch, 1976a, b, c) and have been applied 

previously to a variety of petrogenetic problems (for 

example, Miesch and Morton, 1977; Miesch and Reed, 

1979; Miesch, 1979; Stuckless and others, 1981; Stuckless and Miesch, 1981). The mathematical development 

is not repeated here and the reader is referred to the 

cited papers for details.

However, an easily visualized application of the modeling concepts involves the plagioclase feldspar system. 

If one were given a number of feldspar crystals as unknowns (when in reality they were all samples of oligoclase, andesine, labradorite and bytownite), one could

determine analytically that they were composed principally of four oxides: Si02 , A1203 , Na^O and CaO. But, 

the compositions of the plagioclases can be described 

at least approximately in terms of only two end members, albite and anorthite. Similarly, although the 

batholithic rocks of southern California are composed 

mostly of eight major-oxide constituents, we will show 

that the compositions of these rocks can be approximated in terms of only four end members. The end 

members chosen for the plagioclase series, albite and 

anorthite, are conventional, but they are not the only 

end members that could be used. In a study of island 

arcs, for example, An30 and An55 , rather than Ab and 

An, might be appropriate. In fact, the only requirement 

for the plagioclase end members is that they be some 

combination of albite and anorthite. Otherwise, they 

would not be mathematically compatible with the plagioclase series. That is, the compositions of the plagioclase crystals could not be approximated as linear combinations of the end members. Just as there is a choice 

for the plagioclase end members, there is a choice of 

end members that can be used to describe the compositional variation within the batholithic rocks of southern 

California; the choices must be made on the basis of 

both mathematical evidence and geologic observation or 

speculation regarding the materials actually involved in 

the mixing processes.

NUMBER OF END MEMBERS

The data matrix (Appendix 1) consists of 497 rows 

that represent composite samples and eight columns 

that represent the oxide variables: Si02 , A1203 , FeO 

(total iron), MgO, CaO, NagO, K20, and Ti02 . The 497 

rows of the original data matrix were adjusted so that 

the eight variables in Appendix 1 sum to 100 percent 

for each sample. This constant row-sum is required in 

order to recalculate the results of conventional Q-mode 

factor analysis into the end-member compositions and 

mixing proportions that comprise the model. The original data are given in Baird and others (1979) where 

they are keyed with rock-type designations and the UV geographic coordinates identified on figure 3 of this 

report. The average compositions of all samples and of 

the samples from each of the six structural blocks identified in figure 2 are given in table 1. In order to give 

each oxide equal weight in the modeling procedure, 

each column of the matrix was scaled to have the same 

mean and variance, according to a technique described 

previously (Miesch, 1980). Also, in order to treat the 

data for each sample as a vector of unit length, the 

scaled data for each sample were divided through by 

the square root of the sum of squares (that is, normalized). The scaled and normalized data were then regarded as the coordinates of 497 unit vectors with a 

common origin in eight-dimensional space.
BATHOLITHIC ROCKS OP SOUTHERN CALIFORNIA

.12

EXPLANATION

MAJOR FAULT; dashed where inferred 

Sampling locality

33°

50 KILOMETERS

I______

50 MILES

13 14 15

FIGURE 3. Sampling localities in Mesozoic plutonic rocks of the nothern Peninsular and Transverse Ranges, Calif. Locality numbers are

used in Baird and others (1979) for
DEVELOPMENT OF THE MODEL

117°

16 17 18 19 20 21 22 23 24

116° 

25 26

96

.99

SAN BERNARDINO 

BLOCK

116 108

i17 109 no 

,,,= 106 |05

 a4 , 'i2 ° 

181 180 "1 ° 107 

,_ M3 

75 \J6_ |g2 |83 .165 

0 °I84 vv* '»+-&,*%£*

169 170* l7.2

222

LITTLE SAN BERNARDINO BLOCK

211

216 _

' -I90 3»9405 406 447 

.449 4.00 4S5 4.° 6

N. 408 4J7

.410 .415 

404 »4II "414 

 412 *4I3

312° 3i4 SAN JACINTO BLOCK

.326 °3I3

4 99 504 511

 *

5J5 5^0 514 .523 532 «533

423 434 

506 50,9 .515 * 5 22 "531 \ -436

^508 «5I6 .521 "530 *534 .546 \ »437

507 «520 "529 ^35 '545 

 517

 .528 «536 »544

518 .519

 439

 450 »452 

 453 .441

 438 "454 *45 <5

 453 ^^

PERRIS BLOCK

5S4 «525 g

537 .543 .547*557 

545, ..^ ,556

.541 .555

540 549

 550 *553 

 551

I I

15

14

13

I 33°

16 17 18 19 20 21 22 23 24 25 26

keyed to Appendixes 1 and 2 (prefix B has been deleted from locality numbers on map to save space). The U-V coordinate system was 

convenience in referring to sampling localities.
BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

TABLE 1. Average compositions (in percent) of the batholithic rocks within structural blocks of southern California

[All analyses were expressed as oxides and recomputed to 100 percent before computation of averages]

Structural block

San Gabriel block .............................

San Bernardino block........................

San Jacinto block..............................

Perris block .....................................

Number 

of

samples

....... 47

....... 125

....... 25

....... 101

....... 80

4Q7

SiO2

67.10

70.22

69.90

67.54

67.12

68.38

68.32

A1203

16.41

15.45

15.65

16.41

15.99

15.17

15.83

FeO

3.81

2.22

2.56

3.56

4.02

4.07

3.39

MgO

1.58

0.88

1.16

1.45

1.85

1.70

1.44

Oxide

CaO

3.47

2.86

2.59

3.89

4.43

3.99

3.67

NaaO

3.90

3.76

3.87

3.65

3.78

3.91

3.79

Kas-O

3.15

4.06

3.88

2.76

2.23

2.27

2.97

TiO2

0.57

0.55

0.40

0.73

0.59

0.52

0.58

Methods of principal-components analysis were then 

used to project the vectors into two dimensions, then 

three, and so forth up to seven dimensions (one less 

than the number of oxides). After each projection, the 

compositions represented by the projected vectors were 

determined and were compared with the compositions 

represented by the vectors in the original eight-dimensional space. The correlation coefficients between the 

original and recomputed data were determined and 

squared to give coefficients of determination for each 

oxide. These latter values are measures of the variances 

in the original data that can be explained by mixing 

models with two to seven end members, and are summarized in the factor-variance diagram in figure 4. This 

figure clearly shows that the original data can be closely 

approximated as a four-dimensional vector system, or 

as a four-factor, four-component, or four-end-member 

compositional series. Figure 4 shows that a model with 

only three end members would explain only about 71 

percent of the variance in A1203 and that a five-endmember model offers no substantial improvement over 

a four-end-member model. The values of the coefficients 

of determination for four factors range from 0.85 to 0.97 

(fig. 4), indicating that a four-end-member model can 

account for 85-97 percent of the variance in each oxide 

constituent. Thus, 3-15 percent of the variance in each 

constituent is ascribed to analytical imprecision and to 

other factors, such as minor petrologic processes that 

will not be represented in the model. Also, at least 

some part of this unaccounted for variance may be attributed to the fact that the four end-member compositions to be derived, in actuality, rather than being 

fixed, varied somewhat in both space and time. The 

absolute variances accounted for and not accounted for 

by four factors are listed in table 2.

COMPOSITIONAL STRUCTURE

The concept of compositional structure in igneous 

bodies and rock series was described in a previous report (Miesch and Reed, 1979) and refers to the nature

of the relations among the oxide constituents as represented by a factor-variance diagram. These relations 

determine the number of end members that will be required in a petrogenetic mixing model. The compositional structure in the southern California batholithic 

rocks is closely similar to that of the Sierra Nevada 

batholith (Miesch and Reed, 1979, fig. 7). The fact that 

the variances in the eight oxides can be closely accounted for by the mixing and unmixing of four end 

members is not accidental. It has arisen from the fact 

that the southern California batholithic rocks originated 

mostly as a result of a simple combination of processes 

that involved only four dominant compositions, or 

perhaps four compositional extremes. That is, the 

batholithic rocks might have formed mainly by the separation of three independent mafic phases from a 

magma, by the separation of two phases from mixtures 

of two magmas, or by some other process that involved 

four, and only four, dominant end members. A likely 

possibility is that the batholithic rocks formed primarily 

by the separation of differentiates (mineral assemblages) that varied in composition between two end 

members from a magma that also varied within a twoend-member system. We shall assume that the magma 

varied in composition between an end member (which 

we label M-l) derived from near the present continental 

margin and another end member (labeled M-2) derived 

from farther to the northeast. Composition M-l may 

represent a magma that has undergone relatively little 

or no contamination by continental materials, and M-2 

may represent a magma that includes more continental 

material. We shall also assume that the differentiates 

varied between extremes which we shall label D-l and 

D-2. The compositions of the differentiates, presumably, varied with the composition of the magma, temperature, and other local conditions.

Now the task is to estimate the compositions M-l, 

M-2, D-l, and D-2 in the most reasonable way and 

then to describe the compositions of all 497 samples 

in terms of these four components. The only mathematical requirement for each of the four compositions is that 

they be representable as vectors in the four-dimensional
DEVELOPMENT OF THE MODEL

EXPLANATION

D SiO2

O A12O3

A FeO

+ MgO

X CaO

O Na2O

V K20

B Ti02

NUMBER OF FflCTORS

- 0.7

- 0.6

- 0.5

- 0.4

- 0.3

- 0.2

- 0.1

8

0.0

FIGURE 4. Factor-variance diagram for the batholithic rocks of southern California.

TABLE 2. Chemical variances in the batholithic rocks of southern California that can and cannot 

be accounted for by a four-end-member mixing (factor) model

Oxide

SiO*......... ......... . A1203 .. ................

FeO....................

MgO...................

CaO..... ...............

Na20 ..................

K20. ...................

Ti02 ...................

Accounted for

....... 22.3617

........ 1.9365

2 741 9

........ .9547

........ 2.7561

........ .1515

........ 1.1326

0493

Variance

Not accounted for

0 8719

.0656

20R2

.1404

1334

.0089

.1138

.0089

Total

23.2336

2.0018

2 9481

1.0951

2.8895

1604

1.2464

.0582

space that contains the projected sample vectors. Any 

four compositions that can be represented in this manner can be mixed in varying proportions to approximate

the original data to the degree indicated in figure 4 

for a four-factor model and will lead to variances accounted for and not accounted for as listed in table 2.
10 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

The need to select Af-1, M-2, D-l, and D-2 so that 

they can be represented as vectors in the four-dimensional space of the sample vectors is analogous to the 

need to describe the plagioclase compositions in terms 

of combinations of albite and anorthite.

DERIVATION OF THE DIFFERENTIATE END-MEMBERS D-l

AND 0^2

The principal minerals in the quartz diorite, 

granodiorite, and quartz monzonite are quartz, potassium feldspar, plagioclase, hornblende, biotite, and iron 

oxides, chiefly magnetite and ilmenite. Presumably, the 

differentiates that were precipitated from the magmas 

consisted mainly of the least-soluble phases, plagioclase, 

hornblende, biotite, and the iron oxides. Consequently, 

the compositions of end members D-l and D-2 were 

sought by testing mixtures of the compositions of these 

minerals. Plagioclase was represented by the ideal compositions of albite and anorthite, and ideal compositions 

were also used to represent magnetite and ilmenite. 

Biotite was represented by the average of eight 

analyses (table 3) from Larsen and Draisin (1950, p. 

69). Hornblende was first represented by the average

TABLE 3. Biotite and hornblende compositions (in percent) used in 

determination of end-member compositions, D-l and D-2

Oxide Biotite1 Hornblende2

Si02 ... .................

A1203 .... ..............

FeO. ...................

MgO.. .................

CaO....................

NagQ ..................

Ksf). ...................

Ti02 ...................

37.96

17.70

21.20

9.52

..... 0.39

...... 0.22

9.49

3.51

47.57

8.64

17.46

11.22

11.82

1.18

0.72

1.37

'Average of eight analyses from Larsen and Draisin (1950, p. 69). 

2Analysis 7 from Larsen and Draisin (1950, p. 71).

of eleven analyses given by Larsen and Draisin (1950, 

p. 71), then by the average analysis of the six 

hornblendes from nongabbroic rocks, and finally by the 

individual analyses. The best results were achieved 

using the single hornblende analysis given in table 3. 

A computer program similar to the EQSCAN program 

described previously (Miesch, 1976c) was used to form 

53,130 systematic mixtures of the six selected compositions. The value 53,130 is the number of points at 5-percent increments within the six-dimensional space representing the six compositions. Each mixture was represented as a unit vector in the original eight-dimensional space of the 497 sample vectors, and then projected into the four-dimensional space containing the 

projected sample vectors. After each projection, the 

vector communality (square of vector length) was computed and taken as a direct measure of the nearness 

of the original unit vector to the four-dimensional subspace. The average communality of the 497 sample vectors in four-dimensional space is 0.9951. Of the vectors 

representing the 53,130 mathematical mixtures, only a 

few were represented by vectors with communalities 

this high. The two that led to the highest communalities 

were mixtures of (1) 33.9 percent anorthite, 63.3 percent hornblende, 0.9 percent magnetite, and 1.9 percent 

ilmenite (assemblage 1); and (2) 60.6 percent albite, 35.5 

percent anorthite, 2.0 percent magnetite, and 1.9 percent ilmenite (assemblage 2). No biotite is included in 

either mixture. Thus, of all possible combinations of plagioclase, hornblende, biotite and the iron oxides, these 

two assemblages, and any combinations of them, come 

closest to satisfying the mathematical requirements for 

the differentiates, D-l and D-2. The requirements of 

the model are perfectly satisfied, however, by the two 

vectors representing these compositions after projection into the four-dimensional space. The compositions 

represented by the projected vectors are given in table 

4 (D-l and D-2) along with the compositions repTABLE 4. Compositions (in percent) of two mineral assemblages and end members D-l and

D-2

Oxide

Mineral assemblage1

Assemblage 1 Assemblage 2

End member

D-l D-2

Si02... .............

A1203 .. ............

FeO... ......... ....

MgO...............

CaO................

NajjO ..............

K20. ...............

Ti02 . ..............

44.75

17.89

12.87

7.10

14.31

0.75

0.46

1 88

57.00

24.81

2.87

0.00

7.16

7.16

0.00

1.00

44.68

18.49

13.01

8.01

12.81

0.72

0.42

1.83

56.31

25.12

3.55

0.44

5.91

7.39

0.14

1.13

"Assemblage 1 contains the following percentage concentrations of minerals: anorthite, 33.89; hornblende (see table 3), 63.27; 

magnetite, 0.91; and ilmenite, 1.92. Assemblage 2 contains the following percentage concentrations of minerals: albite, 60.59; 

anorthite, 35.53; magnetite, 1.97; and ilmenite, 1.90.
DEVELOPMENT OF THE MODEL 11

resented by the vectors before projection (assemblage 

1 and assemblage 2). The bulk compositions of all materials precipitated from the magmas in the formation 

of the observed samples, therefore, are assumed to 

have ranged between composition D-l and composition 

D-2. Materials rich in D-l and sparse in D-2 contained 

a more calcic plagioclase and were more mafic. Those 

rich in D-2, on the other hand, contained a more sodic 

plagioclase and were more felsic.

DERIVATION OF THE MAGMA END-MEMBERS M-l AND M-2

The remaining problem is to estimate the compositions of the extremes, M-l and M-2, in the range of 

magmas from which the batholithic rocks were derived. 

Like compositions D-l and D-2, compositions M-l and 

M-2 must also be representable as vectors in the fourdimensional space of the 497 sample vectors. But, an 

additional requirement in the selection of compositions 

M-l and M-2 pertains to the mixing proportions that 

will be required for the 497 samples. Acceptable mixing 

proportions will necessarily be positive for magma compositions M-l and M-2 and must be generally negative 

for differentiate compositions D-l and D-2, inasmuch 

as the differentiates should be separated from the magmas, not added to them, in the formation of most of 

the batholithic rocks. If compositions M-l and M-2 are 

selected arbitrarily, for example, many samples may 

require negative proportions of M-l and (or) M-2. Also, 

some samples may require opposite signs in the mixing 

proportions for D-l and D-2, suggesting that the differentiates separated from the magmas had bulk compositions outside the range for D-l and D-2 (table 4); 

possibly the required bulk composition of the differentiate may be partly negative. In addition, the mixing 

proportions must not be large in absolute value. The 

sum of the mixing proportions for M-l, M-2, D-l and 

D-2 will always equal unity, so if the sum of those for 

M-l and M-2 equals 20, for example, the sum of those 

for D-l and D-2 must equal minus 19. Mixing proportions such as these would indicate that the specific sample resulted from a differentiation process that went 

95 percent of the way towards completion possible for 

some individual samples, but not likely for any large 

mass of batholithic rocks.

The two structural units within the region that are 

the most widely separated in a direction perpendicular 

to the continental margin are the Santa Ana and San 

Bernardino blocks (fig. 2). The chemical data for samples from these two blocks were extracted from the 

main data matrix (Appendix 1) and were examined by 

independent factor analyses of the same type used to 

examine the entire data set. Factor-variance diagrams 

for the two subsets of the data are given in figures 

5 and 6. Both diagrams indicate that the chemical data

from the corresponding structural blocks can be well 

represented in three-dimensional vector systems. 

Stereograms showing the configurations of the vector 

systems are given in figures 7 and 8; the compositions 

represented by selected vectors on the stereograms are 

given in tables 5 and 6. Tables 5 and 6 may be used 

to observe the nature of compositional changes in various directions across the stereograms. Note that both 

configurations of sample vectors (figures 7 and 8) are 

approximately triangular and that those points near the 

lower left corners represent compositions relatively low 

in Si02 and high in FeO and MgO, whereas those points 

to the right represent more siliceous compositions. The 

compositions of the parent magmas for each of these 

groups of samples seem to be at or near the point "N" 

on the corresponding stereogram; the compositions represented by these points are given in tables 5 and 6. 

These compositions were represented as vectors in the 

four-dimensional space of the 497 sample vectors. They 

were then taken tentatively as the M-l and M-2 vectors being sought and as representing two of the end 

members for the model. Vectors D-l and D-2, previously deduced as representative of the range of precipitates separated from the magmas to form the 

batholithic rocks, were taken to represent the other two 

end members. We found, however, that the compositions of many samples could be approximated in the 

mixing computations only by using negative proportions 

of composition M-l. Consequently, alternative compositions for M-l and M-2 were sought by trying vectors 

in the same plane as those representing M-l and M-2, 

but separated by a wider angle. This procedure led to 

the identification of the compositions M-l and M-2 

listed in table 7. The four end-member compositions 

given in table 7 can be mixed in various proportions 

(Appendix 2) to approximate the compositions (to the 

degrees indicated for four factors in fig. 4 and table 

2) of all 497 samples (Appendix 1). With the exception 

of one sample, all the proportions for end members M-l 

and M-2 are positive and in the range from:

M-l 

M-2

Minimum 

0.0 

0.0

to 

to

Maximum 

2.5641 

1.8051

With the exception of 16 samples, the mixing proportions for D-l and D-2 are of the same sign and in the 

range from:

Minimum Maximum 

D-l -1.4776 to 0.1996 

D-2 -1.0498 to 0.1304

Only a few of the samples required positive mixing 

proportions for D-l and D-2, indicating that compositions D-l and D-2 must be subtracted from compositions M-l and M-2 in order to approximate the compo-
12 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

D SiO2 

O A12O3 

A FcO

MgO 

X CaO 

O Na2O 

V K20

TiO2

4567

NUMBER OF FflCTORS

8

FIGURE 5. Factor-variance diagram for the batholithic rocks of the Santa Ana block of southern

California.

sitions of most samples. The compositions of the 16 samples that require mixing proportions of opposite sign 

for D-l and D-2 can be produced from compositions 

M-l and M-2 only by adding or subtracting compositions that include negative values for one or more 

oxides. Therefore, these 16 samples and one (B429)2 

that requires a negative amount of M-l are not accounted for by the model proposed here. Of the 17 

anomalous samples, 11 are from the San Jacinto block 

(B226, B229, B283, B286, B301, B302, B303, B304, 

B306, B308, and B321), 4 from the Perris block (B338, 

B392, B420, and B429), and 1 each from the San Bernardino (B99) and Santa Ana blocks (B513). The 

anomalous samples are discussed in a later section of 

this report.

' See figure 3 for sampling localities and Appendix 1 for the analyses.

CHARACTERISTICS OF THE MODEL

PETROLOGY OF THE MAGMA END-MEMBERS 

M-l AND M-2

The normative mineralogy of M-l (table 7) is that 

of a saturated basaltic or gabbroic rock. The 26 gabbro 

compositions (heretofore not considered in the modeling) were each tested for compatibility with the more 

silicic rocks of the Santa Ana block by computation of 

vector communalities. The two gabbros most compatible (highest communalities) are B545 and B511 (table 

8). The compositions of these two samples need only 

be slightly modified to be perfectly representable as 

vectors (G-l and G-2) in the three-dimensional vector 

space formed by the Santa Ana block sample compositions (fig. 7). The compositions represented by vectors
CHARACTERISTICS OF THE MODEL 13

CU

0.0

EXPLANATION

D SiO2

O A1203

A FeO

+ MgO

X CaO

O Na2O

V K20

H TiO2

3456

NUMBER OF FflCTORS

- 0.7 

I- 0.6 

I- 0.5

- 0.4

- 0.3 

I- 0.2

- 0.1 

0.0

8

FIGURE 6. Factor-variance diagram for the batholithic rocks of the San Bernardino block of southern

California.

G-l and G-2 are given in table 8. The compositions 

are notably close to that of end member M-l (table 

7). Nockolds and Alien (1953) used variation diagrams 

to deduce the compositions of parental magmas for calcalkaline rocks. Their average values, compared with M1 (table 7), are only slightly higher in MgO and K20, 

and slightly lower in FeO and CaO.

Because both compositions M-l and M-2 (table 7) 

were derived by mathematical procedures, we were interested in determining how closely they correspond to 

actual rock compositions. Although composition M-l is 

close to the compositions of some gabbros from the region, as pointed out in the preceding paragraph, none 

of the batholithic rocks have compositions close to composition M-2. Consequently, a search was made of the 

RASS computer-based file (Van Trump and Miesch, 

1977) which contains about 130,000 rock analyses by

laboratories of the U.S. Geological Survey since 1967. 

The analyses are of samples collected throughout the 

United States. The igneous rock analyses in the RASS 

file closest to compositions M-l and M-2 are given in 

table 9. The measure of closeness used was cosine theta 

of Imbrie and Purdy (1962). The closest match to M-l 

is a gabbro of Jurassic age from the Alaska-Aleutian 

Range batholith (Reed and Lanphere, 1973). The 

closest matches to M-2 are an andesite from southwest 

Nevada and tuffaceous rocks from southwest Colorado 

and northern Washington, all of Tertiary age. The average norm for these matches to M-2 includes 16 percent 

quartz, 23 percent orthoclase, and 53 percent sodic andesine, consistent with a leucocratic granodiorite. Composition M-2 is incompatible with any magma or source 

material of an oceanic nature.

One possible origin for end-member M-2 is by mixing
14 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

-1.0-0.8-0.6-0.4-0.2 0.0 0.2 0.4 0.6 0.8

' -1.0-0.8 -0.6-0.4 -0.2 0.0 0.2 0.4 0.8 1.0

FIGURE 7. Sterogram showing the three-dimensional vector system for the batholithic 

rocks of the Santa Ana block of southern California. Open circles represent 80 sample 

vectors. Dashed line outlines area wherein all vectors represent compositions that are 

entirely nonnegative. All vector projections have been from an upper hemisphere vertically onto the plane of the stereogram. See table 5 for compositions represented by 

vectors A through N.

TABLE 5. Compositions represented by some points on figure 7

Oxide

Si02 ........ .........

A1203 ... ............

FeO.................

MgO................

CaO.................

NagO .............. .

K20. ................

Ti02 ................

71 46

............ 15.75

............ 3.29

............ 0.00

............ 2.63

............ 6.08

............ 0.40

............ 0.39

74.67

14.03

2 27

0.00

1 6Q

4.78

2.29

0.26

77 7Q

12.35

1 2Q

0.00

0.77

3.52

4.14

0.14

80 45

10.82

0 44

0.09

0.00

2.29

5.88

0.03

81.20

Q Ifi

.011

1 04

0.05

0.05

8.39

0.00

65.97

13.29

4 fi2

4.10

5.38

0.00

6.01

0.62

51.52

17.23

8.90

6.98

10.43

0.00

3.72

1.21

37.21

21.15

13.13

9.83

15.44

0.00

1 43

1 7Q

32.12

22.91

14.67

10.56

17.14

0.59

0.00

2.00

48.31

20.07

9.99

6.14

11.15

3.01

0.00

1 34

56.70

18.59

7.57

3.85

8 04

4.25

0.00

0 QQ

62.04

17.65

6.03

2.39

6.07

5.05

0.00

0.78

68.47

16.52

4.17

0.63

3.69

6.01

0.00

0.51

54.30

18.60

8.23

4.81

9.02

3.27

0.67

1 OQ

of the gabbroic magma represented by M-l with a partial melt from the continental crust. For example, composition M-2 of table 7 could have been produced by 

mixing 11.76 percent magma of composition M-l with 

88.24 percent melt with a composition as follows:

SiO2 A12O3 

68.02 18.70

FeO MgO CaO Na2O K2O TiO2 

1.29 0.00 2.76 4.78 3.79 0.67

The equivalent normative composition is:

Q

19.2

C

1.7

Or 

22.4

Ab 

40.4

An 

13.7

MIXING PROPORTIONS

Fs 

1.7

II 

1.3

A statistical summary of the mixing proportions for 

the four end members, as required for the 480 samples 

accounted for by the model, is given in table 10. Some 

parameters derived from these values are summarized 

in table 11. The first of these parameters is the sum
CHARACTERISTICS OF THE MODEL

,-1.0-0.8-0.6-0.4-0.2 0.0 0.2 0.4 0.6 0.8

15

' -1.0-0.8 -0.6 -0.4 -0.2 1.0

FIGURE 8. Stereogram showing the three-dimensional vector system for the batholithic 

rocks of the San Bernardino block of southern California. Open circles represent 

125 sample vectors. Dashed line outlines area wherein all vectors represent compositions that are entirely nonnegative. All vector projections have been from an upper 

hemisphere vertically onto the plane of the Stereogram. See table 6 for compositions 

represented by vectors A through N.

TABLE 6. Compositions represented by some points on figure 8

Oxide M

Si02 ... ..............

A1203 .. .............

FeO.... .............

MgO....... .........

CaO. ................

NazO ...............

K20.... .............

Ti02 ................

............ 68.12

90 OQ

............ 0.02

............ 0.00

............ 3.51

............ 6.63

1 90

n 49

72.37

16.50

0 98

0.00

2.31

4.75

3.41

0.36

7C OQ

14.04

n 4fi

0.00

1 4Q

3.46

4 04

n qq

77.16

12.44

O

KO

0.00

0.96

2.62

C QO

0.30

80.54

9 CO

0 84

0.00

0.01

1 08

7.72

0.26

80.06

8.04

2 is

0.60

0.11

0.00

8.64

0 °,7

aa oc

1 fi CQ

7 SQ

3

00

3.85

0.00

fi Q7

1 no

4Q Q0,

10 OO

14 49

6

CC

8.27

0.00

5.01

I CO

Q 04

91 77

30.64

14.60

19.10

0.23

0.00

q 70

OO O1

21.85

17.85

8.53

12.88

3.30

0.00

2.36

46.51

91 QQ

10.52

5.05

9.32

5.08

0.00

1 58

55.78

91 Ofi

5.43

9 fi4

6 84

6.30

0.00

1 04

62.86

22.02

1.51

0.78

4.95

7.26

0.00

0.62

56.67

18.33

7.55

3.52

6.54

3.96

2.25

1.18

of the mixing proportions for end members M-l and 

M-2, which gives the amount of magma from which 

each unit amount of sample was derived. The mean 

value of this parameter for all 480 samples is 1.8744, 

indicating that, according to the model, the average 

sample was formed by removal of 0.8744 parts of the 

differentiates (D-l and D-2) from 1.8744 parts of 

magma (M-l plus M-2); this corresponds to differentiation of about 47 percent. Inspection of the mean values 

for batholithic rocks from the individual structural

blocks (table 11) shows that those for the San Jacinto 

block call for the least amount of differentiation and 

that, in general, the amount of differentiation required 

tends to increase from the northeast to the southwest. 

This regional variability is also apparent from the map 

of individual sample values for this parameter in figure 

9. (Note: The class intervals in figures 9-12 are defined 

by the 20th, 4Qth, 60th, and 80th percentiles of the 

mapped variable.) 

The second parameter derived from the mixing pro-
16 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

TABLE 7. Chemical and normative compositions of the end members for the mixing model

End member

M-l M-2 D-2 D-2

Chemical composition (in percent)

Si02 ... .....................

A1203 ... ...................

FeO................. .......

MgO.. .....................

CaO.. .................... ..

NagO ......................

K20. .......................

Ti02 .......................

.............. 54.41

.............. 18.37

.............. 8.86

.............. 4.76

.............. 8.89

.............. 3.18

.............. 0.30

.............. 1.24

66.42

18.66

2.18

0.56

3.48

4.59

3.38

0.74

44.68

18.49

13.01

8.01

12.81

0.73

0.42

1.83

56.31

25.12

3.55

0.44

5.91

7.39

0.14

1.13

Normative composition (in percent)

Q. .........................

C. .........................

Or.........................

Ab ........................

An........................

Ne ........................

Wo........................

En ........................

Fs. ........................

Fo. ........................

Fa.........................

11..........................

4 9

............... 0.0

1 7

............... 26.9

............... 35.0

............... 0.0

............... 3.8

............... 11.9

14 9

............... 0.0

............... 0.0

............... 2.4

17.3

1.1

20.0

38.8

17.2

0.0

0.0

1.4

2.8

0.0

0.0

1.4

0.0

0.0

2.5

6.2

45.9

0.0

7.4

8.3

8.7

8.2

9.4

3.5

0.0

2.1

0.8

59.8

29.3

1.5

0.0

0.0

0.0

0.8

3.6

2.1

TABLE 8. Compositions (in percent) of two samples of gabbros and the compositions represented

by vectors G-l and G-2 on figure 7

Sample Vector

Oxide B545 B511 G-l G-2

Si02.... ....................

A1203 .. .................. ..

FeO........................

MgO.......................

CaO........................

NagO ......................

K20. .......................

Ti02 .......................

.............. 53.96

.............. 18.01

.............. 8.86

.............. 5.04

.............. 9.14

.............. 3.17

.............. 0.71

.............. 1.13

53.02

19.25

8.71

4.73

9.66

3.19

0.44

1.00

53.89

18.64

8.35

4.96

9.18

3.15

0.74

1.11

52.65

19.02

8.72

5.16

9.60

3.23

0.46

1.16

portions is the percentage of end member M-2 in the 

total magma (M-\ plus M-2) required for each sample. 

The mean values (table 11) and the map of individual 

values (fig. 10) show that this parameter increases from 

the southwest to the northeast, suggesting that the 

more silicic and potassic extreme, M-2, was only a 

minor component in the magmas that formed the rocks 

of the Santa Ana and Perris blocks, but a major component in the magmas farther to the northeast. A major 

discontinuity in the map pattern on figure 10 occurs 

near the San Jacinto fault, in the eastern part of the 

Perris block. This discontinuity is discussed further in 

the next section of this report.

The third parameter is the percentage of end member 

D-2 in the total of the differentiates (D-l plus D-2) 

that separated from the magmas to yield the liquids

that later crystallized to form each sample. The mean 

values (table 11) and the map of individual values (fig. 

11) show that this parameter is somewhat higher for 

the easternmost blocks of batholithic rocks, indicating 

that, according to the model, the precipitates in the 

eastern part of the region included a more sodic plagioclase and less hornblende than those farther west in 

the Santa Ana and Perris blocks. The discontinuity in 

the pattern of figure 10 is also present in figure 11, 

but is somewhat less distinct.

REGIONAL VARIATION IN THE COMPOSITIONS OF 

THE MAGMAS AND DIFFERENTIATES

The compositions of the magmas and, presumably, 

the source materials required for each of the 480 samples, according to the model, can be determined by
CHARACTERISTICS OF THE MODEL 17

TABLE 9. Analyses from the U. S. Geological Survey RASS data file that compare closely with end-member compositions M-1 and M.-2

[Analyses of end members M-1 and M-2 are from table 7. See NOTE for description of samples (from RASS data file) for analyses 1-7. All analyses were recomputed to sum to

100 percent]

M-1 M-2

Si02 ... ................................................. 54.41 54.01 66.42

A1203 ... ............................................... 18.37 19.06 18.66

FeO..... ............................................... 8.86 8.39 2.18

MgO.... ............................................... 4.76 4.92 .56

CaO. ................................................... 8.89 8.61 3.48

NagO .............. .................................... 3.18 3.48 4.59

K20. ...... ............................................. .30 .52 3.38

Ti02 ................................................... 1.24 1.00 .74

NOTE. Description of samples for analyses 1-7:

Analysis 1. Gabbro of Jurassic age from southern Alaska, collected by B. L. Reed, 1970.

Analysis 2. Andesite of Eocene age from southwest Nevada, collected by D. P. Crowder, 1969.

Analysis 3. Quartz-latite welded tuff of Oligocene age from the San Juan Mts., Colo., collected by R.

Analysis 4. Welded tuff of Oligocene age from the Sand Juan Mts. , Colo. , collected by R. G. Luedke,

Analysis 5. Crystal-rich welded tuff of Oligocene age from the Sand Juan Mts., Colo., collected by R.

66.05

18.78

3.17

.38

3 44

3.86

3.76

.56

G. Luedke,

1970.

G. Luedke,

Analysis 6. Quartz-latite welded tuff of Oligocene age from the San Juan Mts., Colo., collected by P. W. Lipman,

Analysis 7. Volcanic tuff of Eocene age from northern Washington, collected by R. C. Pearson, 1973.

65.90

18.22

3,27

o

/\

4

1969.

1970.

1974.

61

Q7

30

90

53

65.56

18.19

3.21

.74

3.35

4.27

4.17

.50

65.49

18.43

3.18

.76

3.50

4.12

4.02

.49

66.58

18.67

2.33

.42

3.39

3.59

4.62

.40

66.39

18.75

2.53

.76

3.79

5.22

2.15

.41

TABLE 10. Statistical summary of mixing proportions required for the batholithic rocks within structural blocks of southern California

Structural block

San Gabriel block ......................

Little San Bernardino block........

Perris block ..............................

Number 

of 

samples

47

124

25

90

115

7Q

480

End member

M-1

0.8805 

0.6422 

0.8778 

0.7294 

1.2651 

1.6256 

1.0053

M-2

Mean

0.8571 

1.1517 

1.0627 

0.8825 

0.6742 

0.6400 

0.8691

D-l D-2 M-1 M-2 D-l D-2

Standard deviation

-0.3889 

-0.3376 

-0.4678 

-0.2816 

-0.5421 

-0.7744 

-0.4598

-0.3488 

-0.4563 

-0.4727 

-0.3303 

-0.3973 

-0.4912 

-0.4146

0.2284 

0.1828 

0.2997 

0.2681 

0.3547 

0.3828 

0.4645

0.2924 

0.2756 

0.2691 

0.2459 

0.2669 

0.3055 

0.3394

0.1809 

0.1321 

0.1846 

0.1958 

0.2711 

0.3581 

0.2883

0.1875 

0.1760 

0.1528 

0.1872 

0.2105 

0.2422 

0.2062

TABLE 11. Mean values of parameters computed from the mixing proportions summarized

in table 10

Structural block

San Gabriel block ......................

San Bernardino block.................

Little San Bernardino block........

San Jacinto block.......................

Perris block ..............................

Santa Ana block........................

All batholithic rocks...................

Relative amount of 

crust from which 

batholithic rocks 

were derived

1.7377

1.7938

1.9405

1.6119

1 Q3Q4

2.2656

1.8744

Percentage of M-2 

in crustal material 

(M-1 plus M-2) from 

which the batholithic 

rocks were derived

48.68

63.74

55.04

55.08

34 71

97 1?

47.21

Percentage of D-2 

in materials (D-l 

plus D-2) separated 

from the crust to form 

the batholithic rocks

47.26

57.12

51.04

56.19

41.75

38.04

48.84

mathematical mixing of end members M-1 and M-2 

(table 7) according to the mixing proportions derived 

for each sample (Appendix 2), followed by adjustment 

of each mixture so that the sum of the oxide values 

is 100 percent. The average compositions of the magmas

required for each structural block, and for the 

batholithic rocks as a whole, are given in table 12. Note 

that the magma composition required for the batholithic 

rocks of the Little San Benardino and San Jacinto 

blocks, on opposite sides of the San Andreas fault zone,
18 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA 

118° 117°

=y yyaa -n=nyD

EXPLANATION

MAGMA

(RELATIVE AMOUNT) 

 > 2.25

D 1.94 to 2.25

D 1.73 to 1.94

B 1.50 to 1.73

- < 1.50

FAULT ZONE; dashed where inferred

25

_,_I

50 KILOMETERS

0 25 50 MILES 

FIGURE 9. Relative amounts of magma required for the formation of the batholithic rocks.

are almost identical even though the average compositions of the samples from these two blocks are somewhat different (table 1). Average compositions of the 

differentiates that were separated from the magmas to 

form the batholithic rocks are given in table 13; these 

averages were obtained from compositions D-l and D-2 

in table 7 and the mixing proportions for these end 

members in Appendix 2.

Maps of chemical variation in the batholithic rocks 

of southern California, as determined from the original 

data (Appendix 1) on the 480 samples accounted for 

by the model, are given in figure 12. This figure also 

shows the areal compositional variations in the magmas 

and in the differentiates according to the model. As 

described previously, the original chemical data show 

continuous patterns of areal change from the southwest 

toward the continental interior. In marked contrast, 

most maps of model-derived parameters (figs. 9-11) 

and compositions of magmas and differentiates (fig. 12) 

show pronounced discontinuities near the boundary between the Perris and San Jacinto blocks, within the

Peninsular Ranges Province. The exact locations of 

these discontinuities differ slightly from map to map. 

Nevertheless, we regard the discontinuity as a single 

feature, although of uncertain exact location. No other 

feature is as prominent in these map patterns as is this 

discontinuity. Certainly, the San Andreas fault, both 

east of the Peninsular Ranges and through the Transverse Ranges, does not correlate with any map pattern 

as significant as the discontinuity near the San Jacinto 

fault trace. In fact, if these maps, derived from the 

model, were used to establish petrologic provinces, two 

such provinces would emerge: one composed of the San 

Gabriel, San Jacinto, San Bernardino, and Little San 

Bernardino blocks and another composed of the Perris 

and Santa Ana blocks.

ANOMALOUS SAMPLES

The distribution of sampling localities whose chemical 

compositions are not accounted for by the model proposed here is far from random; 11 of 17 are in the San
119"

CHARACTERISTICS OF THE MODEL 

118° 117°

19

116°

34°

33°

DBB 

BB B

BBB BBBB

BBDDD 

BDBDB 

BBBBB EXPLANATION

END MEMBER M-2 IN 

MAGMA (PERCENT) 

B > 61

B 50 to 61

D 38 to 50

si 31 to 38

- < 31

 FAULT ZONE; dashed where inferred

50 KILOMETERS

50 MILES

FIGURE 10. Percentages of end-member M-2 in the magmas.

Jacinto block. Further, 8 of the 11 localities are tightly 

clustered (fig. 3) in the easternmost part of the block. 

On the basis of strontium and oxygen isotopes, Taylor 

and Silver (1978, p. 425) interpreted the batholithic 

rocks of the San Jacinto block to be anomalous and "derived from a distinctive source rock at depth." Further, 

high values of 8 180, exceeding +10 in the easternmost 

San Jacinto block, show an anomalous circular low that 

coincides with the cluster of eight sampling localities 

that are anomalous with respect to our model (fig. 3). 

With two exceptions in the Perris block, all other 

anomalous localities are at or near the exposed margins 

of the batholithic rocks, or in the zones of faulting that 

mark the boundaries between blocks.

RELATIONS TO OTHER GEOLOGIC FEATURES

The discontinuity in the areal distributions of the 

model parameters and compositions derived from the 

model correlate well with a number of field relations, 

age relations, and petrologic and structural features of

the batholithic and pre-batholithic rocks. However, except that the most pronounced breaks in the map patterns occur near the San Jacinto fault, there is a poor 

correlation with the pattern of major faults and especially no correlation with the San Andreas fault zone. 

This lack of correlation is surprising in view of the huge 

displacements widely accepted (for example, Crowell, 

1979) for the San Andreas fault in southern California.

Regional asymmetries that appear to correlate with 

the discontinuity in the model parameters have been 

described by many investigators working over a larger 

area than that considered here. In each of the asymmetries, regional gradients are interrupted by sharp 

changes in the eastern Peninsular Ranges, near the 

trace of the San Jacinto fault:

1. Pre-batholithic rock types. Metavolcanic rocks in 

the west are succeeded eastward by metasedimentary 

rocks (Gastil and others, 1978) over much of the length 

of the Peninsular Ranges. A belt of carbonate (shelf?) 

rocks has been recognized in the Transverse Ranges 

(Woodford, 1960). The overall west-to-east sequence
20 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA 

118° 117°

mamma DBDD

BIB

 D D

 ggy DM

EXPLANATION

END MEMBER D-2 IN 

DIFFERENTIATES (PERCENT) 

 > 57

50 to 57

43 to 50

38 to 43 

< 38 

FAULT ZONE; dashed where inferred

 D 

33°-

0 25 50 KILOMETERS

J______

0 25 50 MILES 

FIGURE 11. Percentages of end-member D-2 in the differentiates.

seems to be blueschist-metavolcanic-metasedimentary 

(clastic)-metasedimentary(carbonate). Batholithic rocks 

are emplaced in all types, except in blueschist. The 

most mafic parts of the batholithic rocks are associated 

with the metavolcanics, and the most felsic with 

metasedimentary rocks; this change is at or close to 

the boundary of the Perris and San Jacinto blocks.

2. Wallrock metamorphism. Metamorphic grade increases eastward, with an abrupt increase in grade to 

higher amphibolite facies across a line in the central 

to eastern Perris block (Schwarcz, 1969).

3. Plutonic rock types. Gabbroic rocks are restricted to the Santa Ana block and the western part 

of the Perris block (Baird and others, 1979) and similar 

relations are noted farther south (Gastil and others, 

1975; Todd and Shaw, 1979). Granodiorite dominates 

in the San Jacinto block and quartz diorite in the Perris 

block (Baird and others, 1979, fig. 4). This change may 

mark the "quartz diorite boundary" of Moore (1959) in 

this region and is coincident with the discontinuities apparent in figure 10 and in the maps in figure 12 that 

represent the magmas and, presumably, their source 

materials.

4. Plutonic rock mineralogy. Rocks east of a generally north-south line through the Perris block tend to 

be distinctly richer in potassic feldspar, commonly present as large phenocrysts, and richer in sphene (D. M. 

Morton, oral commun., 1981; Gastil and others, 1975).

5. Plutonic rock structure and form. Plutons of the 

western Peninsular Ranges tend to be small, contain 

internal structures that suggest flow and (or) deformation, and have contact relations that suggest syntectonic emplacement (D. M. Morton, oral commun., 1980; 

Todd and Shaw, 1979). The eastern Peninsular Ranges 

and eastern Transverse Ranges are dominated by 

larger plutons that have irregular outlines and massive 

interiors; they are characteristically post-tectonic (Todd 

and Shaw, 1979).

6. Radiometric ages. The extensive uranium-lead 

zircon dating program conducted by Silver and col-
DISCUSSION 21

TABLE 12. Average compositions (in percent) of the magmas for the batholithic rocks within structural blocks of southern California

Structural block

San Jacinto block.......................

Number 

of

samples

47

124

25

90

115

79

480

SiO2

60.26

62.06

61.02

61.00

58.58

57.67

60.08

A1203

18.51

18.55

18.53

18.53

18.47

18.45

18.51

FeO

5.61

4.60

5.18

5.18

6.54

7.05

5.71

MgO

2.72

2.09

2.45

2.46

3.30

3.62

2.78

Oxide

CaO

6.26

5.44

5.91

5.92

7.01

7.42

6.34

Na.0

3.86

4.08

3.95

3.95

3.67

3.56

3.84

K2O

1.80

2.26

1.99

1.99

1.37

1.13

1.75

TiO2

0.99

0.92

0.96

0.96

1.06

1.10

1.00

TABLE 13. Average compositions (in percent) of differentiates separated from the magmas to form the batholithic rocks within structural

blocks of southern California

Structural block

San Gabrial block ......................

San Bernardino block.................

Little San Bernardino block........

San Jacinto block.......................

Santa Ana block........................

All batholithic rocks...................

Number 

of

samples

47

124

25

Qft

IIC

70

480

SiO2

K(\ ia

51.32

50.62

51.22

40 ivl

40 in

50.36

A1203

21.63

22 28

21.88

99 99

21.26

21 ft9

91 7q

FeO

8 54

7.61

8.18

7.70

9.06

9 4.1

8.39

MgO

4 44

3.69

4.15

3.76

4.85

5

10

4.32

Oxide

CaO

9 *55

8 87

0 90

9 oq

10.19

Q 44

Na.0

3

88

A cq

4.13

4.47

q ci

3.26

3 Q8

K20

0 29

0.26

0.28

0.26

0.30

O qi

ft 9R

Ti02

1 'SO

1.43

1.47

1 44

1 <vt

1 49

leagues (summarized in Silver and others, 1979) has 

demonstrated an age "step" at 105 m.y. (million years) 

along a boundary coincident with the change from syntectonic to post-tectonic plutons noted in paragraph 5 

older plutonic dates to the west, younger to the east. 

(Potassium-argon dates are also available, but these 

present further problems of varying cooling histories 

and argon retentions not relevant to this paper.)

7. Isotopic and trace-element patterns. Strongly 

correlated with the age "step" (paragraph 6) is an abrupt increase in 8180 (Taylor and Silver, 1978; further 

discussed in Silver and others, 1979) over normal igneous values of +6 to +8 in the west to +9 to +11 

in the eastern part of the Peninsular Ranges. Contours 

of 8180 values trend more northerly than do the 

strikes of major fault zones and do not appear significantly offset by the faults. The step crosses the Perris 

block coincident with the other changes just noted. 

Other isotopic and trace-element data (strontium, rareearth elements) show close correlations to the patterns 

of oxygen data (Gromet and Silver, 1979; Silver and 

others, 1979).

The choice of end members M-l and M-2 was not 

totally objective, but the derived map patterns are not 

highly sensitive to these choices. M-l and M-2 can be 

changed significantly without eradicating the marked

discontinuity near the San Jacinto fault zone. On the 

other hand, the map patterns can be eradicated almost 

completely by radical changes in the choice of end-member compositions. The most common difficulty with the 

alternative models that result, however, is that they 

call for far greater degrees of differentiation than the 

model proposed here.

In summary, the model calls for a regional discontinuity in the compositions of the magmas and in the 

compositions of the differentiates separated from them. 

The discontinuity in the magmas is presumed to represent a discontinuity in the compositions of the magma 

source materials. The discontinuity occurs mainly in the 

vicinity of the San Jacinto fault zone near the center 

of the Perris block, and corresponds generally to the 

location of other geochemical, mineralogical, petrological, radiometrical and structural discontinuities. In addition, most of the 17 samples found to be anomalous 

with respect to the other 480 are from a part of the 

region identified as anomalous in previous studies of 

strontium and oxygen isotopes.

DISCUSSION

Investigations cited and summarized in this paper are 

leading toward some firm conclusions about the origins 

of at least the Peninsular Ranges part of the southern
22 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

California batholithic rocks. The batholithic rocks are 

divided longitudinally into a western belt made up of 

older syntectonic plutons of quartz diorite and abundant 

gabbro that were derived from upper mantle rocks of 

a primitive nature, and an eastern belt of chiefly 

younger post-tectonic plutons of mainly granodiorite 

and quartz monzonite of a nonprimitive nature (Taylor 

and Silver, 1978). The oxygen-isotope data indicate that 

the eastern source materials once occurred in a nearsurface environment. Baird, Baird, and Welday (1974) 

and Todd and Shaw (1979) concluded, on separate 

grounds, that the gabbroic magmas were distinct from 

those that supplied the quartz plutonites. Silver and 

colleagues proposed (see summary in Silver and others, 

1979) that sources of the Peninsular Ranges rocks were 

fundamentally basaltic; rare-earth-element patterns 

show that variations in source rocks, not high-level 

crystal fractionation or differentiation, were responsible 

for zonation across the region. They believed that the 

simplest explanation for all observed trace-element and 

isotopic patterns is a two-end-member source for the 

batholithic rocks. Allegre and Othman (1980) showed, 

on the basis of neodymium-strontium isotopic relations, 

that one end member must have consisted of a large 

fraction of recycled older continental crust.

The model we have presented here seems compatible 

with these conclusions. M-l is basaltic and could have 

been derived from upper mantle sources. More or less 

pure M-l, modified or unmodified by the redistribution 

of crystals, could have supplied the gabbroic magmas 

of the western Peninsular Ranges. M-2, a quartzofeldspathic type, represents the nonprimitive end member and may be composed, in some large part, of a 

partial melt from the continental crust. With but few 

exceptions, the magmas required for each of the 497 

samples of the batholithic rocks range in composition 

between M-l and M-2. The model calls for areal patterns with a discontinuity in the eastern part of the 

Peninsular Ranges, probably representing both the 

time and place where significant amounts of continental 

materials became involved.

Although we interpret M-l and M-2 as representing 

magmas and D-l and D-2 as representing differentiates, we recognize that M-l and M-2 could also be 

interpreted as the extremes in a range of crustal rocks 

from which partial melts were derived. End-members 

D-l and D-2 then could be interpreted as the extremes 

in a range of mineral assemblages separated from the 

crustal rocks, not by magmatic differentiation, but by 

residual concentration as refractory materials left behind on crustal melting. Also possible is that both differentiation and residual concentration occurred to 

varying degrees over the region, but the two processes 

are not distinguishable from our model or from the raw 

chemical data. However, the compositional discontinuity in the eastern part of the Peninsular Ranges 

is a necessary part of the model regardless of how the 

end members are interpreted.

SUMMARY AND CONCLUSIONS

The batholithic rocks of southern California were 

examined by a method of Q-mode factor analysis and 

were found to have a compositional structure similar 

to that of the Sierra Nevada batholith. The compositional structure indicates that a petrogenetic model 

with only four end members will account for 85-97 percent of the variation in each of the eight major oxide 

constituents. We assumed that two of the end members 

represent an assemblage of plagioclase and mafic minerals, largely hornblende, that ranges in composition between D-l and D-2 of table 7. We further assumed 

that the other two end members represent a range of 

magmas from which plagioclase and the mafic minerals 

separated; the range was determined by computations 

based on the most likely source-magma compositions 

for the rocks of the southwesternmost Santa Ana block 

and the northeasternmost San Bernardino block. The 

limits of the range are given as end members M-l and 

M-2 in table 7.

Each of 480 sample compositions can be closely approximated as a mixture of the four derived end-member compositions. The 17 sample compositions that cannot be approximated in this manner are regarded as 

anomalous. The mixing proportions indicate that the 

batholithic rocks as a group required differentiation of 

about 47 percent; that is, about 47 percent of the 

magma was removed in the form of plagioclase, 

hornblende, and other mafic minerals.

The model proposed here is comprised of the endmember compositions given in table 7 and of the mixing 

proportions in Appendix 2. The mathematical validity 

of the model can be verified by mathematically combining the magma compositions (M-l and M-2 in table 7) 

and separating the differentiate compositions (D-l and 

D-2 in table 7) according to the mixing proportions in 

Appendix 2. The results will give close approximations 

of the original data in Appendix 1. The goodness-of-fit 

of the model to the original data is given by the parameters in table 2. The loss in goodness-of-fit that would 

be obtained by using fewer than four end members, 

or the improvement by adding more end members, can 

be observed from the factor-variance diagram in 

figure 4.

The principal advantage of the model is that it allows 

examination of its separate components, specifically the 

magmas and the mineral assemblages (differentiates) 

that were separated from them. Comparison of the compositional variation in the batholithic rocks with the 

compositional variation in the magmas, has been of particular interest. The variation in the magmas, or the
REFERENCES CITED 23

magma source materials, shows a discontinuity that is 

not evident in the original compositional data. The discontinuity is mainly near the San Jacinto fault zone 

close to the center of the Perris block. The general correspondence of the discontinuity to similar apparent discontinuities in mineralogic, petrologic, isotopic, and 

structural properties of the batholithic rocks suggest 

that the discontinuity is real and that the derived model 

is valid in at least a general way. The discontinuity 

is interpreted as the western limit of significant contribution of quartzo-feldspathic materials in the continental crust to the magmas that formed the batholithic 

rocks.

The compositional variations in the magmas, or their 

source materials, show no discontinuity at or near the 

San Andreas fault zone; this suggests that no large 

amount of displacement has occurred along this particular strand of the fault since the emplacement of the 

batholithic rocks.

REFERENCES CITED

Abbott, P. L., and Todd, V. R., eds., 1979, Mesozoic crystalline 

rocks: San Diego State University, Department of Geological Sciences, 286 p.

Allegre, C. J., and Othman, D. B., 1980, Nd-Sr isotopic relationship 

in granitoid rocks and continental crust development; a chemical 

approach to orogenesis: Nature, v. 286, p. 335-346.

Atwater, T., 1970, Implications of plate tectonics for the Cenozoic 

tectonic evolution of western North America: Geological Society 

of America Bulletin, v. 81, p. 3515-3536.

Baird, A. K., 1975, Plutonic zones in the Peninsular Ranges of southern California and Northern Baja California Comment: Geology, 

v. 3, p. 676-677.

Baird, A. K., Baird, K. W., and Welday, E. E., 1974, Chemical 

trends across Cretaceous batholithic rocks of southern California: 

Geology, v. 2, p. 493-496.

 1979, Batholithic rocks of the northern Peninsular and Transverse Ranges, southern California, in Abbott, P. L., and Todd, 

V. R., eds., Mesozoic crystalline rocks: San Diego State University, Department of Geological Sciences, p. 111-132.

Baird, A. K., Mclntyre, D. B., and Welday, E. E., 1967, Geochemical 

and structural studies in batholithic rocks of southern California; 

Part II, sampling of the Rattlesnake Mountain pluton for chemical composition and variation: Geological Society of America Bulletin, v. 78, p. 191-122.

Baird, A. K., Morton, D. M., Woodford, A. 0., and Baird, K. W., 

1974, The Transverse Ranges Province; a unique structural-petrochemical belt across the San Andreas fault system: Geological 

Society of America Bulletin, v. 85, p. 163-174.

Bateman, P. C., Clark, L. D., Huber, N. K., Moore, J. G., and 

Rinehart, C. D., 1963, The Sierra Nevada batholith A synthesis 

of recent work across the central part: U.S. Geological Survey 

Professional Paper 414-D, p. D1-D46.

Bateman, P. C., and Dodge, F. C. W., 1970, Variation of major chemical constituents across the central Sierra Nevada batholith: 

Geological Society of America Bulletin, v. 81, p. 409-420.

Crowell, J. C., 1979, The San Andreas fault system through time: 

Quarterly of the Journal Geological Society of London, v. 136, 

p. 293-302.

DePaolo, D. J., 1980, Sources of continental crust; neodymium isotope 

evidence from the Sierra Nevada and Peninsular Ranges: Science, v. 209, no. 4457, p. 684-687.

Gastil, G., Morgan, G. J., and Krummenacher, D., 1978, Mesozoic 

history of Peninsular California and related areas east of the Gulf 

of California, in Howell, D. G., and McDougall, K. A., eds., 

Mesozoic paleogeography of the western United States, Pacific 

Coast paleogeography symposium 2: Pacific Section, Society of 

Economic Paleontologists and Mineralogists, p. 107-115.

Gastil, R. G., Phillips, R. P., and Allison, E. C., 1975, Reconnaissance geology of the State of Baja California: Geological Society 

of America Memoir 140, 170 p.

Gromet, P. L., and Silver, L. T., 1979, Profile of rare earth element 

characteristics across the Peninsular Ranges batholith near the 

international border, southern California, U.S.A., and Baja 

California, Mexico, in Abbott, P. L., and Todd, V. R., eds., 

Mesozoic crystalline rocks: San Diego State University, Department of Geological Sciences, p. 133-142.

Hadley, D., and Kanamori, H., 1977, Seismic structure of the Transverse Ranges, California: Geological Society of America Bulletin, 

v. 88, p. 1469-1478.

Hill, M. L., and Dibblee, T. W., 1953, San Andreas, Garlock, and 

Big Pine faults, California A study of the character, history, 

and tectonic significance of their displacements: Geological Society of America Bulletin, v. 64, p. 443-458.

Imbrie, J., and Purdy, E. G., 1962, Classification of modern Bahamian carbonate sediments, in Ham, W. E., ed., Classification 

of carbonate rocks: American Association of Petroleum Geologists 

Memoir 1, p. 253-272.

Krummenacher, D., Gastil, R. G., Bushee, J., and Doupont, J., 1975, 

K-Ar apparent ages, Peninsular Ranges batholith, southern 

California and Baja California: Geological Society of America Bulletin, v. 86, p. 760-768.

Larsen, E. S., Jr., 1948, Batholith and associated rocks of Corona, 

Elsinore, and San Luis Rey quadrangles, southern California: 

Geological Society of America Memoir 29, 182 p.

Larsen, E. S., Jr., and Draisin, W. M., 1950, Composition of the 

minerals in the rocks of the southern California batholith: International Geological Congress, Report of 18th Session, Great Britain, 1948, pt. II, p. 66-79.

Luyendyk, B. P., Kamerling, M. J., and Terres, R., 1979, Geometric 

model for Neogene crustal rotations in southern California [abs.]: 

Geological Society of America Abstracts with Programs, v. 11, 

p. 470.

Miesch, A. T., 1976a, Q-mode factor analysis of compositional data: 

Computers & Geosciences, v. 1, p. 147-159.

 1976b, Q-mode factor analysis of geochemical and petrologic 

data matrices with constant row-sums: U.S. Geological Survey 

Professional Paper 574-G, 47 p.

 1976c, Interactive computer programs for petrologic modeling 

with extended Q-mode factor analysis: Computers & Geosciences, 

v. 2, p. 439-492.

 1979, Vector analysis of chemical variation in the lavas of 

Paricutin volcano, Mexico: Mathematical Geology, v. 11, p. 345- 

371. 

-1980, Scaling variables and interpretation of eigenvalues in

principal component analysis of geologic data: Mathematical Geology, v. 12, p. 523-538.

Miesch, A. T., and Morton, D. M., 1977, Chemical variability in the 

Lakeview Mountains pluton, southern California batholith A 

comparison of the methods of correspondence analysis and extended Q-mode factor analysis; U.S. Geological Survey Journal 

of Research, v. 5, p. 103-116.

Miesch, A. T., and Reed, B. L., 1979, Compositional structures in 

two batholiths of circum-Pacific North America: U.S. Geological 

Survey Professional Paper 574-H, 31 p.

Miller, C. F., 1977, Early alkalic plutonism in the calc-alkaline 

batholithic belt of California: Geology, v. 5, p. 685-688.

Moore, J. G., 1959, The quartz diorite boundary line in the western 

United States: Journal of Geology, v. 67, p. 198-210.
24 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

Morton, D. M., and Baird, A. K., 1976, The Paloma Valley ring dike 

complex: U.S. Geological Survey Journal of Research, v. 4, p. 

83-89.

Morton, D. M., Baird, A. K., and Baird, K. W., 1969, The Lakeview 

Mountains pluton, southern California batholith, Part II; Chemical composition and variation: Geological Society of America Bulletin, v. 80, p. 1553-1564.

Nishimori, R. K., 1976, The petrology and geochemistry of the gabbros from the Peninsular Ranges batholith, California, and a 

model for their origin: Scripps Institute of Oceanography, Ph.D. 

thesis, 234 p.

Nockolds, S. R., and Alien, R., 1953, Geochemistry of some igneous 

rock series, I: Geochimica et Cosmochimica Acta, v. 4, p. 105- 

142.

Reed, B. L., and Lanphere, M. A., 1973, Alaska-Aleutian Range 

batholith; geochronology, chemistry, and relation to circumPacific plutonism: Geological Society of America Bulletin, v. 84, 

p. 2583-2610.

Richmond, J. F., 1965, Chemical variation in quartz monzonite from 

Cactus Flat, San Bernardino Mountains, California: American 

Journal of Science, v. 263, p. 53-63.

Schwarcz, H. P., 1969, Pre-Cretaceous sedimentation and 

metamorphism in the Winchester area, northern Peninsular 

Ranges, California: Geological Society of America Special Report 

100, 63 p.

Silver, L. T., 1971, Problems of crystalline rocks of the Transverse 

Ranges [abs.]: Geological Society of America Abstracts with Programs, v. 3, p. 193-194.

Silver, L. T., Early, T. 0., and Anderson, T. H., 1975, Petrological, 

geochemical and geochronological asymmetries of the Peninsular 

Ranges batholith [abs.]: Geological Society of America Abstracts 

with Programs, v. 7, p. 375-376.

Silver, L. T., Taylor, H. P., Jr., and Chappell, B., 1979, Some petrological, geochemical and geochronological observations of the 

Peninsular Ranges batholith near the international border of the 

U.S.A. and Mexico, in Abbott, P. L., and Todd, V. R., eds.,

Mesozoic crystalline rocks: San Diego State University, Department of Geological Sciences, p. 83-110.

Streckeisen, A. L., 1973, Plutonic rocks, classification and nomenclature recommended by the I.U.G.S. Subcommision on the systematics of igneous rocks: Geotimes, v. 18, p. 26-30.

Stuckless, J. S., and Miesch, A. T., 1981, Petrogenetic modeling of 

a potential uranium source rock, Granite Mountains, Wyoming: 

U.S. Geological Survey Professional Paper 1225, 34 p.

Stuckless, J. S., Miesch, A. T., Goldich, S. S., and Weiblen, P. W., 

1981, A Q-mode factor model for the petrogenesis of the volcanic 

rocks from Ross Island and vicinity, Antarctica: American 

Geophysical Union, Dry Valley Drilling Project, Antarctica Research Series, v. 33, p. 257-280.

Taylor, H. P., Jr., and Silver, L. T., 1978, Oxygen isotope relationships in plutonic igneous rocks of the Peninsular Ranges 

batholith, southern and Baja California: U.S. Geological Survey 

Open-File Report 78-701, p. 423-426.

Todd, V. R., and Shaw, S. E., 1979, Structural, metamorphic and 

intrusive framework of the Peninsular Ranges batholith in southern San Diego County, California, in Abbott, P. L., and Todd, 

V. R., eds., Mesozoic crystalline rocks: San Diego State University, Department of Geological Sciences, p. 177-231.

Van Trump, G., Jr., and Miesch, A. T., 1977, The U.S. Geological 

Survey RASS-STATPAC system for management and statistical 

reduction of geochemical data: Computers & Geosciences, v. 3, 

p. 475^88.

Walawender, M. J., 1979, Basic plutons of the Peninsular Ranges 

batholith, southern California, in Abbott, P. L., and Todd, V. 

R., eds., Mesozoic crystalline rocks: San Diego State University, 

Department of Geological Sciences, p. 151-162.

Woodford, A. O., 1960, Bedrock patterns and strike-slip faulting in 

southwestern California: American Journal of Science, v. 258A, 

p. 400-417.

Yeats, R. S., 1981, Quaternary flake tectonics of the California Transverse Ranges: Geology, v. 9, p. 16-20.
Maps of the variability of Si02, A1203, FeO, MgO, CaO, Na20, K20, and Ti02 in the batholithic rocks of southern California and in the 

magmas and differentiates as interpreted from the model. Class intervals are defined by the 20th, 40th, 60th, and 80th percentiles of

the mapped variables.
26 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

119° 118° 117° 116°

34°

33°

SiO2 ( PERCENT) V^ 

> 72.70

69.60 to 72.70 

67.00 to 69.60 

64.10 to 67.00

< 64.10 

- FAULT ZONE ,

Si02

SiO2 IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

SiO2 ( PERCENT) 

> 61.70

60.40 to 61.70 

59.00 to 60.40 

58.10 to 59.00

< 58.00 

- FAULT ZONE | SiO2 IN THE MAGMAS

119° 118° 117° 116°

34°

33°

SiO2 ( PERCENT) 

>51.30

50.50 to 51.30 

49.70 to 50.50 

49.10 to 49.70

< 49.10 

- FAULT ZONE , SiO2 IN THE DIFFERENTIATES

o 25

i i I

50 KILOMETERS

50 MILES
119° 118° 117°

FIGURE 12

116°

34°

33°

, Los Angel

A12O3 (PERCENT)V_

> 16.87

16.25 to 16.87 

15.54 to 16.25 

14.61 to 15.54

< 14.61

FAULT ZONE

27

A1203

A12O3 IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

A12O3 (PERCENT)

 > 18.55 

B 18.51 to 18.55 

a 18.48 to 18.51 

18.46 to 18.48 

< 18.46

 FAULT ZONE AI2O3 IN THE MAGMAS

119° 118° 117° 116°

34°

33°

A12O3 

> 22.25

21.80 to 22.25 

21.02 to 21.35 

21.35 to 21.80 

< 21.02 

- FAULT ZONE , A12O3 IN THE DIFFERENTIATES

o 50 KILOMETERS 

I_____

50 MILES
FcO (PERCENT) 

>4.88

3.96 to 4.88 

2.97 to 3.96 

1.90 to 2.97

< 1.90 

FAULT ZONE

BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA 

117° 116° FeO

33° ^

FcO IN BATHOUTHIC ROCKS

119° 118° 117°

FcO (PERCENT)

> 6.82

6.28 to 6.82 

5.50 to 6.28 

4.78 to 5.50

<4.78

FAULT ZONE

33° TL

FcO IN THE MAGMAS

119° 118° 117°

FcO (PERCENT)

>9.41

8.93 to 9.41 

8.27 to 8.93 

7.65 to 8.27

< 7.65

FAULT ZONE

33° n.

FcO IN THE DIFFERENTIATES

i

50 MILES
119° 118° 117°

FIGURE 12 

116°

34°

33°

x_^

MgO (PERCENT) 

B > 2.34 

a 1.65 to 2.34 

a 1.03 to 1.65 

0.50 to 1.03 

< 0.50 5 

 FAULT ZONE

=BD B m,Q DUD 

BBBBBBB^aBBBBB

-- B BNB B 

BB-BBBI

BB==BBB

29

MgO

MgO IN BATHOLITHIC ROCKS

MgO (PERCENT)

>3.48

3.14 to 3.48 

2.65 to 3.14 

2.20 to 2.65

<2.20

FAULT ZONE

33° -

MgO IN THE MAGMAS

119° 118° 117° 116°

34°

33°

MgO

> 5.13

4.75 to 5.13 

4.22 to 4.75 

3.72 to 4.22

< 3.72

FAULT ZONE MgO IN THE DIFFERENTIATES

50 KILOMETERS

50 MILES
30

119° 1T8°

BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA 

117° 116°

a\n

34°

33°

CaO (PERCENT) 

> 5.17

4.14 to 5.17 

2.94 to 4.14 

2.13 to 2.93

<2.13 

 FAULT ZONE

GaO

CaO IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

CaO (PERCENT) 

> 7.24

6.80 to 7.24 

6.17 to 6.80 

5.59 to 6.17 

<5.59 

 FAULT ZONE \ l CaO IN THE MAGMAS

119° 118° 117° 116°

34°

33°

CaO (PERCENT) 

> 10.19

9.84 to 10.19 

9.36 to 9.84 

8.90 to 9.36 

< 8.90 

- FAULT ZONE , CaO IN THE DIFFERENTIATES

o 25 50 KILOMETERS

i I I_____,

^^ \ I

50 MILES
FIGURE 12 31

119° 118° 117° 116°

34°

33°

Na2O IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

Na2O (PERCENT)

 > 4.04 

o 3.88 to 4.04 

a 3.72 to 3.88 

3.61 to 3.72 

<3.61

 FAULT ZONE Na2O IN THE MAGMAS

119° 118° 117° 116°

34°

33°

Na2O (PERCENT) 

i > 4.51 

i 4.05 to 4.51 

i 3.60 to 4.05 

3.27 to 3.60 

< 3.27 

 FAULT ZONE Na2O IN THE DIFFERENTIATES

50 KILOMETERS

50 MILES
32 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

119° 118° 117° 116°

34°

33°

K2O (PERCENT)

> 3.92

3.17 to 3.92 

2.51 to 3.17 

1.88 to 2.51

< 1.88 

 FAULT ZONE K2O IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

K2O (PERCENT) 

> 2.17

1.84 to 2.17 

1.48 to 1.84 

1.24 to 1.48

< 1.24 

- FAULT ZONE K2O IN THE MAGMAS

119° 118° 117° 116°

34°

33°

K20

 > 0.31 

a 0.30 to 0.31 

o 0.28 to 0.30 

0.26 to 0.28 

< 0.26

 FAULT ZONE K2O IN THE DIFFERENTIATES

0 25 50 KILOMETERS

50 MILES
119°

33

TiG>2

33° -^

TiO2 IN BATHOLITHIC ROCKS

119° 118° 117° 116°

34°

33°

TiO2 (PERCENT) 

> 1.09

1.05 to 1.09 

0.99 to 1.05 

0.93 to 0.99 

<0.93 

 FAULT ZONE TiO2 IN THE MAGMAS

119° 118° 117°

TiO2 (PERCENT)

> 1.57

1.53 to 1.57 

1.48 to 1.53 

1.43 to 1.48

< 1.43

FAULT ZONE

DBD «DD mm a o=n am IS=B-HHO===H

BBBDtfH, B = = = BD-D OBB ox, a D=B

HBBBBBBXBBB=>aa 

BBBBBO 

BBBOBB

33° -^

TiO2 IN THE DIFFERENTIATES

50 MILES

APPENDIXES 1 AND 2

Chemical data on batholithic rocks of southern California (Appendix 1) and mixing proportions for end-members M-1, M-2, D-1, and D-2

(Appendix 2)
36 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

APPENDIX 1

Chemical data on batholithic rocks of southern California, 

in percent

Oxide

Sample

Number Si02 A1 203 FeO MgO CaO Na2 0 K2 0 Ti02

San Gabriel block

B 1

B 2

B 3

B 4

B 5

B 6

B 7

B 8

B 9

B 10

B 11

B 12

B 13

B 14

B 15

B 16

B 17

B 18

B 19

B 20

B 21

B 22

B 23

B 24

B 25

B 26

B 27

B 28

B 29

B 30

B 31

B 32

B 33

B 34

B 35

B 36

B 37

B 38

B 39

B 40

B 41

B 42

B 43

B 44

B 46

B 47

B 48

71.21

69.06

63.09

65.87

67.56

75.05

69.56

67.77

72.99

71.97

70.81

66.75

67.53

59.91

63.66

62.14

68.15

73.72

75.01

75.46

66.36

62.10

64.83

62.14

74.14

73.29

63.59

68.64

66.93

67.26

69.51

65.29

60.46

68.13

73.05

67.43

62.59

58.08

58.46

63.68

56.51

60.61

67.08

63.60

71.05

70.16

71.25

15.41

16.59

16.98

15.57

15.68

14.39

15.78

16.49

15.30

15.33

16.05

16.44

16.17

17.51

16.48

17.27

15.33

14.76

14.25

14.57

16.46

18.33

17.30

16.93

14.51

15.56

18.44

16.90

16.47

16.05

16.12

16.85

18.66

15.92

14.80

16.02

17.03

18.48

18.09

16.58

19.22

17.37

16.51

17.92

16.28

16.16

16.15

2.50

2.71

5.45

4.23

3.91

1.19

3.07

3.71

1.64

1.71

2.94

4.14

3.95

6.65

5.43

5.43

4.13

1.61

1.15

0.91

4.11

5.78

4.47

5.64

1.46

1.55

4.66

2.59

3.63

4.25

2.37

4.51

6.29

3.63

1.68

3.77

5.70

6.82

7.05

5.29

7.05

5.96

3.88

4.74

1.94

2.17

1.81

0.87

0.95

2.48

2.81

1.60

0.25

1.21

1.57

0.50

0.50

0.97

1.52

1.31

3.32

2.61

2.63

1.49

0.60

0.22

0.23

1.54

2.81

1.67

2.88

0.47

0.40

1.52

0.95

1.55

1.50

0.67

1.57

2.49

1.53

0.57

1.58

2.43

3.48

3.31

2.49

3.33

3.08

1.38

1.51

0.57

0.53

1.03

2.28

2.71

4.66

3.87

3.65

0.83

2.63

3.21

1.67

1.73

2.12

3.57

3.52

5.45

4.82

5.49

3.25

1.93

0.80

0.76

4.10

5.21

4.64

5.43

1.32

1.55

4.01

2.47

3.79

3.14

2.07

4.26

5.44

3.20

1.83

3.42

4.36

6.73

5.86

4.49

6.79

5.16

3.95

4.03

2.22

2.17

2.70

4.14

4.38

3.92

3.88

3.62

4.01

4.03

4.22

4.17

3.94

3.36

3.91

3.70

3.96

3.81

3.93

3.68

3.61

3.52

3.16

4.09

3.55

4.13

3.85

3.79

3.53

4.53

3.85

3.75

4.10

4.21

4.09

3.83

3.64

3.76

3.72

3.89

3.61

4.16

3.96

4.12

4.16

3.79

4.10

4.00

4.08

3.96

3.16

3.12

2.65

3.19

3.42

4.11

3.32

2.55

3.44

4.46

3.27

2.99

3.16

2.27

2.42

2.32

3.38

3.55

4.83

4.76

2.56

1.46

2.07

2.21

4.16

3.88

2.64

4.18

3.18

2.99

4.63

2.90

2.16

3.42

4.10

3.57

3.17

1.98

2.23

2.85

1.92

2.86

2.64

3.37

3.57

4.35

2.73

0.44

0.49

0.77

0.58

0.56

0.17

0.40

0.49

0.30

0.37

0.49

0.68

0.64

0.92

0.78

0.79

0.59

0.22

0.22

0.15

0.79

0.75

0.89

0.92

0.17

0.24

0.62

0.42

0.70

0.70

0.42

0.54

0.67

0.54

0.22

0.49

0.83

0.82

0.85

0.66

1.06

0.79

0.77

0.74

0.37

0.37

0.37

San Bernardino block

B 54

B 55

B 56

B 57

B 58

B 59

B 60

B 61

B 62

72.80

70.24

64.65

63.99

64.85

64.96

67.37

62.06

64.31

15.45

15.38

17.02

17.55

16.92

17.07

16.26

17.13

17.15

0.74

2.45

4.01

4.05

4.11

3.89

3.29

5.48

4.19

0.27

0.88

1.56

2.17

1.62

1.57

1.11

2.50

1.61

2.43

3.32

4.39

4.35

4.23

4.32

3.64

5.31

4.48

3.97

3.60

4.27

4.01

4.10

4.15

3.91

3.91

4.21

3.96

3.53

3.16

2.98

3.27

3.15

3.72

2.64

3.08

0.37

0.60

0.93

0.89

0.90

0.88

0.71

0.96

0.97

Oxide

Sample 

Number

B 63

B 64

B 65

B 66

B 67

B 68

B 69

B 70

B 71

B 72

B 74

B 75

B 78

B 79

B 80

B 81

B 85

B 86

B 94

B 95

B 96

B 97

B 98

B 99

B100

B101

B102

B103

B104

BIOS

B106

B107

BIOS

B109

B110

Bill

B112

B113

B114

BUS

B116

B117

B118

B120

B121

B124

B125

B127

B128

B129

B130

B131

B132

B133

B134

B135

B136

B137

B138

B139

B140

B141

B142

B143

B144

ao2

70.13

73.67

73.66

66.84

66.97

73.30

69.82

64.11

68.14

74.06

63.26

73.89

70.40

70.35

66.63

70.77

68.75

76.76

71.45

72.71

73.80

62.97

67.21

65.37

73.31

68.82

67.58

70.07

68.46

75.51

71.97

71.15

63.94

75.28

75.96

76.19

75.73

75.85

77.40

73.67

63.70

70.91

73.59

71.82

68.79

72.66

73.18

72.57

63.78

73.39

72.84

73.61

73.20

74.33

73.95

72.37

71.72

71.62

72.45

72.86

72.44

70.93

71.81

71.96

72.13

"2°,

15.49

14.58

14.34

16.15

17.34

14.65

15.54

16.67

15.86

14.40

16.49

14.53

15.96

15.31

16.46

15.22

15.53

12.83

15.20

14.72

14.62

16.93

15.86

15.99

15.55

15.55

16.13

15.51

16.26

13.35

14.80

15.22

16.15

13.32

12.85

13.02

12.36

12.70

12.11

15.37

16.70

16.05

14.63

14.39

15.48

14.36

14.67

15.13

16.91

14.42

15.25

14.59

14.95

14.48

14.64

15.73

15.20

15.23

14.96

14.88

14.99

15.40

15.15

15.07

14.72

FeO

2.14

0.81

1.41

3.48

2.93

1.19

2.41

4.46

3.25

0.89

5.08

0.78

2.51

2.27

3.51

2.40

2.90

0.16

1.49

1.02

0.89

4.60

2.92

3.44

0.13

2.58

2.77

2.14

2.50

0.76

1.64

1.73

5.20

1.95

1.05

0.14

1.39

1.13

0.69

0.40

4.76

1.54

1.10

2.16

3.02

1.67

1.12

1.38

4.50

1.22

1.30

1.04

1.25

0.79

0.90

0.68

1.51

1.76

1.42

1.29

1.42

1.77

1.54

1.41

1.69

MgO

0.80

0.17

0.25

1.46

1.63

0.27

0.85

1.99

1.10

0.20

2.64

0.30

0.83

0.78

2.08

0.98

0.96

0.02

0.40

0.30

0.35

2.32

1.17

1.58

0.10

1.11

1.22

0.84

1.03

0.20

0.60

0.71

2.48

0.32

0.20

0.08

0.35

0.22

0.08

0.20

2.18

0.56

0.31

0.56

1.25

0.55

0.37

0.37

2.07

0.33

0.49

0.25

0.30

0.08

0.18

0.20

0.55

0.59

0.40

0.38

0.38

0.57

0.51

0.45

0.51

CaO

3.02

1.92

1.94

3.80

3.44

2.13

3.28

4.61

3.58

1.82

4.87

2.24

1.60

2.43

3.86

2.15

2.94

1.28

2.23

2.03

2.23

4.82

2.82

4.12

2.45

3.21

3.45

2.75

3.06

1.50

2.43

2.57

4.62

1.04

1.47

1.34

1.70

1.44

1.28

1.81

4.75

2.84

2.23

2.01

2.61

2.39

2.08

1.97

4.89

1.88

1.78

2.13

2.24

1.63

1.85

2.21

2.52

2.44

2.27

2.18

2.24

2.58

2.34

2.44

2.35

H, 2 0

3.71

3.71

3.64

3.71

3.84

3.46

3.94

3.88

3.94

3.42

3.94

3.79

3.98

4.41

3.87

4.04

3.71

3.65

3.67

3.64

3.81

3.97

4.54

3.64

4.03

3.95

4.05

3.74

4.19

3.93

3.81

3.83

4.01

2.74

2.98

2.78

3.27

3.02

2.87

4.01

3.85

4.17

3.47

3.45

3.82

3.60

3.80

3.62

3.81

3.36

3.48

3.58

3.62

3.60

3.79

4.04

3.81

3.71

3.70

3.68

3.58

3.88

3.62

3.72

3.62

V

4.17

4.81

4.38

3.83

3.20

4.63

3.54

3.35

3.45

4.85

2.76

4.11

4.16

3.86

2.74

3.78

4.52

5.04

5.04

5.10

3.94

3.55

4.74

5.05

4.16

4.15

4.12

4.37

3.95

4.38

4.25

4.26

2.91

5.02

5.14

6.13

4.81

5.26

5.22

4.23

3.31

3.50

4.28

5.10

4.24

4.32

4.31

4.49

3.28

5.01

4.43

4.44

4.03

4.76

4.35

4.44

4.18

4.14

4.34

4.28

4.50

4.35

4.54

4.50

4.49

««,,

0.55

0.34

0.37

0.74

0.66

0.37

0.62

0.93

0.68

0.37

0.96

0.37

0.55

0.58

0.85

0.66

0.68

0.27

0.52

0.47

0.37

0.83

0.73

0.82

0.27

0.63

0.68

0.57

0.55

0.37

0.50

0.53

0.68

0.34

0.35

0.32

0.39

0.39

0.33

0.32

0.75

0.43

0.38

0.51

0.77

0.45

0.47

0.47

0.77

0.40

0.44

0.37

0.40

0.33

0.34

0.33

0.52

0.52

0.46

0.45

0.45

0.52

0.48

0.45

0.48
APPENDIX 1 37

APPENDIX i . Continued

Oxide

Sample

Number Si0 2 A1 2 0 3 FeO

San Bernard ino

BUS

B146

B147

B148

B149

B150

B151

B152

B153

B155

B156

B157

B158

B159

B160

B161

B162

B163

B164

B165

B166

B168

B169

B170

B171

B172

B173

B174

B175

B176

B177

B178

B179

B180

B181

B182

B183

B184

B185

B186

B187

B188

B189

B190

B191

B192

B193

B194

B195

B196

B197

B198

B199

B200

B201

B202

B203

B204

B205

B206

B207

72.12

73.32

71.64

71.87

72.84

72.08

70.67

65.95

67.49

61.93

63.74

71.88

60.80

64.43

65.27

68.35

69.21

74.59

59.57

74.49

59.03

59.70

59.12

70.61

69.21

61.21

73.61

72.10

71.54

71.18

72.87

74.89

63.87

72.32

74.03

72.67

71.52

75.38

68.99

71.38

71.46

71.10

74.77

73.35

73.04

72.48

73.60

69.38

74.59

68.12

73.91

72.14

72.49

69.47

70.43

72.69

72.40

73.58

71.21

74.73

73.43

14.98

14.66

15.20

15.27

14.88

15.18

15.56

16.37

16.54

16.89

16.88

15.31

17.84

16.55

16.48

16.39

15.78

15.17

17.93

14.43

17.69

17.36

17.29

16.45

16.26

16.90

14.79

14.97

15.18

16.15

14.97

14.44

17.64

15.27

14.86

14.49

14.95

13.80

15.80

15.73

15.60

15.23

14.73

15.24

15.18

15.53

15.16

16.08

14.61

16.35

14.92

Little

15.80

15.06

16.50

15.90

16.29

16.64

14.47

14.97

13.64

15.04

1.41

1.22

1.46

1.40

1.07

1.36

1.84

3.90

3.16

5.10

4.36

1.33

5.88

4.58

4.22

3.86

3.03

0.86

6.45

0.86

6.37

6.36

6.65

1.53

2.41

6.02

0.44

1.56

1.60

1.40

0.79

0.21

4.77

0.92

0.62

1.45

2.27

0.91

2.46

1.73

1.31

1.93

0.21

0.49

0.59

1.01

0.64

2.29

0.26

2.63

0.41

MgO CaO Na2 0 K2 0 Ti0 2

block Continued

0.50

0.33

0.50

0.50

0.35

0.42

0.62

1.67

0.98

2.42

1.59

0.33

2.40

2.25

1.96

1.66

0.81

0.22

3.15

0.20

3.34

3.14

3.26

0.49

0.95

2.80

0.20

0.57

0.62

0.53

0.22

0.08

1.78

0.52

0.22

0.53

0.93

0.18

0.99

0.85

0.56

0.72

0.07

0.20

0.12

0.41

0.20

0.95

0.15

1.07

0.21

2.36

2.07

2.49

2.50

2.22

2.37

2.78

4.31

3.30

5.18

4.63

2.15

5.28

4.76

4.61

1.84

2.96

1.83

5.19

2.18

6.37

6.11

6.46

3.19

3.29

5.72

1.90

2.51

2.64

3.17

1.95

1.59

4.74

2.33

2.00

2.37

2.47

1.06

3.10

2.22

2.59

2.57

1.58

2.26

2.19

2.28

1.96

3.08

1.98

3.23

2.04

3.69

3.71

3.77

3.81

3.78

3.78

3.84

3.79

4.09

3.74

3.96

3.98

4.04

3.54

3.79

3.74

3.89

3.81

3.95

3.66

3.95

3.76

3.80

4.33

4.02

4.12

3.57

3.44

3.58

4.03

3.83

3.42

4.26

4.11

3.73

3.31

3.35

2.54

3.81

3.84

3.78

3.52

3.74

3.81

3.69

3.76

3.83

3.99

3.64

3.96

3.55

4.45

4.27

4.43

4.16

4.42

4.34

4.17

3.33

3.91

3.90

4.53

4.61

2.82

3.16

2.97

3.48

3.79

2.79

2.82

3.86

2.26

2.60

2.38

2.94

3.30

2.30

5.14

4.39

4.40

3.09

5.02

5.08

2.17

4.11

4.24

4.73

3.88

5.73

4.20

3.73

4.25

4.45

4.63

4.26

4.87

4.18

4.26

3.70

4.46

4.03

4.62

0.50

0.42

0.50

0.49

0.44

0.47

0.54

0.70

0.53

0.84

0.31

0.42

0.93

0.74

0.70

0.68

0.52

0.73

0.94

0.32

1.00

0.97

1.03

0.46

0.55

0.94

0.35

0.45

0.45

0.45

0.35

0.29

0.76

0.42

0.32

0.45

0.62

0.40

0.65

0.50

0.43

0.49

0.28

0.39

0.32

0.36

0.35

0.54

0.32

0.61

0.33

San Bernardino block

1.13

1.79

1.76

2.34

1.23

1.17

1.49

2.15

1.59

1.25

0.50

0.45

0.50

0.76

0.42

0.29

0.55

0.69

0.22

0.43

1.83

1.80

2.46

2.33

1.57

1.28

1.87

2.02

0.84

1.58

3.77

3.80

4.82

3.88

3.35

3.75

3.69

3.33

3.52

3.91

4.49

4.37

4.30

3.94

4.27

4.33

4.13

5.19

5.24

4.17

0.34

0.24

0.19

0.41

0.18

0.15

0.22

0.43

0.23

0.20

Oxide

Sample

Number

B208

B209

B210

B211

B212

B213

B214

B215

B216

B217

B218

B219

B220

B221

B222

Si0 2

73.92

68.91

66.99

71.33

70.36

62.87

61.34

75.13

67.02

72.26

65.78

68.12

71.61

64.72

64.45

A1 2 0 3

13.84

14.62

16.49

16.04

16.07

17.35

16.75

14.17

16.90

14.74

16.52

16.09

15.45

16.34

15.64

FeO

2.02

2.80

3.71

1.96

2.33

5.70

5.98

0.99

1.47

2.19

3.61

3.19

1.90

4.80

5.40

MgO

0.48

3.02

1.49

0.61

0.78

2.25

3.10

0.25

2.33

0.30

2.16

1.81

0.64

2.67

2.20

San Jacinto

B223

B224

B225

B226

B227

B228

B229

B230

B231

B232

B233

B234

B235

B236

B237

B238

B239

B240

B241

B242

B243

B244

B245

B246

B247

B248

B249

B250

B251

B252

B253

B254

B255

B256

B257

B258

B259

B260

B261

B262

B263

B264

B265

B266

B267

B268

B269

B270

B271

B272

66.88

71.27

67.79

66.49

64.61

68.69

63.94

67.61

69.36

64.29

64.86

67.55

68.60

68.00

65.74

68.19

66.00

67.46

67.83

67.17

66.09

64.96

66.34

69.67

67.70

70.43

68.30

69.17

63.83

67.92

66.45

67.45

75.57

66.56

65.81

66.73

73.00

65.86

67.01

71.26

70.58

72.61

64.74

75.41

75.19

69.90

63.96

75.26

75.13

72.69

17.22

15.72

17.35

16.78

16.49

16.05

18.34

16.21

16.47

17.64

15.92

16.88

16.90

15.78

17.30

16.24

17.11

17.22

17.04

16.90

17.31

16.50

16.29

16.33

16.92

15.89

16.44

16.34

16.86

17.00

16.62

17.03

13.68

16.45

17.22

16.72

14.61

16.74

16.94

15.94

15.10

14.98

16.80

14.29

13.61

15.43

17.57

13.73

14.17

14.56

3.39

2.14

2.89

4.21

4.14

3.20

3.80

3.67

2.79

4.36

5.14

3.46

3.00

3.68

3.84

3.21

3.86

3.09

3.17

3.65

3.69

4.36

4.64

2.73

3.37

2.78

2.94

2.64

5.10

3.18

4.03

3.45

1.13

4.04

3.93

3.98

2.26

4.58

3.70

2.07

3.53

2.27

4.85

0.46

1.65

3.58

4.74

1.64

1.36

3.30

1.29

0.72

1.05

1.64

2.32

1.12

1.56

1.35

1.05

1.75

2.43

1.32

1.10

1.54

1.36

1.14

1.39

1.13

1.18

1.36

1.44

2.52

1.29

0.93

1.24

0.92

1.16

1.00

2.10

1.17

1.59

1.33

0.31

1.51

1.43

1.45

0.45

1.50

1.34

0.99

0.78

0.55

2.07

0.15

0.18

1.09

1.94

0.32

0.27

0.58

CaO

1.21

3.16

3.70

2.51

2.93

4.84

5.84

1.10

4.67

1.58

2.94

2.48

1.96

3.41

4.75

block

4.59

2.73

4.17

4.40

4.97

3.78

5.42

4.01

3.28

4.96

4.74

4.11

3.90

3.82

4.76

4.00

4.65

4.09

3.74

3.97

4.68

5.14

4.09

3.07

3.83

3.04

3.94

3.62

5.40

3.63

4.30

3.87

1.65

4.31

4.62

4.10

1.90

3.89

4.01

2.78

2.59

2.21

4.48

1.18

1.12

3.00

5.03

1.31

1.24

2.20

Na 2 0

4.06

3.47

3.89

4.15

4.14

3.62

3.90

3.82

3.88

3.76

4.89

4.01

3.88

3.93

3.61

4.20

3.39

4.13

3.22

3.36

3.68

4.11

3.62

3.79

4.06

3.40

3.91

4.01

3.37

4.03

3.84

3.98

4.02

4.03

3.89

3.94

3.59

3.81

3.87

4.11

3.82

3.73

3.54

3.74

4.06

3.82

3.97

2.88

3.60

3.87

3.91

3.38

4.23

3.83

3.46

3.73

3.45

3.83

2.75

2.62

3.52

4.06

3.84

3.77

3.95

K2 0

4.11

3.65

3.23

3.09

3.02

2.59

2.19

4.46

3.09

4.89

3.50

3.80

4.32

3.48

3.15

1.72

3.50

1.98

2.28

3.19

2.79

1.82

2.77

2.66

1.93

2.70

2.01

1.87

3.19

2.12

2.66

2.17

2.31

2.34

2.28

2.05

2.12

2.74

2.87

2.16

2.59

2.80

3.06

2.00

2.36

2.30

2.21

4.51

2.68

2.25

2.27

4.09

2.42

2.39

3.02

3.13

3.59

2.35

5.62

5.48

2.98

1.69

3.70

3.87

2.36

Ti02

0.35

0.38

0.50

0.31

0.37

0.77

0.89

0.08

0.64

0.27

0.61

0.51

0.25

0.64

0.80

0.71

0.53

0.64

0.99

0.92

0.69

1.00

0.76

0.59

1.01

0.81

0.76

0.62

0.64

0.84

0.72

0.84

0.68

0.66

0.78

0.81

0.81

0.80

0.53

0.68

0.54

0.69

0.62

0.96

0.68

0.89

0.71

0.27

0.85

0.86

0.84

0.32

0.78

0.78

0.49

0.57

0.34

0.90

0.15

0.16

0.50

1.01

0.22

0.20

0.37
BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

APPENDIX 1. Continued

Oxide

Sample 

Number Sio2 A1 2°3 FeO MgO CaO ». 2 o K2 0 Ti02

San Jacinto block Continued

B273

B274

B275

B276

B277

B278

B279

B280

B281

B282

B283

B284

B285

B286

B287

B288

B289

B290

B291

B292

B293

B294

B295

B296

B297

B298

B299

B300

B301

B302

B303

B304

B305

B306

B307

B308

B309

B310

B311

B312

B313

B314

B315

B317

B318

B319

B320

B321

B322

B323

B324

B325 

B326

B327

B328

B330

B331

B332

B333

B334

B336

65.62

66.32

70.18

66.77

64.05

65.89

70.28

68.94

70.36

73.79

66.23

68.84

66.83

63.47

69.17

65.22

68.85

64.38

69.21

69.67

68.89

69.56

62.78

68.72

65.50

64.97

65.85

61.79

65.68

64.92

67.89

62.41

62.25

65.08

65.56

63.18

68.70

63.96

64.18

77.23

75.87

73.09

64.60

65.13

63.96

65.26

63.77

63.53

65.58

63.62

66.09

66.27 

64.42

66.35

68.65

72.16

72.79

74.07

73.74

75.29

60.86

16.97

16.88

16.01

16.46

16.69

17.12

15.77

16.25

15.70

14.41

16.08

16.20

16.39

17.29

15.63

16.62

15.99

16.87

15.43

15.22

15.53

15.61

17.27

16.09

16.85

16.71

17.13

17.89

16.69

17.00

16.87

18.06

17.73

17.24

16.66

17.76

16.08

16.46

17.31

12.84

13.66

14.63

17.43

17.56

17.52

17.46

17.74

18.31

16.81

18.08

17.16

16.03 

15.81

15.55

15.28

12.94

14.29

14.00

14.19

13.58

16.99

4.63

3.67

2.20

3.97

5.01

4.29

3.24

3.76

2.94

1.75

4.53

2.76

3.41

4.54

2.96

4.29

2.65

4.53

3.00

3.09

3.22

2.98

4.90

3.04

3.86

4.19

3.49

4.89

3.90

4.22

2.87

4.68

4.97

3.91

3.82

4.53

3.04

5.33

4.83

0.90

1.29

2.51

4.80

4.25

4.57

4.16

4.58

4.59

4.33

4.56

4.53

Perris

4.57 

5.16

4.83

4.06

1.75

2.51

1.92

1.97

1.60

6.44

1.79

1.82

0.98

1.79

2.70

1.81

0.65

0.68

0.89

0.47

2.10

1.13

1.72

2.55

1.22

2.24

1.34

1.97

1.14

1.23

1.37

1.23

2.65

1.40

2.16

2.29

1.69

2.76

2.11

2.11

1.28

2.52

2.56

2.08

2.16

2.44

1.40

2.51

2.11

0.15

0.19

0.39

1.86

1.52

1.80

1.52

1.83

1.69

1.76

1.93

1.50

block

1.94 

2.88

1.85

1.35

3.50

0.75

0.60

0.61

0.45

3.38

4.51

4.24

3.16

3.83

4.29

3.95

2.45

2.60

3.16

1.75

3.25

3.25

4.25

5.24

3.71

4.99

3.59

5.05

3.54

3.72

3.52

3.42

5.47

3.41

4.40

4.74

4.46

5.71

4.56

4.43

3.93

5.52

5.22

4.50

4.64

5.14

3.42

4.38

4.60

0.67

1.34

1.72

4.77

5.02

5.34

4.97

5.43

5.28

4.69

5.07

4.41

4.48 

5.14

4.62

3.84

1.45

2.21

1.85

2.17

1.41

6.71

3.98

3.61

3.44

3.54

3.46

3.60

3.80

4.08

3.43

2.86

2.99

3.35

3.39

3.50

3.36

3.46

3.67

3.79

3.35

3.37

3.49

3.49

3.55

3.32

3.39

3.35

3.68

3.74

3.29

3.32

3.29

3.63

4.03

3.23

3.30

3.60

3.32

3.35

3.64

3.50

3.39

3.87

3.78

3.97

3.85

3.96

3.78

3.77

3.90

4.12

4.08

3.63 

3.48

3.90

3.79

3.66

3.91

3.75

3.86

3.72

3.42

1.57

2.59

3.39

2.85

2.87

2.54

3.36

3.22

2.90

4.55

3.96

3.77

3.21

2.43

3.22

2.21

3.24

2.43

3.67

2.98

3.24

3.01

2.34

3.23

2.97

2.81

2.78

2.25

2.88

3.12

3.14

2.23

2.22

3.08

3.02

2.35

3.23

3.07

2.47

4.50

3.97

3.43

1.92

1.74

1.97

1.80

1.83

1.86

1.96

1.65

1.46

2.29 

2.38

2.24

2.48

4.30

3.24

3.56

3.18

3.73

1.42

0.94

0.87

0.64

0.79

0.92

0.80

0.44

0.47

0.63

0.41

0.86

0.71

0.80

0.98

0.73

0.98

0.67

0.97

0.67

0.71

0.74

0.71

1.03

0.78

0.87

0.93

0.92

0.98

0.89

0.87

0.73

0.96

1.02

0.88

0.86

1.00

0.80

0.93

0.84

0.21

0.29

0.36

0.84

0.82

1.00

0.86

1.03

0.98

0.98

0.98

0.77

0.80 

0.73

0.66

0.55

0.23

0.30

0.27

0.27

0.22

0.78

Oxide

Sample 

Number

B337

B338

B339

B340

B341

B342

B343

B344

B345

B346

B347

B348

B350

B351

B352

B353

B354

B355

B356

B357

B358

B359

B360

B361

B363

B364

B366

B367

B368

B369

B370

B371

B372

B373

B374

B375

B376

B377

B378

B380

B381

B382

B383

B384

B385

B386

B387

B388

B389

B390

B391

B392

B394

B395

B396

B397

B398

B399

B400

B401

B402

B403

B404

B405

B406

Si0 2

69.53

63.95

63.45

63.34

54.16

60.27

64.76

63.46

65.94

74.21

62.31

74.94

68.91

68.83

63.36

63.03

67.46

68.21

68.71

61.38

64.19

61.53

68.74

68.55

64.47

74.69

69.53

75.02

74.22

75.92

65.54

65.44

65.43

64.18

64.46

62.31

62.99

65.19

67.17

65.15

62.76

64.47

64.38

65.79

64.08

64.13

73.77

75.54

74.26

69.09

70.98

61.90

66.46

65.11

72.41

67.15

64.77

67.67

68.40

61.08

69.23

61.11

66.67

63.25

71.33

"2°3

14.58

19.74

16.86

16.31

19.25

16.86

15.94

16.10

15.13

13.37

16.75

13.45

15.74

15.77

16.31

17.21

15.64

15.09

15.91

16.34

16.06

16.61

15.54

16.29

14.07

13.51

15.68

12.81

14.10

12.82

15.12

17.12

16.48

18.02

16.73

18.36

17.20

17.19

16.40

17.77

18.45

17.64

17.84

17.82

17.32

15.30

14.91

13.20

13.97

16.81

16.02

19.52

16.65

16.82

15.00

17.17

17.41

16.58

16.57

16.88

14.42

16.54

16.13

17.39

13.91

FeO

3.66

3.97

5.04

5.56

7.65

6.45

5.18

5.73

5.35

2.41

7.11

2.03

3.99

3.82

5.66

5.36

4.45

4.01

4.03

6.38

5.44

6.28

4.08

3.65

6.32

2.14

3.63

1.06

2.06

1.86

5.12

4.11

4.34

4.03

5.04

4.26

5.60

4.54

4.20

4.20

4.41

4.25

4.00

3.64

4.54

4.44

1.79

1.59

1.92

2.61

2.09

3.93

3.94

4.02

1.87

3.25

4.19

3.45

3.01

6.39

4.16

6.93

5.20

4.94

3.20

MgO

1.64

0.89

2.65

2.81

4.80

3.51

2.60

2.94

2.48

0.50

1.31

0.42

1.24

1.37

2.74

2.63

1.76

1.67

1.14

3.58

2.74

3.30

1.29

1.38

3.11

0.61

1.20

2.49

0.56

0.45

2.59

1.81

1.80

1.90

1.88

3.14

2.63

1.95

1.60

1.86

2.14

1.82

1.90

1.43

2.15

4.08

0.45

0.51

0.49

0.94

0.81

1.69

1.72

2.03

0.71

1.30

1.99

1.40

1.17

3.19

1.98

2.86

0.38

2.75

2.05

CaO

3.84

4.35

6.29

5.92

9.01

7.04

5.49

5.57

5.31

2.01

6.90

1.68

3.45

3.63

6.04

6.45

4.31

3.95

3.31

6.89

5.72

6.72

3.72

3.49

5.43

2.16

3.51

0.91

2.14

1.39

4.85

5.43

5.07

5.35

5.71

5.58

5.43

5.75

4.97

5.44

6.08

5.51

5.85

4.91

5.69

6.51

1.48

1.30

1.40

4.12

3.53

5.09

4.71

5.45

2.84

4.06

5.06

4.22

4.25

6.55

2.84

6.34

5.08

5.41

2.66

Se 2 0

3.35

5.36

3.81

3.81

3.06

3.63

3.54

3.64

3.44

4.21

3.54

4.28

3.92

4.11

3.34

3.49

3.50

3.63

4.06

3.28

3.65

3.15

4.39

4.05

3.79

4.11

4.33

3.85

3.92

3.75

3.45

4.03

3.82

4.26

3.34

4.20

3.33

3.97

3.89

3.80

4.20

4.13

4.01

4.19

4.00

3.27

3.64

4.19

4.36

4.51

4.33

4.63

3.91

3.95

3.57

4.08

3.91

3.85

4.65

3.50

2.86

3.78

3.61

3.35

2.46

K2 0

2.87

1.38

1.20

1.54

1.08

1.44

1.81

1.81

1.70

3.03

1.25

2.97

2.27

2.02

1.89

1.20

2.27

2.88

2.35

1.42

1.52

1.67

1.76

2.15

2.09

2.51

1.69

3.75

2.72

3.58

2.51

1.29

2.17

1.49

2.15

1.39

2.06

0.81

1.25

1.19

1.12

1.38

1.20

1.58

1.36

1.77

3.72

3.47

3.39

1.50

1.87

2.48

1.89

1.75

3.28

2.40

1.84

2.19

1.47

1.62

3.58

1.55

2.23

2.14

3.76

2

0.53

0.37

0.70

0.71

0.98

0.80

0.67

0.76

0.64

0.25

0.82

0.24

0.49

0.45

0.67

0.64

0.61

0.56

0.49

0.74

0.67

0.74

0.48

0.44

0.72

0.27

0.42

0.10

0.27

0.22

0.82

0.77

0.90

0.78

0.69

0.77

0.77

0.60

0.52

0.59

0.84

0.81

0.82

0.64

0.87

0.50

0.24

0.19

0.22

0.42

0.36

0.75

0.72

0.87

0.32

0.58

0.83

0.63

0.49

0.79

0.93

0.90

0.69

0.77

0.63
APPENDIX 

1 39

APPENDIX 1. Continued

Oxide

Sample 

Number S1o2 "A FeO MgO CaO »a

20K20 Ti02

Perris block Continued

B407

B408

B409

B410

B411

B412

B413

B415

B416

B417

B418

B420

B421

B422

B423

B424

B425

B426

B427

B428

B429

B430

B431

B432

B433

B434

B435

B436

B437

B438

B439

B440

B441

B442

B447

B448

B449

B450

B451

B452

B453

B454

B455

B456

B458

B459

B460

B461

B462

B464

B465

B466

B469

B470

B471

B472

B473

B474

B475

71.97

64.37

66.48

66.65

65.14

57.13

67.00

67.93

74.79

62.39

74.14

61.13

76.29

72.74

63.51

74.15

72.13

68.22

62.88

77.04

59.97

65.65

67.18

64.33

65.94

70.65

64.42

62.94

65.61

64.17

65.64

69.98

66.77

66.11

70.07

62.42

66.36

74.09

69.88

67.00

66.51

66.04

67.83

66.25

74.36

76.20

74.83

75.88

70.01

72.75

74.85

73.21

74.91

75.04

79.10

72.51

67.36

65.86

75.82

15.41

16.61

16.31

16.19

16.76

20.18

15.46

15.11

14.39

15.83

13.87

17.45

12.85

14.53

15.79

15.09

14.60

15.38

16.01

12.35

18.83

16.57

15.35

17.09

16.24

15.59

17.04

17.50

17.31

17.32

16.80

15.40

16.47

15.96

16.05

17.82

16.12

14.15

15.54

15.78

16.59

16.62

15.76

15.98

13.84

13.31

13.70

12.09

14.12

13.77

13.50

13.99

13.46

13.41

10.92

14.55

15.86

15.06

12.99

2.02

4.85

3.92

3.84

4.93

6.42

4.51

4.08

1.22

5.85

1.64

6.66

1.64

2.29

5.91

1.17

2.12

4.27

6.01

0.99

5.67

4.38

4.73

4.81

4.31

2.64

4.52

3.05

3.76

4.50

3.85

3.59

4.01

4.54

2.69

4.49

4.55

1.48

3.37

3.96

4.09

3.88

4.00

4.49

Santa

2.27

1.46

1.97

2.54

4.19

3.02

2.12

3.02

2.06

2.33

1.30

2.71

4.86

5.09

1.98

0.62

2.44

1.81

2.13

0.20

3.58

2.15

2.05

0.37

3.78

0.41

2.73

0.85

0.64

3.06

0.42

0.86

1.58

3.13

0.20

1.99

2.10

1.99

2.35

2.27

1.08

2.18

5.69

1.78

2.10

1.91

1.00

1.78

1.98

0.90

2.21

2.15

0.47

1.29

1.82

1.76

1.87

1.80

1.93

2.61

5.60

5.04

4.67

9.30

7.17

4.40

3.85

1.75

6.13

1.71

6.29

1.15

2.19

5.44

2.04

2.62

4.19

6.51

0.89

5.70

4.79

4.16

5.40

4.93

3.46

5.58

4.18

4.97

5.25

5.10

3.58

4.61

4.85

3.38

6.18

4.54

1.59

3.77

4.73

4.39

4.57

3.91

4.90

4.09

3.68

3.87

3.73

2.59

3.66

3.48

3.29

3.62

3.11

3.52

3.06

3.01

3.42

3.08

4.21

3.59

4.00

3.47

3.47

7.18

3.11

3.50

3.30

3.63

4.04

3.97

4.19

4.19

3.79

3.98

4.19

3.71

3.77

3.95

4.90

3.64

3.19

3.79

3.48

3.64

3.63

3.50

3.77

2.93

1.69

1.92

2.25

0.61

1.06

2.36

3.22

3.73

2.09

4.45

1.73

3.94

3.90

2.47

2.73

3.79

1.79

1.13

4.95

0.10

2.82

2.47

1.97

2.06

2.19

1.51

1.86

1.72

2.09

2.04

1.82

1.90

1.98

2.50

1.09

2.00

4.81

1.92

2.45

2.29

2.63

2.50

1.88

0.34

0.75

0.65

0.54

0.47

0.80

0.62

0.49

0.13

0.81

0.26

0.95

0.27

0.29

0.73

0.17

0.30

0.57

0.85

0.10

0.57

0.59

0.63

0.75

0.62

0.34

0.77

0.57

0.66

0.78

0.67

0.44

0.74

0.81

0.47

0.89

0.63

0.22

0.44

0.79

0.75

0.75

0.69

0.81

Ana block

0.35

0.17

0.40

0.38

1.36

0.89

0.28

0.31

0.48

0.35

0.05

0.54

1.44

2.74

0.38

1.78

1.11

1.97

1.48

3.27

2.50

1.41

1.79

2.03

1.76

0.73

2.35

4.07

5.17

1.69

4.25

4.02

4.27

3.91

3.49

3.58

3.96

4.42

3.88

3.85

3.52

4.29

4.09

3.30

3.56

2.88

3.57

2.61

3.50

2.97

3.09

3.66

2.97

2.92

2.97

4.23

2.70

1.68

2.13

3.35

0.27

0.17

0.25

0.22

0.59

0.41

0.22

0.29

0.25

0.28

0.15

0.34

0.65

0.65

0.23

Oxide

Sample 

Number SiO A1 7°3

B476

B478

B479

B480

B482

B484

B485

B486

B487

B489

B490

B491

B492

B493

B494

B495

B496

B497

B498

B499

B500

B502

B503

B504

B506

B507

B508

B510

B513

B514

B515

B516

B517

B518

B519

B520

B521

B522

B523

B524

B525

B528

B529

B530

B531

B533

B536

B537

B538

B539

B540

B541

B542

B543

B544

B546

B547

B548

B549

B550

B551

B553

B555

B556

B557

70.82

69.63

74.84

75.24

77.21

59.55

73.26

65.71

58.14

74.18

75.99

75.16

67.26

71.19

64.42

64.55

72.59

67.14

61.14

66.62

61.79

65.93

60.08

74.79

71.54

66.05

72.63

74.43

53.86

56.68

77.17

76.96

69.05

60.46

63.48

73.16

73.95

60.40

58.70

64.04

65.91

73.17

61.20

59.81

61.53

54.76

55.28

59.88

73.04

72.52

72.49

72.78

70.34

56.32

64.55

65.75

59.48

64.05

70.45

76.45

72.03

77.36

63.72

65.54

59.80

13.92

14.86

13.70

13.34

12.75

18.10

14.53

15.93

18.37

14.45

13.35

13.65

15.67

15.44

16.05

15.80

14.03

14.72

16.05

15.12

16.72

16.87

17.45

13.91

14.66

15.78

14.55

13.80

18.93

18.26

12.41

12.82

14.43

17.06

15.92

13.92

14.32

17.46

17.73

15.29

14.92

14.08

17.19

17.49

16.46

18.75

17.66

16.86

14.10

14.36

14.31

13.91

14.97

17.46

16.75

15.90

17.81

16.90

14.68

12.97

15.33

12.96

16.68

15.91

18.24

FeO

3.71

3.76

2.37

2.04

1.32

6.58

2.26

4.70

6.79

1.54

1.49

2.01

4.42

2.47

5.21

5.10

3.62

4.88

6.64

6.10

6.06

3.35

6.19

1.79

3.21

4.78

2.70

2.14

8.14

7.03

1.74

1.79

4.54

6.14

5.67

3.08

2.22

6.20

6.83

6.01

5.22

2.97

6.03

6.14

6.36

7.82

8.06

6.88

2.67

3.06

2.71

3.07

3.96

7.56

5.30

5.04

6.10

4.74

3.91

1.35

3.03

0.45

5.19

4.68

5.95

MgO

1.45

1.64

0.35

0.45

0.05

3.25

0.55

2.43

3.65

0.13

0.23

0.22

1.88

0.39

2.75

2.95

0.74

2.23

3.69

1.74

3.22

1.67

3.43

0.37

0.74

2.00

0.54

0.44

4.64

4.29

0.02

0.15

1.68

3.82

3.12

0.40

0.37

3.24

3.71

2.71

2.32

0.37

3.14

3.82

3.24

4.96

4.93

3.67

0.62

0.65

0.60

0.65

0.82

4.94

2.33

1.81

3.54

2.43

0.84

0.02

0.60

0.02

2.51

2.34

3.15

CaO

3.33

3.72

1.81

1.93

0.77

6.76

2.17

5.19

7.72

1.18

1.26

1.62

4.42

2.48

5.39

5.52

2.75

4.70

6.50

4.39

6.13

6.34

7.25

1.91

2.73

4.96

2.45

2.17

9.16

8.27

0.93

1.71

4.11

6.88

5.59

2.07

2.00

6.65

7.37

5.65

5.17

2.25

6.20

7.12

6.10

8.48

8.75

6.79

2.33

2.75

2.34

2.35

3.24

8.43

5.63

4.56

6.55

5.67

2.87

0.51

2.44

0.70

5.80

4.80

6.48

»a20

3.66

3.68

3.54

3.79

4.12

3.80

3.70

3.89

3.62

4.64

3.87

4.03

3.47

5.51

3.59

3.67

4.22

3.78

3.49

3.79

3.55

3.70

3.47

3.77

4.46

4.39

4.47

4.15

3.61

3.48

4.19

4.35

3.67

3.57

3.78

4.69

4.40

3.84

3.62

4.05

3.96

4.78

3.57

3.42

3.34

3.40

3.39

3.43

4.15

4.52

4.20

4.11

4.91

3.40

3.57

3.66

3.94

3.91

4.23

3.89

4.25

3.69

3.77

3.83

3.85

K20

2.67

2.26

3.14

2.97

3.68

1.12

3.24

1.53

0.86

3.73

3.64

3.09

2.27

2.24

1.92

1.73

1.57

1.79

1.59

1.50

1.70

1.82

1.33

3.23

2.28

1.44

2.33

2.60

0.71

1.13

3.41

2.04

1.96

1.29

1.71

2.38

2.49

1.42

1.19

1.43

1.75

2.08

1.93

1.47

2.11

0.85

1.00

1.67

2.75

1.75

3.00

2.77

1.23

1.07

1.33

2.60

1.60

1.51

2.50

4.72

1.98

4.74

1.48

2.14

1.57

2

0.44

0.47

0.25

0.25

0.10

0.85

0.29

0.62

0.85

0.13

0.18

0.22

0.61

0.29

0.67

0.68

0.48

0.76

0.90

0.75

0.83

0.34

0.79

0.23

0.39

0.59

0.32

0.27

0.95

0.86

0.13

0.18

0.55

0.78

0.74

0.30

0.23

0.81

0.86

0.81

0.76

0.30

0.74

0.73

0.86

0.96

0.93

0.83

0.34

0.39

0.34

0.37

0.52

0.81

0.54

0.67

0.98

0.79

0.52

0.10

0.34

0.08

0.85

0.76

0.96
40 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

APPENDIX 2 

Mixing proportions

End member

Sample 

Number

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

B

1

2

3

4

5

6

7

8

9

10

11

12

13

14

15

16

17

18

19

20

21

22

23

24

25

26

27

28

29

30

31

32

33

34

35

36

37

38

39

40

41

42

43

44

46

47

48

M-l M

San

1.2174

0.9619

0.

1.

0.

1.

1.

1.

1.

0.

0.

.9302

,2767

,9208

,2507

,1276

,2485

,1917

7177

,6233

0.8445

0.

0.

1.

0.

1.

1.

0.

0.

0.

0.

0.

0.

1.

0.

0.

0.

0.

1.

0.

0.

0.

0.

1.

0.

0.

0.

0.

1.

0.

0.

0.

0.

7706

9792

1089

9389

0423

1551

8019

5837

9391

7831

8008

9681

1512

7134

7229

3545

6434

0392

5875

9966

6869

8412

0494

8666

7273

7242

9959

1020

5382

9570

7424

3696

0.7325

0.

1.

6038

0573

-2

Gabriel

0

0

0

0

0

1

0

0

1

1

1

0

0

.9289

.8786

.6186

.7197

.9135

.2092

.9123

.7044

.0451

.2399

.1228

.8223

.9073

0.4384

0

0

0

1

1

1

0

.5788

.5381

.8977

.1495

.4285

.5388

.7171

0.4762

0 .6209

0.5208

1

1

0

1,

0

0

1

.2196

.2828

.6464

.1692

.9085

.7829

.1692

0.7151

0

0,

1

0

0,

0

.5134

.9545

.1927

.9352

.7084

.4060

0,3676

0,.6300

0.3488

0,.5350

0.8197

0.8393

1.

1,

.1015

.1752

0.9368

D-l D-2

block

-0.

-0.

-0.

-0.

-0.

-0.

-0.

,6709

,5231

,3118

5559

,3952

7926

5895

-0.6100

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

7145

4496

2827

3519

3155

2641

3939

2886

4700

6630

5291

3978

3907

1414

2773

2828

7038

4335

2956

1861

2393

4777

3648

4309

-0.1251

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

3684

6240

3847

2085

0590

2722

4273

0236

3101

2780

0817

4289

3727

5685

-0.

-0.

-0.

-0.

-0.

-0.

,4755

,3174

,2369

,4404

,4391

,6673

-0.4504

-0.

-0.

3429

,5224

-0.5080

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

4634

3150

3624

1535

2937

1884

4700

6416

7014

7248

2654

1178

1444

2061

-0.6670

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

5626

0737

3376

3126

3444

3919

2808

0752

4272

6180

4171

2272

0712

0913

3047

0894

1818

2841

1272

4051

4064

4256

San Bernardino block

B 54 0.7080 1.2247 -0.4546 -0.4781

B 55 0.7045 1.0839 -0.3346 -0.4538

B 56 0.5472 0.7952 -0.1855 -0.1568

B 57 0.4363 0.7923 -0.0867 -0.1418

B 58 0.5181 0.8350 -0.1629 -0.1903

B 59 0.5160 0.8225 -0.1667 -0.1718

B 60 0.5270 1.0037 -0.2191 -0.3116

B 61 0.7139 0.6223 -0.1693 -0.1669

B 62 0.4926 0.7891 -0.1410 -0.1407

B 63 0.5426 1.1837 -0.2808 -0.4455

End member

Sample 

Number

B 64

B 65

B 66

B 67

B 68

B 69

B 70

B 71

B 72

B 74

B 75

B 78

B 79

B 80

B 81

B 85

B 86

B 94

B 95

B 96

B 97

B 98

B 99

B100

B101

B102

B103

B104

B105

B106

B107

BIOS

B109

B110

Bill

B112

B113

B114

B115

B116

B117

B118

B120

B121

B124

B125

B127

B128

B129

B130

B131

B132

B133

B134

B135

B136

B137

B138

B139

B140

B141

B142

B143

B144

B145

M-l

0.

0.

0.

0.

0.

6369

8435

4837

3876

5702

0.7879

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

1.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

1.

0.

0.

1.

0.

0.

0.

1.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

5139

7682

5272

8694

8799

5754

9923

7478

8413

4104

0616

2961

3964

9281

5656

6223

1145

6653

6535

5175

4882

6614

2093

7563

6321

2012

6404

7476

2485

1397

7591

8734

6849

7195

8083

6657

5096

5248

8158

7314

4719

5882

4652

4224

6876

7061

6287

8028

5352

6184

6047

6140

6512

5243

5696

4753

5632

6402

5508

M-2

1.

1.

1.

0.

1.

1.

0.

0.

1.

0.

1.

1.

0.

0.

1.

1.

1.

1.

1.

1.

0.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

0.

1.

1.

1.

1.

1.

1. 'l.

0.

1.

1.

1.

1.

1.

1.

1.

0.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

1.

3884

2957

0171

9667

3892

0210

8303

9463

4569

6447

2560

1626

9954

8041

0596

1881

4356

3932

4304

2204

7990

0403

1810

2826

0780

0506

2123

0296

2510

2086

2025

6206

5559

5435

7961

3705

5381

5886

2952

7742

0521

3399

3764

1163

2503

2730

3466

8055

4625

3774

3436

2742

4218

3048

2980

2242

2280

2863

2892

3352

2175

3185

2942

2850

2966

D-l

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

4281

5139

1670

1231

3572

4022

1225

3541

3500

2744

5439

3299

5698

2722

-0.4558

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

1866

6989

2011

2761

5649

1500

3450

0293

4638

3283

2423

2585

3529

7557

4381

3601

4870

3669

4569

2146

6659

4642

5394

4731

2294

4734

4026

2935

2401

4657

4523

2979

1571

2998

2644

4301

4245

4263

5161

3801

3616

3425

3714

3958

3205

3343

2846

3429

3720

3306

D-2

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

5972

6253

3337

2312

6022

4067

2218

3604

6341

2397

5920

4082

4178

2797

4451

4119

7983

4882

5507

5835

2146

3177

3249

4840

4032

3257

4420

3381

7046

5268

4746

3349

8295

8342

8300

8443

8331

9226

5070

2643

3870

6030

5925

4011

6004

5521

5205

2365

6279

5354

6011

5557

6241

5915

4530

4811

4901

5289

5446

5392

4528

5091

5145

5532

5168

End member

Sample

Number

B146

B147

BUS

B149

B150

B151

B152

B153

B155

B156

B157

B158

B159

B160

B161

B162

B163

B164

B165

B166

B168

B169

B170

B171

B172

B173

B174

B175

B176

B177

B178

B179

B180

B181

B182

B183

B184

B185

B186

B187

B188

B189

B190

B191

B192

B193

B194

B195

B196

B197

M-l

0.7554

0.5304

0.6137

0.6469

0.5771

0.5503

0.6898

0.6108

0.4314

0.6582

0.5937

0.5699

0.6619

0.8222

0.6458

0.7669

0.7325

0.6338

0.9658

0.8182

0.7335

0.8207

0.8835

0.7430

1.0757

0.3673

0.5195

0.5281

0.7910

0.5045

0.4426

0.8881

0.7911

0.7332

0.5015

0.5930

0.0000

0.4551

0.6726

0.5206

0.4868

0.6386

0.5585

0.4142

0.5742

0.6465

0.6755

0.6606

0.4675

0.4803

M-2

1.2815

1.2744

1.2324

1.2973

1.2738

1.1946

0.8747

1.0084

0.8466

0.9458

1.2770

0.6217

0.8163

0.7752

0.9970

1.0411

1.1465

0.5702

1.2500

0.4391

0.5355

0.4652

0.9454

0.9793

0.4596

1.4962

1.3222

1.2866

1.0308

1.3977

1.5445

0.5737

1.1830

1.3216

1.3937

1.2168

1.8051

1.1473

1.1476

1.2551

1.2859

1.4182

1.3280

1.4301

1.2855

1.3172

1.0501

1.3934

1.0851

1.4336

D-l

-0.4623

-0.3194

-0.3650

-0.4073

-0.3536

-0.3100

-0.2527

-0.3028

-0.0503

-0.2783

-0.3885

-0.0971

-0.1758

-0.2971

-0.2746

-0.3915

-0.4256

-0.0955

-0.5862

-0.1585

-0.1201

-0.1485

-0.5081

-0.3765

-0.3519

-0.2835

-0.2926

-0.3003

-0.4448

-0.3611

-0.3357

-0.3306

-0.4966

-0.4761

-0.2884

-0.2818

-0.0365

-0.2176

-0.3764

-0.3147

-0.2640

-0.4551

-0.3777

-0.3084

-0.3648

-0.4323

-0.3523

-0.4458

-0.2234

-0.3356

D-2

-0.5746

-0.4854

-0.4811

-0.5369

-0.4973

-0.4349

-0.3118

-0.3163

-0.2276

-0.3258

-0.4822

-0.0945

-0.3024

-0.3003

-0.3683

-0.4165

-0.4535

-0.1084

-0.6295

-0.0987

-0.1489

-0.1373

-0.3209

-0.3458

-0.1834

-0.5801

-0.5492

-0.5144

-0.3771

-0.5411

-0.6514

-0.1312

-0.4775

-0.5787

-0.6068

-0.5280

-0.7686

-0.3848

-0.4438

-0.4610

-0.5087

-0.6017

-0.5087

-0.5359

-0.4950

-0.5313

-0.3733

-0.6082

-0.3292

-0.5783

Little San Bernardino block

B198

B199

B200

B201

B202

B203

B204

B205

B206

B207

0.4478

0.8866

0.9771

0.7056

0.2879

0.3669

1.0912

0.3380

0.9024

0.9836

1.3347

1.2342

1.0126

1.1290

1.4270

1.3695

1.2119

1.4218

1.4280

1.2223

-0.3044

-0.5413

-0.6330

-0.3941

-0.2046

-0.2850

-0.6478

-0.1933

-0.5792

-0.6171

-0.4782

-0.5795

-0.3567

-0.4406

-0.5103

-0.4514

-0.6554

-0.5665

-0.7512

-0.5889
APPENDIX 2 41

APPENDIX 2. Continued

End member

Sample 

Number

Little

B208 

B209 

B210

B211

B212

B213

B214

B215

B216

B217

B218

B219

B220

B221

B222

B223

B224

B225

B226

B227

B228

B229

B230

B231

B232

B233

B234

B235

B236

B237

B238

B239

B240

B241

B242

B243

B244

B245

B246

B247

B248

B249

B250

B251

B252

B253

B254

B255

B256

B257

B258

B259

B260

B261

B262

B263

B264

B265

B266

B267

M-l M-2 D-l D-2

San Bernardino block Continued

1.3615 

1.3327 

0.8695

1.0856

1.0926

0.6930

1.1242

1.1917

0.5367

0.8028

1.2019

0.8707

0.8327

0.9761

0.9861

San

0.9859

0.5269

0.8099

0.3335

0.3873

0.7662

0.3394

0.7027

0.7688

0.5791

0.9301

0.8227

0.9812

0.7323

0.6757

0.7945

0.7069

0.7020

0.7869

0.7418

0.6834

0.9483

0.8296

0.8339

0.9322

1.0296

0.6344

0.5227

0.8156

0.7942

0.7450

0.8024

0.7274

0.6158

0.5904

0.7911

0.8759

1.0092

0.6684

0.6928

1.0899

0.9418

0.8129

0.1626

0.4676

1.1131 

0.9114 

0.8661

0.9661

0.9137

0.6728

0.4543

1.2863

0.9199

1.2984

0.7027

0.9628

1.1981

0.7734

0.7372

-0.8115 

-0.6194 

-0.3869

-0.6212

-0.5971

-0.1555

-0.3542

-0.7610

-0.1936

-0.4994

-0.6238

-0.4292

-0.5017

-0.3945

-0.3458

-0.6631 

-0.6246 

-0.3487

-0.4305

-0.4092

-0.2103

-0.2242

-0.7171

-0.2630

-0.6017

-0.2808

-0.4043

-0.5290

-0.3550

-0.3775

Jacinto block

0.6163

1.1874

0.7333

0.8727

0.8940

0.9098

0.6504

0.8791

0.9180

0.6307

0.7230

0.7338

0.7210

0.9621

0.6984

0.8537

0.7113

0.7919

0.7907

0.7718

0.7075

0.6390

0.7806

0.9386

0.7245

0.8927

0.9222

1.0323

0.5936

0.7917

0.7447

0.7573

1.4937

0.8424

0.7457

0.7382

1.2565

0.6565

0.7997

1.0889

0.9518

1.1636

0.6700

1.7666

1.6743

-0.4217

-0.2494

-0.3553

0.0324

-0.0063

-0.3189

-0.0075

-0.2533

-0.3496

-0.1327

-0.2860

-0.3230

-0.4435

-0.2682

-0.2248

-0.3348

-0.2417

-0.2888

-0.3413

-0.2798

-0.2253

-0.2984

-0.3135

-0.4089

-0.4146

-0.5081

-0.2490

-0.2031

-0.2161

-0.3493

-0.2511

-0.3275

-0.4254

-0.1786

-0.1681

-0.2928

-0.4897

-0.4307

-0.2364

-0.3289

-0.5424

-0.5102

-0.2551

-0.1621

-0.2933

-0.1804

-0.4648

-0.1879

-0.2386

-0.2749

-0.3571

0.0177

-0.3286

-0.3372

-0.0771

-0.3670

-0.2334

-0.2587

-0.4262

-0.1493

-0.3134

-0.1766

-0.2051

-0.2363

-0.2338

-0.1656

-0.2888

-0.2967

-0.3636

-0.2421

-0.4142

-0.3075

-0.3520

-0.1931

-0.2366

-0.2386

-0.2322

-0.7958

-0.2796

-0.1680

-0.2364

-0.6427

-0.2350

-0.2317

-0.4529

-0.4993

-0.5951

-0.2279

-0.7672

-0.8486

End member

Sample

Number

B268

B269

B270

B271

B272

B273

B274

B275

B276

B277

B278

B279

B280

B281

B282

B283

B284

B285

B286

B287

B288

B289

B290

B291

B292

B293

B294

B295

B296

B297

B298

B299

B300

B301

B302

B303

B304

B305

B306

B307

B308

B309

B310

B311

B312

B313

B314

B315

B317

B318

B319

B320

B321

B322

B323

B324

M-l

1

0

1

1

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

1

1

0

0

0

0

0

0

0

0

1

.0436

.7386

.5060

.2724

.7592

.9636

.4859

.4204

.6237

.5948

.5477

.9333

.9770

.7293

.4173

.1947

.2175

.3901

.4279

.5701

.6260

.6420

.6324

.5500

.8084

.6962

.7272

.4824

.3890

.3528

.4075

.3154

.4704

.3563

.2546

.1444

.3335

.6179

.0977

.3589

.3225

.3749

.5617

.5814

.2970

.1211

.2809

.7331

.7599

.5452

.7249

.4567

.2819

.7896

.6313

.1072

M-2

0

0

1

1

0

0

0

1

0

0

0

1

0

1

1

1

1

0

0

1

0

0

0

1

0

0

0

0

1

0

0

0

0

0

0

1

0

0

0

0

0

1

0

0

1

1

1

0

.9379

.5526

.1208

.1995

.7880

.5577

.8500

.1421

.8767

.7799

.8156

.0080

.9052

.0214

.4874

.1170

.1809

.9863

.7348

.0460

.7331

.9983

.7067

.1095

.9822

.9963

.9919

.6804

.0707

.9094

.8574

.8865

.6234

.9111

.9323

.0893

.6797

.5864

.9747

.9237

.7292

.0721

.8145

.7289

.3622

.3030

.0455

.6313

0.6091

0

0

0

0

0

0

0

.6453

.6300

.6404

.6737

.6504

.5529

.5289

D-l

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

4854

2010

8940

7740

9433

3389

1016

1659

1874

1031

1293

4850

5050

3135

2221

0732

0330

0627

0064

2011

1171

2687

1502

2079

3271

2730

2983

0083

0928

-0.0053

-0.

-0.

-0.

0.

0.

0.

0.

-0.

0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

0096

0172

0057

0039

0568

0494

0641

1186

1468

0018

0577

0838

0804

1146

8076

6676

7273

1986

2398

0892

2229

0264

0641

2489

1475

4441

D-2

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

4961

0901

7327

6979

6039

1824

2343

3966

3130

2716

2340

4563

3773

4372

6825

3850

3655

3137

1691

4150

2420

3716

1890

4516

4634

4195

4208

1546

3669

2569

2552

1847

0882

2713

2437

2832

0773

0857

2192

2808

1094

3632

2958

1957

8516

7565

5991

1658

1292

-0.1013

-0.

-0.

-0.

-0.

-0.

-0.

1320

0707

0197

1910

0368

1920

Perris block

B325 1.0270 0.6908 -0.3763 -0.3415

B326 1.2220 0.6021 -0.4297 -0.3943

B327 1.4513 0.5810 -0.6315 -0.4008

B328 1.3916 0.7255 -0.6483 -0.4688

B330 1.7953 0.9791 -0.9467 -0.8277

End member

Sample 

Number

B331

B332

B333

B334

B336

B337

B338

B339

B340

B341

B342

B343

B344

B345

B346

B347

B348

B350

B351

B352

B353

B354

B355

B356

B357

B358

B359

B360

B361

B363

B364

B366

B367

B368

B369

B370

B371

B372

B373

B374

B375

B376

B377

B378

B380

B381

B382

B383

B384

B385

B386

B387

B388

B389

B390

B391

B392

B394

B395

B396

B397

B398

B399

B400

B401

M-l

1

1

1

1

1

1

1

1

1

0

1

1

1

1

2

1

2

1

1

1

1

1

1

1

.5502

.4352

.5518

.4987

.2551

.3087

.1805

.4054

.5226

.5722

.3682

.4111

.4100

.6812

.0244

.2062

.0263

.4198

.6113

.2370

.2389

.2425

.2820

.4016

1.4453

1

1

1

1

2

2

1

2

1

1

1

1

0

0

0

0

0

1

1

1

0

0

0

0

1

1

1

1

1

1

1

0

1

0

1

0

0

0

1

1

.5523

.1839

.8643

.3819

.0647

.0905

.8375

.0478

.7444

.8090

.2524

.1371

.8761

.8987

.8425

.9793

.8043

.4700

.5581

.0473

.8412

.9697

.8729

.9437

.0219

.7529

.0528

.9236

.7926

.4990

.5496

.3044

.0670

.9725

.0863

.8499

.7902

.9724

.6440

.2272

M-2

0

1

0

1

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

.9483

.0775

.9864

.1368

.3337

.8591

.3435

.3488

.3666

.1931

.2810

.4971

.4402

.4779

.8481

.3612

.8663

.6986

.6087

.5046

.3859

.7050

.7921

.6942

.3245

.4009

.4262

.4958

.6714

.3651

.8017

.5314

.9741

.9050

.0659

.6511

0.4786

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

0

0

0

0

.6609

.4922

.6663

.3972

.6020

.3375

.4664

.4904

.4006

.4813

.4801

.5656

.4591

.4200

.1913

.9767

.9340

.5528

.6817

.6424

0.6235

0

1

0

0

0

0

0

.5664

.0770

.7583

.6071

.7382

.4768

.3712

D-l

-0

-0

-0

-0

-0

-0

-0

-0

-0

0

-0

-0

-0

-0

-1

-0

-1

.8582

.8182

.8744

.8786

.3420

.5859

.6150

.5089

.5774

.1996

.4121

.5270

.5073

.6754

.1517

.3572

.1735

-0.6824

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-1

-0

-1

-0

-1

-0

-0

-0

-0

.7936

.3927

.3839

.5080

.5759

.6872

.4348

.5916

.2977

.9396

.6709

.8853

.1718

.9395

.1496

.9761

.0442

.4604

.4329

.2943

.3191

-0.2210

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-0

-1

-1

-0

-0

-0

-0

.3103

.1637

.5895

.6848

.3671

.2394

.3410

.2686

.3808

.3388

.6622

.6190

.1362

.0611

.7762

.8332

.0475

.4249

-0.3392

-0

-0

-0

-0

-0

-0

.5842

.3735

.2416

.4102

.8424

.3480

D-2

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

6404

6945

6637

7569

2469

5819

0910

2453

3118

0352

2372

3812

3428

4837

7208

2102

7192

4360

4264

3489

2410

4395

4982

4086

3350

3615

3125

4205

3825

5446

7204

4295

8722

6733

8307

4430

1828

2427

0718

2878

0662

2427

2180

3397

1706

0024

1100

0844

1286

1422

5106

6251

7641

6655

2757

3981

1007

2656

1997

5791

2347

1558

3005

2784

2504
42 BATHOLITHIC ROCKS OF SOUTHERN CALIFORNIA

APPENDIX 2. Continued

End member

Sample 

Number M-l

Perris

B402

B403

B404

B405

B406

B407

B408

B409

B410

B411

B412

B413

B415

B416

B417

B418

B420

B421

B422

B423

B424

B425

B426

B427

B428

B429

B430

B431

B432

B433

B434

B435

B436

B437

B438

B439

B440

B441

B442

B447

B448

B449

B450

0

1

0

0

0

1

1

1

1

0

0

1

1

1

1

1

0

1

1

1

1

1

1

1

1

2

0

1

0

1

1

1

1

1

0

1

1

.6372

.3768

.9711

.6742

.7566

.2854

.1790

.2244

.2343

.9239

.4703

.3006

.1394

.2384

.2209

.0601

.6256

.3384

.0345

.1152

.5740

.1126

.6943

.5244

.4103

.6100

.6489

.3082

.7463

.2086

.5552

.1509

.4615

.0942

.7841

.0627

.7744

1.0250

1

1

1

1

0

.1911

.1217

.3424

.2736

.7420

M-2 D-l D-2

block Continued

1.

0.

0.

0.

1.

0.

0.

0.

0.

0.

0.

0.

0.

1.

0.

1.

0.

1.

1.

0.

0.

1.

0.

0.

1.

-0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

0.

1.

0920

3126

7182

6510

2203

9295

5061

5982

6591

5092

2809

6849

8811

2007

5101

2860

5349

2911

1845

6262

9303

1130

5408

3121

3798

3401

8630

7015

6594

6159

7281

4707

3951

5450

6277

6097

5888

6584

6003

8412

2424

6097

4328

-0. 1744

-0.4490

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-1.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

3703

1048

2567

7204

4077

5067

5153

1467

1185

5267

4749

7388

3363

6292

0153

7400

5660

3193

9321

6041

7948

5077

8749

3843

1454

5398

1526

4664

8070

4200

5794

4529

2259

4216

9042

-0.3863

-0.

-0.

-0.

-0.

-0.

4619

5649

5602

5074

4471

-0.5547

-0.2403

-0. 3189

-0.2204

-0.7202

-0.4945

-0. 2774

-0.3159

-0. 3781

-0.2864

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

1304

4588

5456

7003

3948

7169

1758

8895

6530

4221

5723

6215

4404

-0.3287

-0.

0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

9152

1144

3665

4698

2531

3581

4764

2016

2773

1863

1859

2508

4591

2970

3296

3980

0246

3760

7277

End member

Sample 

Number M-l M-2 D-l D-2

B451 1.5397 0.6778 -0.7416 -0.4759

B452 0.9229 0.7731 -0.3253 -0.3706

B453 0.8337 0.7454 -0.2872 -0.2919

B454 0.7106 0.7977 -0.2244 -0.2839

B455 1.0197 0.7925 -0.4010 -0.4112

B456 1.2100 0.5883 -0.4708 -0.3274

Santa Ana block

B458

B459

B460

B461

B462

B464

B465

B466

B469

B470

B471

B472

B473

B474

B475

B476

B478

B479

B480

B482

B484

B485

B486

B487

B489

B490

B491

B492

B493

B494

B495

B496

B497

B498

B499

1

1

2

2

1

1

1

1

1

1

2

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

1

2

1

.9135

.7670

.0496

.1629

.4343

.5710

.6721

.9508

.8732

.8369

.0347

.7620

.5866

.5042

.7422

.7772

.6282

.5948

.8548

.9808

.1093

.3515

.6495

.0815

.6731

.6631

.8256

.2329

.1502

.3882

1.5606

2

1

1

1

.2246

.7294

.4506

.7833

0 .8606

1.0704

0

0

0

0

1

0

0

0

1

0

0

0

1

0

.8175

.9533

.8453

.9421

.0488

.8012

.9285

.9476

.2250

.7959

.5076

.5765

.0713

.7606

0.6953

1

0

1

0

1

0

0

0

1

0

0

0

0

0

0

0

0

0

.0462

.9585

.0664

.2486

.0358

.4253

.1737

.9822

.1061

.9594

.7007

.5189

.5007

.4386

.5550

.4977

.3243

.4276

-1.

-1.

-1.

-1.

-0.

-0.

-0.

-1.

-1.

-1.

-1.

-0.

-0.

-0.

-0.

-0.

1011

0623

1759

2337

6722

8209

9802

1159

0555

0367

2098

9843

7271

5789

9861

8813

-0.7726

-0.

-1.

-1.

-0.

-0.

-0.

-0.

-1.

-0.

-1.

-0.

-1.

-0.

-0.

-1.

-0.

-0.

-0.

8869

0452

2051

2721

7494

6999

2007

0446

9912

0607

4954

2684

5172

6090

1734

7516

4534

7683

-0.

-0.

6730

7751

-0.6912

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-1.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

8826

6074

6921

7407

6360

7461

7479

0498

5736

3671

5018

8274

6565

5509

7542

7680

8421

0859

6378

3748

0545

6107

7781

7244

4382

4007

3717

3902

6061

4754

3215

4426

End member

Sample 

Number

B500

B502

B503

B504

B506

B507

B508

B510

B513

B514

B515

B516

B517

B518

B519

B520

B521

B522

B523

B524

B525

B528

B529

B530

B531

B533

B536

B537

B538

B539

B540

B541

B542

B543

B544

B546

B547

B548

B549

B550

B551

B553

B555

B556

B557

M-l

1

1

1

1

1

1

1

1

1

1

2

2

1

1

1

2

1

1

1

1

1

2

1

1

1

1

1

1

1

2

1

1

2

1

1

1

0

1

1

1

1

1

1

1

.2032

.2378

.1302

.5663

.9503

.9119

.9738

.9703

.0880

.0534

.1895

.5641

.8413

.3600

.5813

.2689

.9913

.2333

.1810

.8796

.7953

.3401

.0731

.1585

.0718

.0072

.3371

.2498

.8314

.2172

.7085

.8661

.3167

.4461

.4404

.1315

.9797

.1964

.7151

.4935

.7885

.3364

.2041

.2864

0.7757

M-2

0

0

.4107

.5842

0.3147

1

0

0

0

0

0

0

0

0

0

0

0

.0441

.6488

.3398

.6965

.8275

.0000

.1775

.9767

.7164

.5840

.2735

.3836

0.6373

0 .7746

0.2972

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

0

1

0

1

0

0

0

.2259

.2871

.4217

.5816

.4469

.3245

.4949

.0829

.0609

.3334

.8159

.5596

.8473

.8006

.3555

.0870

.4186

.6895

.3356

.4501

.6954

.2775

.6883

.3784

.4383

.5755

.3869

0-1

-0

-0

.3525

.5065

-0.2648

-0.8981

-1

-0

-1

-1

-0

-0

-1

-1

-0

-0

-0

-1

-1

-0

-0

-0

-0

-1

-0

-0

-0

-0

-0

-0

-1

-1

-0

-1

-1

-0

-0

-0

-0

-0

-0

-0

-0

-0

.0632

.8939

.1051

.1149

.1165

.1530

.3064

.4776

.8553

.3995

.6068

.2865

.1445

.3680

.2744

.7876

.7808

.3256

.2912

.2768

.2703

.0706

.2591

.3295

.0151

.2106

.9539

.0206

.2362

.3423

.5373

.4431

.2268

.4272

.8955

.9442

.9721

.8653

-0.4052

-0

-0

.5126

.1188

D-2

-0.

-0.

-0.

-0.

2615

3155

1800

7124

-0.5359

-0.

-0.

-0.

0.

-0.

-0.

-0.

3578

5652

6828

0285

0779

8598

8029

-0.5699

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

-0.

2339

3582

6197

6214

1625

1325

3791

4362

5961

2288

2062

2964

0195

1390

2537

6322

5662

6018

6461

4360

1908

3217

3779

0885

2193

5150

8267

5048

8495

2371

3493

0438

 £ 11.5. GOVERNMENT PRINTING OFFICE 1984 776-041/4035