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Compositional Characteristics of 

Middle to Upper Tertiary Volcanic Rocks 

of the Bolivian Altiplano 

By Edward A. du Bray, Steve Ludington, William E. Brooks, Bruce M. Gamble, 

James C. Ratte, Donald H. Richter, and Eduardo Soria-Escalante 

U.S. GEOLOGICAL SURVEY BULLETIN 2119 

Major oxide and trace element data for 

lavas and ash-flow tuffs of the Bolivian Altiplano 

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1995 
U.S. DEPARTMENT OF THE INTERIOR 

BRUCE BABBITT, Secretary 

U.S. GEOLOGICAL SURVEY 

Gordon P. Eaton, Director 

For sale by U.S. Geological Survey, Information Services 

Box 25286, Federal Center 

Denver, CO 80225 

Any use of trade, product, or firm names in this publication is for descriptive purposes only and 

does not imply endorsement by the U.S. Government 

Library of Congress Cataloging-in-Publication Data 

Compositional characteristics of middle to upper Tertiary volcanic rocks of the Bolivian 

Altiplano I by Edward A. du Bray ... [et al.]. 

p. em. -(U.S. Geological Survey bulletin ; 2119) 

Includes bibliographical references. 

Supt. of Docs. no.: B 19.3:2119 

1. Volcanic ash, tuff, etc.-Bolivia-Composition. 2. Geology, StratigraphicTertiary. I. du Bray, E. A. II. Series. 

QE75.B9 no. 2119 

[QE461] 

557.3 s-dc20 95-3059 

[552'.2'0984] CIP 
CONTENTS 

Abstract. ......................................................................................................................... . 

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

Petrography..................................................................................................................... 4 

Geochemistry.................................................................................................................. 4 

Analytical Methods................................................................................................. 4 

Unaltered Rocks ...... .. . ...... .. . . ... .. . . . .. . .. . . . . ... .. . . . . .. ... . . .. ...... ... . . ... ... . . .... .. . . .. .. ... . .... ........ 4 

Altered Rocks......................................................................................................... 18 

Discussion and Conclusions .. .. .... ... . . .......... .. ... . . . . . . ... .. . . . . ....... .. .. . .. . . . .. .......... ........ ........ ... 20 

Unaltered Rocks..................................................................................................... 20 

Altered Rocks . . ... ... . . ... .. .. . . ..... .. .... .. .. . . ............ .. . . . . . . ... . .. . . . ... ... . .... ....... .. ... . .. . . ... . .. .. . . .. 21 

References Cited............................................................................................................. 21 

Appendixes-Brief Descriptions of Samples................................................................. 23 

FIGURES 

1. Maps showing volcanic features and sample locations, Altiplano and Cordillera...................................................... 2 

2. Total alkali-silica variation diagram showing analyses of volcanic rock samples..................................................... 5 

3. Histogram of Si02 contents......................................................................................................................................... 16 

4. Variation diagrams showing abundances of major oxides.......................................................................................... 17 

5. Variation diagram showing rubidium and strontium abundances............................................................................... 18 

6. Histogram of rubidium-strontium ratios...................................................................................................................... 18 

7. Ternary variation diagram showing the relative proportions of rubidium, potassium, and strontium........................ 19 

8. Trace element-tectonic setting discrimination variation diagrams............................................................................. 19 

9. Ternary AFM variation diagram . . ......... ... ... . . . .. .. . . . ... .... . . . .. . ... .. . . . ... ... . . ......... .. . ...... .. . . ... .. . . . . . . . .. . . ......... .. . . ... .. . . . . .. . .. . . . . .. .. 20 

TABLES 

1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano........................................ 6 

2. Chemical compositions of altered volcanic rock samples from the Bolivian Altiplano............................................ 14 

III 

Compositional Characteristics of Middle to Upper Tertiary 

Volcanic Rocks of the Bolivian Altiplano 

By Edward A. du Bray, Steve Ludington, William E. Brooks, Bruce M. Gamble, 

James C. Ratte, Donald H. Richter, and Eduardo Soria-Escalante 

ABSTRACT 

Middle to upper Tertiary lava flows, hypabyssal flow 

domes, and ash-flow tuffs of the Bolivian Altiplano, including those genetically associated with polymetallic vein 

deposits, are composed dominantly of metaluminous dacite. 

Major oxide and trace element compositions of these rocks, 

which contain variable combinations and abundances of plagioclase, biotite, hornblende, clinopyroxene, quartz, and 

potassium feldspar, are similar to those of continental margin, volcanic arc rocks throughout the world. Abundances of 

Al203, total iron, MgO, CaO, and Ti02 decrease with 

increasing Si02, whereas K20 abundances increase with 

increasing Si02. Compositional variation trends defined by 

these rocks primarily reflect crustal contamination of primitive, asthenospheric, mantle-derived partial melts that have 

undergone subsequent evolution involving varying amounts 

of crystal fractionation. Alumina saturation indices of the 

Altiplano volcanic rocks average 0.958, a value that precludes any significant involvement of sedimentary rock in 

the crustal assimilation assemblage. These observations are 

consistent with the genesis of these I-type rocks in the archetypal continental volcanic arc. 

Samples of volcanic rock genetically related to polymetallic vein deposits have distinctive compositions that reflect 

hydrothermal alteration. Most of the altered Altiplano volcanic rocks have low Na20 and CaO contents and high K20 

and loss on ignition (LOI) contents, all of which reflect sericitic alteration. A smaller number of altered samples, which 

also contain secondary quartz, have high Si02 abundances, 

which reflect silicification. 

INTRODUCTION 

The U.S. Geological Survey and the Servicio Geologico 

de Bolivia ( 1992) conducted a mineral resource assessment of 

the Altiplano and Cordillera Occidental in southwestern 

Bolivia during 1990-91. During fieldwork for the assessment, 

field parties visited many Cenozoic volcanic centers (fig. 1 ), 

particularly those with associated mineral deposits, and the 

volcanic rocks were sampled. Geochemical and petrographic 

data were obtained to aid in the characterization of these rocks 

and in the interpretation of the geologic setting of the associated mineral deposits. Data and interpretations presented here 

are byproducts of the mineral resource assessment. 

Mesozoic and Cenozoic igneous rocks of the Andes in 

western South America have long been recognized as the 

products of archetypal continental margin, subduction-related volcanic arc magmatism (Mitchell and Reading, 

1969; Dewey and Bird, 1970). Volcanoes in the western part 

of the South American arc have been more extensively studied (see, for example, Harmon and Rapela, 1991) than those 

of the Altiplano, primarily because they are the locus of 

ongoing igneous activity within the arc. 

A detailed review of central Andean geology is beyond 

the scope of this study and would be redundant in light of 

already published reports. Richter and others (1992) provided a synopsis of southwestern Bolivian geology, and references cited therein present current concepts concerning the 

geologic evolution of the Altiplano. One of the world's 

archetypal continental volcanic arcs, the Andean arc, whose 

origin is related to subduction of the Nazca plate beneath the 

western edge of the South American continental plate, trends 

northerly through southwestern Bolivia. The Andean arc has 

been divided into northern, central, and southern volcanic 

zones (Thorpe and others, 1982); the area of the Bolivian 

Cordillera Occidental (the western of the two Andean mountain chains extending through the length of Bolivia) and Altiplano is within the central volcanic zone (see Richter and 

others, 1992, fig. 2). In Bolivia, the central volcanic zone is 

composed of western and eastern limbs separated by the 

Altiplano; the two limbs merge to a single arc in southernmost Bolivia. Igneous centers, principally ash-flow calderas 

and lava flow and dome complexes of intermediate composition, along the east edge of the Altiplano segment of the 

central volcanic zone were active during the Oligocene and 
2 

21 • 

22• 

0 

• 

DR006 + 

0 

I 

TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

• 

rl'' .~ •• 008 

+ 08010 \ + 08004 

OBOOQ DBo~J> ~~~0 1 + 08003 

•• 08006 

SL054 + 

+ R036G + ROl7 

0 

o- 61ca it~B~\ R010 

-flo ~..t 

..,o )r + R022 

+ 11; + 8G001A 

""'+ 8G013C 

., 

0 

0 Uyuni 

EXPLANATION 0 

01 igocene-Miocene ~ 

volcanic center 

DR035 + SL057 + e + SL060 

Intrusive center 

Sample site and 

number 

0 

20 40 60 80 100 KILOMETERS 

I I I I I I I I I 

+ DR012 • 

ODR037 

+ DR038 

+ DR034 0 

~16 

o~~~:v 

DR015 ++ DR043 

+ DR039 

OR041-41A 

+ + OR042 

DR054-5 'II- DR053 

0.:-. • ~'00~ 

e +~ SL073 DR057 (."'\<!? 

SL074 SL102\!...:II Bot rv sL~79 r:;-J) +sL 104-7 __ --I A 

\.:._)"--./ + PNZO&-~ ' ,Jd"_.,J RGENTINA 

I 

0 r-r' 

I 

/ 

A.RGEJVT 

A CHILEI 1NA. 

23• ~------------~--------------L-------------~~--------------~--------~ 

Figure 1 (above and facing page). Maps showing middle to upper Tertiary volcanic features and sample locations, Altiplano and Cordillera Occidental, Bolivia. All sample numbers are prefixed by 90B. Modified from 

Richter and others (1992). A, Unaltered volcanic rocks. B, Altered volcanic rocks. 
17. 

18" 

20" 

21 • 

22. 

69. 

PERU 

Lago 

Titicac~ ,. 

I (I • ,t~soos • 

+;:a., 

' .ro,C!' 

0 

• 

DR025 + 

BG024 + BG0228 

..., 

0 

0 

EXPLANATION 

01 igocene-Miocene ~ 

volcanic center 

Intrusive center 

Sample site and 

number 

• 

0 

INTRODUCTION 

68. 67" 66" 

LA PAZ 

• 

<1(0 Oo. 

SLOdJ+ •"' ~R001A 

00 Oruro ~ e SL010 

0 

0 DRO~S1C + e SL090+ 

• 

SL103Q. BOLzv SL083c:JO! PN 10 ----lA r-0! _..,~ :4RaeNr r N;- 0 

0 ... r 

I 

I ' 

0 

I 20 40 60 80 1 00 K I Lot.tETERS r 

Al?GElV'f 

CHILEI /}VA 

I I I I I I I I I 

B 

23•L_ __________ _L ______________ L_ __________ ~,~--------------~------~ 

3 
4 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Miocene. Igneous centers, principally stratovolcanoes, in the 

Cordillera Occidental became active during the Miocene and 

are the locus of ongoing arc magmatism. Exceptionally thick 

(as much as 70 km) continental crust (James, 1971) beneath 

both limbs of the central volcanic zone in Bolivia developed 

during Oligocene and Miocene time by thin-skinned tectonic 

processes (Sempere and others, 1990). The Altiplano region 

is considered to represent a series of contiguous, intermontane foreland basins; sediment deposited in these basins was 

shed from fold and thrust belt uplifts that developed in 

response to crustal shortening and thickening (Richter and 

others, 1992). 

Middle to upper Tertiary volcanic rocks on the Altiplano 

that are associated with the majority of the Bolivian polymetallic vein deposits have been relatively little studied. Kussmaul and others ( 1977) provided an excellent description of 

the geologic framework of southwestern Bolivia. They presented major oxide and trace element data for 26 samples of 

volcanic rocks that they combined with analyses from 

Fernandez and others (1973) to infer five major cycles of 

magmatic activity during which magmas formed by partial 

melting at different crustal levels were erupted as lavas and 

ash-flow tuffs. Baker and Francis ( 1978) showed that the ages 

of major eruptive centers are highly variable in different parts 

of the central volcanic zone. Davidson and others (1991), de 

Silva (1991), and Davidson and de Silva (1992) offered modern interpretations of the plate tectonic and magmatic processes that have influenced the petrogenesis of volcanic rocks 

of the central volcanic zone. 

Acknowledgments.-The mineral resource assessment 

of the Bolivian Altiplano (U.S. Geological Survey and Servicio Geologico de Bolivia, 1992), of which this report is an 

outgrowth, was carried out with the able assistance of many 

people. The acknowledgments section in the assessment 

report is equally applicable to this one. We would also like 

to thank G.B. Sidder and D.J. Bove for their thoughtful and 

helpful reviews. 

PETROGRAPHY 

Most middle to upper Tertiary volcanic rocks of the 

Altiplano are petrographically similar. They are chiefly porphyritic dacite that contains variable proportions of plagioclase, biotite, hornblende, pyroxene, quartz, and potassium 

feldspar phenocrysts in a very fine grained groundmass that 

befits its hypabyssal to extrusive nature. Combinations of 

opaque oxide minerals, apatite, titanite, and zircon are 

present as accessory minerals. Ash-flow tuffs have 

well-developed vitroclastic textures, display various degrees 

of welding, are moderately pumiceous, and have variably 

devitrified glassy groundmass textures. 

Some Altiplano volcanic rocks studied exhibit varying 

degrees of propylitic or sericitic alteration. Feldspars, 

plagioclase in particular, in most of the intensely 

hydrothermally altered Altiplano volcanic rocks have been 

replaced by fine-grained intergrowths of white mica. Six 

samples of altered volcanic rocks that have anomalously 

high Si02 contents contain secondary silica. 

GEOCHEMISTRY 

Geochemical analyses were obtained for 105 igneous 

rock samples. Of these samples, 82 are considered to represent unaltered igneous compositions. They include 53 lava 

flows (including hypabyssal intrusions and flow domes), 24 

ash-flow tuffs, 2 plutonic rocks, 2 dikes, and 1 mafic 

enclave (table 1). 

The compositions of the remaining 23 samples (table 2) 

reflect various types and intensities of gydrothermal alteration. These rocks were altered by cogenetic hydrothermal 

fluids that are responsible for genesis of associated mineral 

deposits. Some of these samples were collected to determine 

the mobility of certain oxides and elements during hydrothermal alteration and to determine whether particular oxide 

or element abundances experienced relative gains or losses. 

Some weak alteration, not recognized at the time of sample 

collection, became apparent during data analysis; compositions atypical of common igneous rocks were identified as 

suspicious. Hand specimen or microscopic examination subsequently confirmed the altered nature of these samples. 

ANALYTICAL METHODS 

All of the geochemical data presented here were determined in analytical laboratories of the U.S. Geological Survey in Denver, Colorado. Major oxide analyses were 

performed (analysts, J.E. Taggart and D.F. Siems) using 

X-ray fluorescence techniques (Taggart and others, 1987); 

FeO, C02, F, and Cl were determined by wet chemistry (analysts, C.S. Papp, T.R. Peacock, J.D. Sharkey, and K.J. Curry) 

(Jackson and others, 1987). Fe2+ to total iron as Fe2+ ratios 

were adjusted to 0.80 and major oxide abundances recalculated to 100 percent, on an anhydrous basis. Trace element 

abundances were determined (by E.A. du Bray) by 

energy-dispersive X-ray fluorescence spectroscopy (Elsass 

and du Bray, 1982) using 109Cd and241Am radioisotope 

excitation sources; the accuracy of this type of data is discussed by Sawyer and Sargent (1989). 

UNALTERED ROCKS 

Middle to upper Tertiary Altiplano volcanic rocks 

were classified following the system of the International 

Union of Geological Sciences (Le Bas and others, 1986); 

however, the alkaline-subalkaline subdivision of Irvine and 

Baragar ( 1971) was used to classify the alkalinity of these 
GEOCHEMISTRY 5 

A ASH-FLOW TUFF 

+ LAVA 

1- 10 z 

w 

() 

a:: 

w 

a.. 

1-

I 

(.!) 

w 

3: 

z 

. 

0 

C\1 

~ 

+ 0 

C\1 

0 5 - z 

/ / / / 1-----v 

// 

/ / 

+ 

/ 

// 

TRACHYTE 

+ 

ANDESITE 

RHYOLITE 

·· ... + & 

·· ............. + 

+ &+ \& + 

··.+ 

.· 

DACITE 

BASALT 

BASALTIC 

ANDESITE 

0 

43 55 67 

Si02, IN WEIGHT PERCENT 

Figure 2. Total alkali-silica variation diagram with lUGS classification grid (Le Bas and others, 1986) showing analyses of 

volcanic rock samples from the Bolivian Altiplano. Alkaline-subalkaline division is that of Irvine and Baragar (1971). Dotted line 

outlines the area in which data for the 59 samples of Altiplano volcanic rock of Fernandez and others (1973) and Kussmaul and 

others ( 1977) plot. 

rocks. All but one of these rocks are subalkaline, and most 

cluster in the dacite and trachyte-trachydacite fields (fig. 2); 

andesitic-trachyandesitic and rhyolitic compositions are 

each represented by about 10 samples, one sample is 

composed of basaltic andesite, and one sample is composed 

of basalt. 

Geochemical variation among the middle to upper Tertiary volcanic rocks of the Altiplano is similar to that of most 

continental volcanic arc calc-alkaline igneous rocks (table 

1). Si02 contents of the analyzed samples display a 

well-defined mode at about 65 weight percent (fig. 3). 

Al203, FeO*(total iron expressed as FeO), MgO, CaO, and 

Ti02 abundances decrease with increasing Si02, whereas 

K20 abundances increase with increasing Si02; Na20, 

MnO, and P20 5 abundances display no consistent relationship to Si02 abundances (fig. 4 ). K20 abundances in most 

of these samples plot in the high-potassium-calc-alkaline 

series of Ewart (1982), and Na20 to K20 ratios are approximately normally distributed about an average of 0.88 at an 

average Si02 content of about 65 weight percent. 

Compositions of the analyzed samples are metaluminous to weakly peraluminous. The alumina saturation index 

(ASI), the molar ratio of Al203/(CaO+K20+Na20), for the 

average of the 82 unaltered samples is 0.958. This value is a 
6 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano. 

[Sample numbers prefixed by 90B. Major oxide data (weight percent) normalized to 100 percent, volatile free. FeO/FeO*(total iron as FeO) 

recalculated to 0.80. FeOa, ferrous iron content by wet chemistry. H20+, chemically bound water; HzO-, adsorbed water. Trace element data in parts 

per million. Sumi. prenormalization total with total iron as Fe20 3• LOI, loss on ignition. bdl, below detection limit] 

Sample DROOlB DR005 DR006 DR012 DR015 DR016 DR034 DR035 DR037 DR038 DR039 

Lava Lava Tuff Tuff Tuff Tuff Tuff Lava Lava Lava Lava 

Lat 0S. 17.7828 19.3314 19.5678 21.3541 22.2985 22.1678 21.4433 21.2317 21.4950 21.6669 22.4300 

Long 0W 67.4290 66.8404 66.8446 67.6469 67.7679 67.5866 67.4633 67.6900 67.8633 67.9077 67.8800 

Si02 65.31 63.64 65.98 64.96 61.44 64.49 66.06 63.89 61.20 63.91 62.96 

Al203 15.68 16.60 17.11 16.63 18.05 16.40 16.90 17.83 17.23 16.67 16.30 

Fe203 1.00 0.93 0.72 1.03 1.20 1.06 0.96 0.99 1.17 1.10 1.18 

FeO 3.61 3.34 2.58 3.71 4.33 3.83 3.45 3.55 4.19 3.96 4.25 

MgO 2.23 2.29 1.35 1.18 2.84 2.28 1.00 1.68 2.97 2.63 2.82 

CaO 3.44 4.73 3.51 4.98 5.68 4.93 4.10 4.11 5.43 4.16 5.16 

Na20 3.27 2.71 2.56 3.22 2.97 2.78 2.99 3.67 3.25 3.22 2.42 

K20 4.23 4.21 4.79 3.19 2.42 3.20 3.57 3.24 3.28 3.25 3.77 

Ti02 0.86 1.10 0.86 0.75 0.83 0.78 0.73 0.66 0.94 0.85 0.87 

P20s 0.30 0.39 0.52 0.29 0.13 0.17 0.19 0.31 0.26 0.17 0.18 

MnO 0.06 0.06 0.04 0.06 0.08 0.07 0.07 0.08 0.07 0.07 0.07 

LOI 2.90 1.45 2.41 1.74 1.53 0.37 2.08 1.70 1.10 1.17 1.51 

Sumi 99.59 99.39 99.69 99.58 99.49 99.57 99.88 99.13 100.25 99.39 99.49 

FeOa 0.37 2.90 1.53 0.10 2.84 2.36 0.04 1.71 3.77 0.82 2.69 

H20+ 2.17 1.02 1.77 1.12 1.30 0.32 0.70 1.37 0.88 0.76 1.44 

H20- 0.39 0.34 0.41 0.48 0.39 0.14 1.24 0.49 0.32 0.42 0.26 

C02 bdl bdl 0.01 0.02 bdl bdl bdl bdl bdl bdl bdl 

CL 0.18 0.04 0.04 0.02 0.02 0.02 0.01 0.05 0.04 bdl 0.03 

F 0.04 0.04 0.06 0.03 0.01 0.02 0.02 0.02 0.03 0.02 0.02 

Rb 127 148 294 129 101 151 142 86 114 136 142 

Sr 509 514 456 348 406 310 307 729 531 406 384 

y 10 18 17 13 24 29 23 30 17 11 22 

Zr 205 268 190 130 153 160 121 210 183 154 158 

Nb 13 18 21 11 10 12 9 21 13 13 12 

Pb 24 11 44 43 28 bdl 101 bdl 16 34 - 7 

Th 19 17 bdl bdl 16 12 bdl bdl bdl 12 21 

Ba 1,179 1,400 1,015 724 609 588 606 1,303 817 801 607 

La 55 66 68 34 26 39 31 48 46 13 31 

Ce 111 142 66 59 77 71 71 97 76 70 68 

Nd 46 58 65 31 34 33 23 45 32 16 24 
GEOCHEMISTRY 7 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample DR041 DR041A DR042 DR043 DR044 DR046 DROS3 DROS4 DROSS DROS7 DR060B 

Lava Lava Tuff Lava Tuff Tuff Lava Lava Lava Lava Lava 

Lat os 22.6217 22.6217 22.6450 22.3233 22.2217 22.1717 21.5650 21.5600 21.5600 21.7800 21.8100 

Long 0

W 67.7300 67.7300 67.6633 67.7367 67.7200 67.6900 66.8550 66.8667 66.8667 66.5600 66.4983 

Si02 65.30 62.16 65.79 63.69 65.70 63.64 63.46 52.61 76.20 66.42 65.62 

Ah03 16.33 16.79 16.22 16.87 15.74 16.59 16.66 18.22 13.45 15.94 16.40 

Fe20 3 0.97 1.31 0.95 1.02 0.98 1.15 1.21 1.94 0.14 0.86 1.00 

FeO 3.48 4.70 3.44 3.67 3.53 4.14 4.35 6.98 0.51 3.10 3.59 

MgO 2.21 2.98 1.81 2.44 2.09 2.50 2.22 3.54 0.19 1.58 2.79 

CaO 4.56 5.30 4.51 5.27 4.56 4.93 4.81 10.10 1.11 4.56 3.34 

Na20 3.06 2.77 3.20 2.91 2.75 2.82 3.20 2.88 3.31 2.15 2.50 

K20 3.15 2.69 3.19 3.13 3.63 3.12 2.96 1.82 4.89 4.38 3.59 

Ti02 0.69 0.96 0.66 0.74 0.76 0.84 0.76 1.42 0.06 0.70 0.75 

P20s 0.18 0.24 0.15 0.18 0.18 0.19 0.25 0.34 0.07 0.28 0.29 

MnO 0.07 0.09 0.06 0.07 0.07 0.08 0.11 0.15 0.06 0.03 0.12 

WI 1.94 1.74 0.42 1.34 0.31 0.35 1.76 1.41 0.40 4.56 2.46 

Sumi 99.71 99.90 100.06 99.56 99.17 99.64 99.46 99.87 98.62 98.98 99.16 

FeOa 2.83 3.56 1.91 3.19 2.56 2.11 1.88 3.78 0.27 1.51 0.21 

H20+ 1.71 1.57 0.45 1.25 0.18 0.35 1.68 0.37 0.19 1.69 1.63 

H20- 0.33 0.43 0.14 0.23 0.16 0.11 0.37 0.23 0.20 1.17 1.03 

C02 bdl bdl bdl bdl 0.14 bdl 0.04 1.28 0.04 2.14 0.25 

CL 0.03 0.02 0.02 0.02 0.04 0.02 0.05 0.01 bdl 0.03 0.04 

F 0.02 0.02 0.01 0.02 0.01 0.02 0.02 0.03 bdl 0.02 0.03 

Rb 130 108 142 121 158 145 117 55 201 168 220 

Sr 321 351 318 365 271 315 477 473 132 304 534 

y 22 30 17 29 24 30 23 32 32 24 23 

Zr 133 194 127 159 162 174 156 154 65 149 171 

Nb 7 6 11 10 16 7 22 14 41 20 24 

Pb bdl 29 22 41 48 24 27 bdl 7 27 132 

Th bdl 18 bdl 19 40 16 bdl bdl bdl 21 23 

Ba 597 585 508 678 630 588 767 385 410 813 936 

La 25 26 27 25 30 35 30 23 11 49 53 

Ce 72 78 62 79 79 77 62 51 27 95 79 

Nd 28 26 13 26 25 35 19 23 6 33 27 
8 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample BGOOlA 80003 80004 B0013C 80059 R008 ROlO R019 R020 R022 R031 

Pluton Lava Lava Lava Dike Lava Tuff Lava Lava Tuff Tuff 

Lat 0S 19.0680 19.0105 19.0105 19.1364 19.6781 18.8318 18.8548 19.0185 19.0156 18.9898 18.7893 

Long 0W 68.5158 68.7248 68.7248 68.6379 67.7099 68.6181 68.6103 68.8162 68.8186 68.6367 68.8066 

Si02 70.84 75.94 76.96 62.87 61.27 59.51 72.40 60.32 66.14 75.21 75.85 

Al203 14.60 13.64 13.61 17.22 17.36 18.43 14.75 16.40 16.28 13.52 13.52 

Fe203 0.71 0.16 0.08 1.04 1.14 1.44 0.44 1.28 0.79 0.25 0.26 

FeO 2.54 0.59 0.29 3.74 4;10 5.17 1.57 4.61 2.85 0.91 0.93 

MgO 0.62 0.26 0.17 1.87 2.25 0.95 0.92 2.88 1.47 0,25 0.62 

CaO 1.21 1.91 0.74 4.80 4.19 6.53 1.24 5.13 3.36 0.97 0.68 

Na20 3.88 2.13 3.30 3.76 4.48 4.16 2.04 4.32 4.40 3.68 2.66 

K20 4.88 5.22 4.74 3.27 3.79 2.54 6.25 3.20 3.67 5.03 5.27 

Ti02 0.52 0.15 0.11 0.96 0.90 0.81 0.31 1.18 0.70 0.18 0.18 

P20s 0.12 bdl bdl 0.41 0.40 0.39 bdl 0.58 0.28 bdl bdl 

MnO 0.07 bdl bdl 0.05 0.11 0.07 0.08 0.09 0.07 bdl 0.03 

LOI 0.75 5.89 0.90 3.30 1.94 1.67 3.30 0.14 1.90 0.38 2.14 

Sumi 98.99 99.05 98.65 98.33 99.17 99.35 99.05 99.45 99.28 98.87 99.14 

FeOa 0.01 0.14 0.07 1.50 2.36 1.07 bd1 2.35 1.59 0.12 0.08 

H20+ 0.71 2.44 0.72 1.76 1.86 0.51 1.26 0.14 1.82 0.36 0.93 

H20- bdl 3.19 0.23 1.07 0.08 0.18 1.55 0.16 0.18 bdl 1.23 

C02 bdl bdl bdl bdl 0.30 1.08 bdl bdl bdl 0.03 bdl 

CL bdl 0.01 bdl 0.06 0.01 0.01 0.30 0.03 0.10 bdl bdl 

F 0.03 0.01 0.02 0.03 0.03 0.03 0.02 0.03 0.02 bdl 0.03 

Rb 167 146 162 96 92 41 155 63 109 106 181 

Sr 123 235 98 759 644 712 176 1209 717 176 71 

y 33 21 10 30 31 16 19 19 15 9 40 

Zr 259 84 88 227 298 213 205 250 208 105 147 

Nb 6 9 12 14 25 18 17 17 14 14 12 

Pb 47 9 23 22 47 22 7 25 45 31 19 

Th bdl 12 22 bdl bdl bdl bdl bdl bdl 9 22 

Ba 1,021 1,11g 1,160 1,141 1,278 1,069 1,262 1,467 1,422 575 648 

La 36 38 40 48 58 31 35 68 43 39 41 

Ce 71 75 64 99 100 66 66 126 105 96 79 

Nd 29 8 15 59 29 40 20 37 45 16 20 
GEOCHEMISTRY 9 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample R036G R037 R041 R044 R044A PNZOl PNZ03 PNZ05 PNZ06 PNZ07 SL004 

Lava Tuff Lava Lava Lava Tuff Tuff Tuff Tuff Tuff Lava 

Lat os 18.2497 18.2753 19.6252 19.6200 19.6200 unk unk unk 21.9919 21.9919 17.7687 

Long 0

W 68.5370 68.2868 67.7074 67.7019 67.7019 unk unk unk 66.4735 66.4735 67.5047 

Si02 64.94 71.18 47.78 66.33 67.50 65.14 65.52 65.48 66.10 64.87 67.36 

Al203 17.60 14.52 14.41 15.86 15.80 16.46 16.22 16.14 16.01 17.29 15.40 

Fe20 3 0.80 0.57 2.94 0.91 0.87 1.06 1.13 1.13 1.16 0.96 0.84 

FeO 2.89 2.05 10.59 3.28 3.12 3.80 4.07 4.05 4.16 3.47 3.04 

MgO 0.93 1.10 7.22 1.51 1.72 1.97 2.04 2.04 1.89 1.76 2.18 

CaO 2.97 2.04 11.61 2.64 2.31 4.04 4.08 4.22 3.64 4.24 1.78 

Na20 4.31 3.89 2.57 4.30 3.70 2.01 1.77 1.80 1.77 2.08 4.54 

K20 4.13 3.92 0.12 3.80 3.72 4.12 3.83 3.82 3.92 4.07 3.87 

Ti02 1.06 0.51 2.27 0.86 0.82 1.02 1.00 0.99 1.03 0.90 0.69 

P20s 0.37 0.18 0.25 0.46 0.43 0.32 0.28 0.28 0.27 0.31 0.26 

MnO bdl 0.05 0.23 0.04 0.03 0.06 0.06 0.05 0.06 0.05 0.04 

LOI 1.22 0.82 0.71 1.96 3.64 0.90 2.65 2.62 3.22 1.35 2.10 

Sumi 98.70 98.83 98.33 98.80 98.93 99.72 99.86 99.72 99.88 99.46 97.88 

FeOa 0.56 0.06 1.17 0.47 0.34 3.17 2.30 2.37 1.96 2.85 1.20 

H20+ 0.96 0.68 0.55 0.72 1.21 0.52 0.98 0.93 1.14 1.21 1.85 

H20- 0.29 0.10 0.27 1.45 2.38 0.35 1.33 1.28 1.57 0.26 0.29 

C02 bdl bdl bdl bdl bdl bdl bdl bdl bdl bdl 0.86 

CL 0.02 0.02 0.02 bdl bdl 0.03 0.03 0.03 0.03 0.05 0.03 

F 0.05 0.02 0.03 0.03 0.03 0.03 0.02 0.02 0.02 0.02 0.04 

Rb 115 83 76 90 89 168 137 145 153 166 102 

Sr 1,076 593 1,345 1,101 973 326 307 309 284 342 275 

y 25 7 16 11 10 29 22 18 26 25 19 

Zr 364 120 229 186 194 233 174 179 191 196 162 

Nb 25 16 25 20 21 13 19 13 10 15 12 

Pb 24 bdl 11 7 bdl 34 14 26 22 26 14 

Th bdl bdl bdl bdl bdl 13 9 bdl 15 bdl 10 

Ba 1,744 1,201 1,185 1,183 1,191 855 739 743 780 748 1,285 

La 77 31 55 63 55 58 45 41 28 46 31 

Ce 137 81 111 94 85 111 81 89 89 95 90 

Nd 71 33 57 37 36 53 33 36 35 38 25 
10 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano--Continued. 

Sample SL034 SL040 SL046 SL047 SL048 SLOSO SL051 SL054 SL057 SL060 SL067 

Enclave Lava Lava Lava Lava Lava Tuff Lava Pluton Dike Lava 

Lat 0

S 17.7568 17.7888 17.7577 17.7588 17.7549 17.7645 17.7889 17.3788 21.2240 21.2707 21.7536 

Long ow 67.4632 67.4539 67.4623 67.5069 67.5090 67.6300 67.6106 67.7776 67.2317 67.2589 67.2218 

SiOz 61.38 63.74 65.89 64.37 65.53 71.97 70.17 65.86 61.77 64.80 69.39 

Al203 16.53 15.31 16.00 15.02 15.35 16.13 14.67 15.17 16.95 17.39 15.61 

Fe203 1.19 1.07 0.89 1.07 0.97 0.25 0.58 0.88 1.23 0.77 0.55 

FeO 4.27 3.85 3.21 3.86 3.51 0.92 2.10 3.18 4.44 2.76 1.99 

MgO 2.51 2.70 1.53 2.78 2.73 0.42 1.25 2.28 2.04 0.47 1.08 

CaO 6.05 3.92 4.60 2.79 2.86 1.81 2.58 4.00 2.69 6.06 3.17 

Na20 3.66 3.77 3.44 3.79 3.80 3.90 3.82 3.17 7.17 3.26 2.51 

K20 3.19 4.35 3.50 4.95 4.05 3.95 4.11 4.32 2.42 3.51 4.74 

TiOz 0.84 0.80 0.65 0.80 0.71 0.53 0.45 0.76 0.77 0.61 0.71 

PzOs 0.25 0.36 0.21 0.28 0.26 0.12 0.20 0.30 0.43 0.32 0.23 

MnO 0.12 0.13 0.06 0.29 0.22 bdl 0.05 0.07 0.10 0.05 bdl 

LOI 4.19 3.39 3.56 2.85 1.71 2.16 1.80 4.55 1.01 2.31 1.14 

Sumi 99.62 99.18 99.51 99.11 99.14 98.97 98.79 99.17 99.44 99.21 99.35 

FeOa 3.09 2.12 1.43 1.93 2.12 0.08 0.43 2.12 2.17 1.09 1.75 

HzO+ 1.48 1.45 1.34 1.35 1.05 1.08 1.52 1.43 0.80 0.68 0.58 

HzO- 0.19 0.27 0.40 0.24 0.29 0.40 0.27 0.34 0.15 0.26 0.33 

C02 2.84 1.77 1.88 1.43 0.58 bdl 0.01 3.06 bdl 1.31 0.19 

CL 0.02 0.02 0.01 0.04 0.06 0.01 0.03 0.02 0.15 0.04 0.04 

F 0.02 0.04 0.02 0.03 0.02 0.06 0.02 0.03 0.03 0.02 0.02 

Rb 95 162 126 181 135 126 129 127 47 73 202 

Sr 531 528 398 254 599 535 495 451 310 531 272 

y 23 23 22 15 21 bdl 11 12 23 22 15 

Zr 130 203 145 161 157 172 159 183 268 205 185 

Nb 19 8 14 13 14 16 11 14 14 10 15 

Pb bdl 138 10 214 117 21 23 7 bdl 13 31 

Th bdl bdl 10 bdl bdl 15 12 bdl bdl bdl bdl 

Ba 1,062 1,725 1,212 1,400 1,513 1,017 1,056 1,215 1,127 1,111 781 

La 32 67 36 53 49 26 35 68 40 30 35 

Ce 76 122 81 88 89 71 64 111 96 82 84 

Nd 27 63 26 55 33 27 28 45 38 30 41 
GEOCHEMISTRY 11 

. Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample SL073 SL074 SL079 SL102 SL104 SL105 SL106 SL107 DBOOl DB003 DB004 

Lava Lava Tuff Lava Tuff Tuff Tuff Tuff Lava Lava Lava 

Lat 0 S 21.7622 21.8795 21.9504 21.8372 21.9034 21.9034 21,9033 21.9033 17.1963 17.1939 17.0297 

Long ow 67.1441 66.9410 66.7462 66.5638 66.4549 66.4542 66.4533 66.4524 67.7270 67.7180 67.8853 

Si02 58.64 63.08 66.89 67.69 68.67 65.09 64.35 64.82 66.61 65.83 64.85 

Al203 18.82 16.03 15.69 14.88 15.21 16.40 16.80 16.47 15.70 15.36 16.11 

Fe20 3 1.25 1.16 0.83 0.81 0.79 0.88 0.97 0.95 0.93 0.97 1.02 

FeO 4.50 4.18 2.97 2.92 2.85 3.15 3.51 3.41 3.34 3.51 3.68 

MgO 2.73 3.53 1.55 2.05 2.16 1.96 2.55 2.40 1.83 2.35 1.88 

CaO 8.03 4.81 5.67 3.61 4.34 3.83 4.78 4.08 2.77 3.74 3.61 

Na20 3.09 2.60 2.72 2.37 2.05 2.45 2.75 2.95 3.42 3.12 3.42 

K20 2.14 3.37 2.85 4.71 3.07 5.26 3.24 3.88 4.19 3.79 4.02 

Ti02 0.50 0.84 0.60 0.66 0.60 0.67 0.73 0.70 0.89 0.89 0.89 

P20s 0.23 0.28 0.19 0.27 0.24 0.28 0.30 0.29 0.30 0.30 0.47 

MnO 0.07 0.13 0.04 0.04 0.02 0.04 0.03 0.04 0.03 0.13 0.05 

LOI 3.00 2.25 4.18 2.01 5.68 1.33 4.44 3.61 2.04 3.28 1.41 

Sumi 99.66 99.41 99.43 99.09 99.32 99.23 99.45 99.31 99.23 99.35 99.27 

FeOa 2.82 2.86 0.98 1.82 0.86 0.13 0.25 0.98 0.36 3.44 1.49 

H20+ 0.67 1.50 1.32 0.93 2.43 0.53 2.09 1.81 0.71 1.96 0.56 

H20- 0.42 0.33 0.58 0.19 2.61 0.55 1.88 1.43 1.19 0.17 0.84 

C02 2.15 0.44 2.21 1.08 bdl 0.01 0.02 0.03 bdl 1.88 bdl 

CL 0.02 0.13 0.02 0.04 0.04 0.16 0.06 0.05 bdl bdl 0.03 

F 0.01 0.02 0.02 0.02 0.02 0.01 0.02 0.02 0.03 0.04 0.03 

Rb 77 124 119 209 140 194 146 167 159 126 141 

Sr· 758 499 392 405 651 530 689 636 505 488 643 

y 10 16 18 17 22 16 20 21 18 13 16 

Zr 79 136 137 170 125 146 158 159 221 225 225 

Nb 8 13 7 20 14 18 16 17 15 16 29 

Pb 11 30 29 318 25 5 12 23 21 6 bdl 

Th bdl 13 16 bdl bdl 20 20 16 13 bdl 12 

Ba 746 910 572 777 821 881 933 896 1,019 958 1,333 

La 11 38 34 50 52 50 50 63 51 33 65 

Ce 49 74 74 91 76 86 93 106 104 97 122 

Nd 12 28 34 32 41 28 32 33 34 24 67 
12 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample DB005 DB006 DB007 DB008 DB009 DBOlO DBOll DB012 DB013 ESOll ES012 

Lava Lava Lava Lava Lava Lava Lava Lava Lava Tuff Lava 

Lat os 17.1774 17.2272 17.1341 16.9689 17.1427 17.0245 16.9631 16.7677 16.7326 17.2512 17.2527 

Long ow 67.9806 67.9988 68.0668 68.2242 68.1526 68.4602 68.4193 68.2839 68.2450 69.5522 69.5614 

Si02 63.92 61.05 67.48 67.82 67.25 65.05 61.59 68.38 62.69 63.06 62.55 

Al203 16.01 16.21 16.20 15.00 16.20 18.03 17.79 15.39 15.05 16.69 17.34 

Fe203 1.06 1.36 0.93 0.75 0.91 0.99 1.14 0.68 1.30 1.14 1.00 

FeO 3.81 4.89 3.34 2.69 3.28 3.55 4.09 2.44 4.69 4.12 3.61 

MgO 2.25 2.68 1.38 0.76 1.13 0.66 1.54 1.35 2.79 1.57 2.24 

CaO 4.75 5.52 2.40 3.76 3.32 3.48 5.69 2.69 4.30 4.24 4.25 

Na20 3.18 3.26 3.08 3.53 3.54 2.73 4.14 4.08 3.49 4.25 4.29 

K20 3.79 3.44 3.94 4.54 3.29 4.77 2.79 4.09 3.93 3.62 3.49 

Ti02 0.75 1.00 0.62 0.76 0.60 0.48 0.68 0.65 1.20 0.90 0.84 

P20s 0.37 0.46 0.54 0.37 0.44 0.22 0.37 0.28 0.49 0.31 0.32 

MnO 0.11 0.12 0.09 0.02 0.04 0.04 0.18 bdl 0.06 0.10 0.06 

LOI 4.08 0.76 1.50 4.28 1.57 1.51 0.46 0.85 1.93 0.94 2.08 

Sumi 99.44 99.41 99.37 99.23 99.48 99.52 99.30 99.25 99.42 99.07 99.35 

FeOa 2.31 1.99 1.33 0.62 0.06 0.83 2.36 0.34 0.76 0.09 2.08 

H20+ 0.74 0.62 1.20 1.20 0.60 1.16 0.42 0.41 0.68 0.35 1.66 

H20- 0.68 0.34 0.36 0.46 0.49 0.23 bdl 0.22 0.88 0.19 0.51 

C02 2.83 bdl bdl 2.03 bdl bdl 0.03 bdl bdl bdl bdl 

CL 0.02 0.06 0.02 0.01 0.02 0.04 0.07 0.02 0.03 0.02 0.12 

F 0.03 0.02 0.02 0.07 0.02 0.03 0.02 0.02 0.03 0.03 0.02 

Rb 135 127 132 113 119 264 101 116 111 92 86 

Sr 671 711 457 929 621 800 916 799 928 1,089 1,256 

y 22 33 23 12 20 27 27 11 35 18 17 

Zr 194 213 155 241 209 264 206 172 234 183 174 

Nb 28 29 22 15 22 20 26 8 19 8 11 

Pb 23 17 16 25 40 bdl 5 34 11 bdl 17 

Th 16 18 bdl 9 13 bdl bdl bdl bdl bdl 12 

Ba 945 916 826 1,500 1,109 1,695 1,488 1,440 1,444 1,468 1,482 

La 45 53 42 87 43 41 43 50 60 57 68 

Ce 99 100 91 108 89 108 109 91 129 98 104 

Nd 44 42 37 46 29 44 44 28 44 28 62 
GEOCHEMISTRY 13 

Table 1. Chemical compositions of unaltered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample ES013 ES031 ES033 ES035 ES036 Lava Tuff Lava Tuff 

Lava Lava Lava Lava Lava average average average average 

Lat os 17.2546 17.1881 17.2675 17.2200 17.2683 n=53 n=24 F and K1 FandK1 

Long 0W 69.5594 69.5386 69.4058 69.4264 69.4181 

Si02 64.63 60.99 64.01 64.18 62.13 64.47±4.73 66.72±3.72 63.84±4.39 67.99±3.32 

Al203 16.18 17.16 16.43 15.99 16.75 16.17±1.15 16.05±1.18 16.27±0.63 15.83±1.41 

Fe203 0.89 1.26 1.04 1.03 1.17 1.01±0.42 0.88±0.28 1.15±0.36 0.77±0.18 

FeO 3.19 4.52 3.74 3.72 4.19 3.62±1.50 3.17±1.00 4.15±1.29 2.76±0.64 

MgO 1.95 2.36 1.95 2.11 2.18 2.06±1.09 1.71±0.65 2.58±1.87 1.41±0.49 

CaO 3.83 5.57 4.25 4.32 4.63 4.20±1.89 3.89±1.42 4.53±1.59 3.51±0.87 

Na20 4.42 3.83 3.93 3.79 4.00 3.40±0.63 2.74±0.68 2.84±0.61 2~91±0.52 

K20 3.81 2.89 3.56 3.75 3.61 3.67±0.86 3.86±0.92 3.44±1.12 3.92±0.55 

Ti02 0.76 1.00 0.73 0.70 0.87 0.80±0.32 0.70±0.24 0.91±0.27 0.67±0.19 

P20s 0.29 0.34 0.29 0.32 0.38 0.30±0.12 0.22±0.12 0.21±0.09 0.17±0.08 

MnO 0.05 0.08 0.07 0.08 0.09 0.08±0.06 0.06±0.03 0.08±0.04 0.06±0.03 

LOI 1.45 1.56 0.36 1.31 0.43 2.01±1.22 2.00±1.48 1.00±0.54 1.36±0.81 

Sumi 99.43 99.94 99.35 99.62 99.40 

FeOa 1.81 2.12 1.73 1.88 0.82 1.61±1.04 1.35±1.11 

H20+ 1.32 1.44 0.28 1.36 0.28 1.10±0.55 1.01±0.60 

H20- 0.17 0.40 0.34 0.33 0.28 0.51±0.55 0.75±0.71 

C02 bdl bdl bdl bdl bdl 0.47±0.84 0.10±0.45 

CL 0.13 0.07 0.02 0.07 0.01 0.04±0.04 0.05±0.06 

F 0.02 0.02 0.02 0.02 0.04 0.03±0.01 0.02±0.01 

Rb 88 76 99 111 78 125± 43 148± 41 

Sr 1,191 692 825 946 1,196 638±304 401±190 

y 8 9 23 17 16 19±8 21±8 

Zr 180 151 169 167 191 184± 50 161± 32 

Nb 13 12 8 12 11 16±7 14±4 

Pb 39 10 28 21 25 34± 55 26± 21 

Th bdl bdl bdl bdl bdl 6±8 10±0 

Ba 1,503 1,036 1,228 1,261 1,465 1117±334 811±248 

La 51 35 32 54 55 45± 16 41± 12 

Ce 95 55 77 97 117 91± 23 82± 15 

Nd 50 24 54 31 41 37± 15 33± 11 1

Femandez and others (1973), 20 lavas and 13 tuffs; and Kussmaul and others (1977), 18lavas and 8 tuffs. 
14 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Table 2. Chemical compositions of altered vofcanic rock samples from the Bolivian Altiplano. 

[Sample numbers prefixed by 90B. Major oxide analyses (weight percent) normalized to 100 percent, volatile free. FeO/FeO*(total iron as FeO) 

recalculated to 0.80. Trace element data in parts per million. Sumi, prenormalization total with total iron as Fe203. LOI, loss on ignition. bdl, below 

detection limit] 

Sample DROOl A DR008A DR008B DROlO DR025 DR030 DR031 DR058C DR061C BG022B BG024 

Lat os 17.8029 21.1167 21.1167 21.1100 20.9364 21.0929 21.1100 21.8100 21.6368 18.9387 18.9387 

Long ow 67.4485 67.2000 67.2000 67.2133 66.2913 67.2032 67.2133 66.4483 66.5147 68.6274 68.6274 

Si02 86.79 68.64 66.93 64.61 65.22 64.19 62.48 64.20 67.74 75.16 80.88 

Al20 3 8.36 16.62 16.13 15.86 16.23 18.35 19.04 15.46 16.21 13.13 12.03 

Fez03 0.25 0.41 0.89 1.40 0.95 0.60 0.88 2.21 0.54 0.28 0.07 

FeO 0.89 1.46 3.19 5.04 3.42 2.15 3.15 7.96 1.95 1.02 0.24 

MgO 0.37 0.65 0.61 0.92 1.85 0.48 0.54 1.08 0.51 bdl 0.10 

CaO 0.03 0.39 0.35 0.64 3.78 1.91 0.90 0.58 0.41 0.11 0.18 

Na20 bdl 2.05 1.54 1.09 2.78 2.66 1.07 0.34 0.74 1.20 1.66 

KzO 2.57 8.96 9.61 9.50 4.48 8.76 10.52 5.87 11.15 8.84 4.72 

TiOz 0.68 0.47 0.45 0.45 0.88 0.63 0.92 0.72 0.50 0.20 0.13 

Pz05 0.06 0.23 0.22 0.22 0.27 0.29 0.42 0.28 0.25 0.06 bdl 

MnO bdl 0.13 0.07 0.25 0.16 bdl 0.09 1.29 bdl bdl bdl 

LOI 2.75 1.89 1.79 2.83 4.33 1.10 3.77 5.07 1.69 1.46 1.71 

Sumi 99.40 99.52 98.20 98.55 98.98 98.86 99.18 99.04 98.74 98.30 98.18 

Rb 91 228 208 186 233 267 307 276 650 325 160 

Sr 22 72 200 233 223 632 111 39 110 95 48 

y 20 26 15 18 15 18 12 15 47 18 15 

Zr 164 193 190 193 175 181 232 160 137 177 107 

Nb 12 16 17 17 10 20 21 15 11 18 14 

Pb 85 56 178 346 24 28 253 70 45 2243 33 

Th bdl bdl bdl bdl bdl bdl bdl 11 30 bdl 13 

Ba 528 1,535 5,003 4,072 927 1,224 1,776 538 1,012 1,075 1,066 

La 29 26 31 30 51 

Ce 106 50 46 52 80 

Nd 12 47 48 44 22 

close approximation to the mean ASI (0.985) of 1,074 1-type 

granites from the Lachlan Fold Belt of Australia, which suggests that the Altiplano volcanic rocks were derived from an 

igneous (mantle) source (Chappell and White, 1992). 

Ferrous-ferric iron data for volcanic rocks are notorious 

for being unrepresentative of magmatic oxidation levels; 

late-stage volcanic processes including outgassing and devitrification cause many volcanic rocks to become significantly 

more oxidized than their associated magma. Use of this type 

of data in petrologic studies, including computation of normative mineralogy, can lead to erroneous conclusions (Middlemost, 1989). Review of ferrous and ferric iron data for 

middle to upper Tertiary volcanic rocks of the Altiplano 

indicates that these samples have also experienced varying 

amounts of posteruption oxidation (table 1). Values of 

FeO/FeO* for these samples are randomly distributed 

between 0 and 0.8 but converge on a maximum, unoxidized 

value between 0.75 and 0.80, which is similar to the iron oxidation value of 0.74 suggested by Middlemost (1989) for 

dacitic compositions. Consequently, FeO/FeO* values for 

31 61 56 29 39 48 

67 82 89 69 68 68 

40 53 31 54 30 11 

all of the samples described here have been adjusted to a 

value of 0.80 (table 1). 

Major oxide compositions of ash-flow tuffs and lavas of 

the Bolivian Altiplano display slight, but significant differences (table 1). The average composition of24 ash-flow tuff 

samples is more evolved than that of 54 lava flow samples. 

Relative to abundances in lava samples, abundances of Si02 

and K20 are high in ash-flow tuff samples and those of 

FeO*, MgO, CaO, Na20, Ti02, and P20s are low. Despite 

the differences between average compositions for the 

ash-flow tuffs and lava flows, their compositional data form 

colinear arrays or overlapping fields on variation diagrams 

(figs. 2, 4). 

Trace element abundances of the Altiplano ash-flow 

tuffs are also distinctly more evolved than those of the lava 

flows (table 1, fig. 4). Rubidium abundances in the 

ash-flow tuffs are slightly higher, relative to those of the 

lava flows, whereas abundances of strontium, zirconium, 

and barium are lower. As was the case for the major 

oxides, trace element abundances for the ash-flow tuffs and 
GEOCHEMISTRY 15 

Table 2. Chemical compositions of altered volcanic rock samples from the Bolivian Altiplano-Continued. 

Sample PNZlO SL002 SL003 SL005 SLOlO SL083 SL090 SL103 ES002 ES003 ES005 ES016 

Lat os 21.9919 17.8030 17.8004 17.7674 17.9538 21.9414 21.6706 21.8392 17.1214 17.1184 17.1158 17.2197 

Long oW 66.4735 67.4494 67.4496 67.5070 67.1192 66.7407 66.2923 66.5367 69.4333 69.4342 69 4303 69.4261 

Si02 70.58 78.55 89.52 71.93 70.35 65.62 

A}z03 15.44 12.10 6.69 13.26 15.22 16.35 

Fe203 0.56 1.05 0.18 1.65 2.15 0.96 

FeO 2.03 3.77 0.64 5.95 7.75 3.47 

MgO 1.36 0.37 0.27 0.90 0.55 0.89 

CaO 0.42 bdl 0.04 0.20 0.04 1.74 

NazO 0.18 bdl bdl 0.19 bdl 1.63 

K20 8.81 3.55 1.96 4.29 3.05 8.23 

Ti02 0.44 0.61 0.64 1.14 0.72 0.76 

PzOs 0.19 bdl 0.05 0.48 0.17 0.29 

MnO bdl bdl bdl bdl bdl 0.06 

LOI 2.67 4.71 3.89 8.59 7.19 1.61 

Sumi 99.38 99.31 98.91 98.16 98.66 99.21 

Rb 428 153 77 224 144 341 

Sr 25 17 20 1,173 111 343 

y 21 16 14 23 18 19 

Zr 125 153 174 231 146 160 

Nb 9 13 15 21 20 17 

Pb 22 26 11 111 46 102 

Th 11 11 bdl bdl bdl bdl 

Ba 1,376 292 225 1,267 534 949 

La 38 36 52 95 43 34 

Ce 58 79 76 176 65 63 

Nd 31 23 23 87 39 40 

lava flows form colinear and mostly overlapping fields on 

variation diagrams (figs. 5, 7, 8). 

Compositional data for unaltered Altiplano volcanic 

rocks are characterized by groups of oxides and elements 

whose abundances show mutual covariation. These covariant relations suggest that compositional variation was 

controlled by a distinct mineral assemblage, in accord with 

the fact that the compositions of Altiplano volcanic rocks 

form linear arrays on many variation diagrams. The minerals inferred to have influenced Altiplano volcanic rock 

compositional variation are present as phenocrysts therein. 

These minerals influenced compositional variation by their 

occurrence in the partial melting residuum or in crystal 

fractionation assemblages. 

The oxides whose abundances are most highly correlated are FeO*, CaO, MgO, Ti02, and MnO. Correlation 

coefficients (r 2) between FeO and CaO, MgO, and Ti02 are 

all greater than 0.85; within this group, mutual correlation 

coefficients exceed 0. 7. FeO* and MgO abundance variations are also correlated with those ofMnO; correlation coefficients values 1lre more than 0.6. Mutual abundance 

covariations involving these oxides indicate hornblende or 

67.27 64.67 66.12 67.88 68.06 73.20 

15.76 16.11 17.80 17.16 18.70 17.10 

0.73 1.04 1.62 0.99 L30 0.56 

2.63 3.76 5.83 3.57 4.69 2.01 

1.63 2.02 0.88 1.01 0.53 0.35 

1.30 6.15 0.31 1.58 0.13 0.11 

2.03 0.39 1.90 3.10 1.20 0.77 

7.72 4.75 4.24 3.60 3.93 4.80 

0.59 0.77 1.00 1.02 1.03 0.86 

0.23 0.29 0.29 0.10 0.43 0.24 

0.12 0.06 bdl bdl bdl bdl 

2.08 8.38 6.48 5.28 8.16 7.24 

99.44 99.37 99.19 98.91 99.00 99.25 

364 163 75 72 88 128 

197 133 634 755 797 873 

21 22 18 19 12 10 

157 150 207 205 216 173 

15 10 15 11 13 16 

28 34 40 24 40 31 

16 10 bdl bdl bdl bdl 

1747 648 1,608 1,616 1,485 1,342 

36 51 44 61 65 43 

57 99 95 103 116 79 

49· 25 46 44 67 43 

clinopyroxene as minerals influencing the compositional 

variation of the Altiplano volcanic rocks. The lack of a 

significant correlation between K20 abundances and those 

of this group of oxides indicates that biotite was not important in the geochemical evolution of the Altiplano volcanic 

rocks. 

Abundance variations of Si02 and K20 have a correlation coefficient of 0.78, whereas those of K20 and rubidium 

have an correlation coefficient of 0.60. These abundance 

covariations indicate potassium feldspar as another phase 

that influenced Altiplano volcanic rock compositional variation. Additional significant abundance covariations were 

not identified within the major oxides. 

Abundance covariations principally involving trace 

elements identify. three accessory minerals that may have 

influenced Altiplano volcanic rock compositional variation. 

Significant abundance covariations involving P205, Sr, La, 

Ce, and Nd; CaO and Ti02; and Zr, La, Ce, and Nd indicate 

apatite, titanite, and zircon, respectively, as additional 

phases that probably influenced compositional variation 

within the Altiplano volcanic rocks. 
16 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

1 5 (/) 

w 

_J 

0... 

L 

<( 

(/) 

l.J.... 1 0 

0 

et:: 

w 

m 

L 

::J 

z 5 

1-

1-

1-

0 j_ _Ll J 

50 

-

'::' -

.... P 

.·. 

-

r 

J U]b l.t;: 

>I k 

60 65 70 75 

IN WEIGHT PERCENT 

Figure 3. Histogram showing Si02 of volcanic rock samples 

from the Bolivian Altiplano. 

Compositions of Altiplano volcanic rocks can be compared to data of Macdonald and others (1992), which provides the best compendium of volcanic rock compositions 

versus tectonic setting relations. Their compilation is of 

obsidian compositions and thus is biased toward more 

evolved, rhyolitic compositions. Although their database is 

not entirely compatible with that for the majority of middle 

to upper Tertiary Altiplano volcanic rocks, the average composition of subduction-related obsidian from a continental 

margin setting (Macdonald and others, 1992) is grossly similar to that of the Altiplano volcanic rocks. 

The major oxide abundances of most of the Altiplano 

volcanic rocks are considerably less evolved than those of 

the average obsidian from continental margin, subduction-related settings (Macdonald and others, 1992). In particular, Si02 and total alkalis are lower in the Altiplano rocks, 

whereas abundances of Al203, FeO*, MgO, CaO, and Ti02 

are higher. The halogen contents of middle to upper Tertiary 

Altiplano volcanic rocks are slightly lower than those of the 

average obsidian from continental margin subduction-related settings (Macdonald and others, 1992). Fluorine 

contents in the Altiplano rocks are approximately normally 

distributed around a mean value of 0.03 weight percent, 

whereas the average fluorine content of subduction-related 

obsidian is about 0.05 weight percent. Chlorine contents in 

the Altiplano rocks are approximately normally distributed, 

though slightly skewed to higher abundances, around a mean 

value of 0.04 weight percent, whereas the average chlorine 

content of subduction-related obsidian is about 0.07 weight 

percent. Many of the major oxide and halogen abundance 

differences between the Altiplano rocks and the subduction-related obsidian of Macdonald and others (1992) may 

principally reflect the intrinsic bias toward rhyolitic, more 

evolved compositions characteristic of the latter. Trace element abundances (including Rb, Zr, Nb, Y, La, Ce, and Nd) 

in middle to upper Tertiary volcanic rocks of the Altiplano 

are similar to those of the average obsidian from continental 

margin subduction-related settings (Macdonald and others, 

1992) in many respects. The average abundances of barium 

and strontium, 1,027 and 558 ppm, respectively, in the Altiplano samples are considerably greater, however, than those 

in the continental margin, subduction-related rocks (730 and 

120 ppm, respectively) and may again relate to a sampling 

bias, toward rhyolitic compositions, in the latter. Barium and 

strontium abundances in the Altiplano rocks are also high 

relative to their abundances in granite (600 and 285 ppm, 

respectively) or the crust (425 and 375 ppm, respectively) 

(Krauskopf, 1967). 

The average zirconium abundance ofthe unaltered Altiplano samples is 180 ppm, similar to the value for obsidian 

from continental margin, subduction-related settings (Macdonald and others, 1992) and approximates the experimentally determined (Watson and Harrison, 1983) zirconium 

saturation threshold (several hundred parts per million) for 

subalkaline rocks. Because the zirconium threshold 

increases to values greater than 180 ppm in peralkaline liquids and at temperature greater than about 860°C, we ca.n 

infer that magmas represented by the Altiplano volcanic 

rocks did not equilibrate with peralkaline liquids or at unusually high temperatures. 

The average rubidium abundances of the Altiplano volcanic rocks and obsidian from continental margin, subduction-related settings, 130 and 135 ppm (Macdonald and 

others, 1992), respectively, are remarkably similar. Rubidium abundances of the Altiplano volcanic rocks decrease 

systematically with increasing strontium abundances (fig. 5), 

a relationship observed for most igneous rocks (Macdonald 

and others, 1992). The average rubidium-strontium ratio for 

the Altiplano rocks, 0.23, is significantly lower than the 

average value of 1.1 for obsidian from continental margin, 

subduction-related settings, however. The disparity between 

these two rubidium-strontium ratios emphasizes the disparity between strontium abundances in volcanic rocks of the 

Altiplano and those in obsidian from continental margin, 
~ 18-

La..l 

u 

a::: f- •La.J 

I'")Q.. 

ONI- 16 f- -:I: 

<e> La.J f--

31\: 

z 14f1-

z 

La.J 2f- u 

a::: 

La.J -a.. f- N 

0 

1-

1-

:I: 

(!) 

La.J 

31\: 

z 

z 

1-

z 

La.J 

u 

a::: 

La.J 

1 f-

-

-a.. 

0 011-

:::::E:I: (!) 

La.J 

3:2fz 

~10 f- La.J 

u 

e:i f- -a.. 

<61-6fu:x: (!) 

La.J f---

31\: 

Z2fGEOCHEMISTRY 17 

·:··· ·.+ 

·+. 

.. ··:: 

....... 

............... ·.';·:. ,... . -. + +·+..-.: ~~~ . ~ ~·· .. +.~ .. iit···· -.----,.~~. ~ . ········. &·····.t .. +.t.~~ .•• :::··. 

... · .. ++ 

.·.·.·.·::· •......•.. •••• .• + 

51 55 

·• + 

·· ...... :::::··.;;.·~·· . .., .. . +· .•• :li.4tl-""· + .. fi.i.·,. .. ~~ ..... #; ......... ~ .t. 

+ +++";.j .. <~~ .. ~~~-~········ .. = + 

i··· ... ·• ,.+ 

59 63 67 71 75 

Si02, IN WEIGHT PERCENT 

1-

z 

~ + 

e:i .2 1-

-a... 

0 

C:I-

:::::E:I: (!) 

La.J .1 1-

31\: 

z 

1-. 

z 

tf6ta::: •La..l 

oa... 

~~-- 4 1- Z:I: (!) 

La.J + 

31\: 21-

z 

~.51-

La..l 

u 

a::: r- La.J -a.. 

Oil) I-. 31-

N:I: 

Q..(!) 

·. 

+ + 

. :::: ....................... ~ .;~ :-~ ~!:;~;; ~~ -:~ ~ ... ~ ~ .... + ••• 

.. .;. • . • + .. + + 4 .•,..+ .. : .. 

·· ......... ·········· ... :t: ..... ~:. + + ,.. •••••••• 

........ 

······ 

........ - 1- 6_ Shoshonite series _.......,... ........ z .... ............. 

~ . ; .... 1~~ ....... t ............. ~ • ~ 4 HI gh-K . .... .... ......--; ,....;"+,.. + ': 

~1- -(calc-alkaline) ·::;..-:-:-:-..... +t··.,:..·l'~ "'t + . . ........ :· "; 2~;;iii~~;;~:~{~ 

z 

~250r­ _J 

_J 

E:::::E 

:J 

·-a::: 

~ ~ 1501- ..c 

:J(/) 

0:::1- a::: 

< fa.. 50r- z 

Calc-alkol ine series 

51 55 59 63 67 

Si02, IN WEIGHT PERCENT 

......... ..... ·· ... 

71 75 

Figure 4.- Variation diagrams showing abundances (table 1) of major oxides, normalized to 100 percent volatile free, in volcanic rock 

samples from the Bolivian Altiplano. Data for lava flows and ash-flow tuffs are shown by pluses and triangles, respectively. Dashed discriminant lines on K20 versus Si02 diagram are from Ewart (1982). Dotted line outlines the area in which data for the 59 samples of Altiplano volcanic rock of Fernandez and others (1973) and Kussmaul and others (1977) plot. 
18 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

z 

0 

-

...J 

...J 

-

i 200-

a:: 

w 

a. 

(/) 

~ 

~ - a. 

z 

-:i 100 I- :::> 

c; 

-

lil 

:::> 

a:: I0 

....... ·· ... 

······· ... 

+ 

+ \ + 

+/ 

++ / +... • • ,. ++ .J.•; + ·· .. , • 

'·.··.. /' + + i + .. + ····-.. :.··· ... ../ +• + + -$-+ i + +• • + i + 

~--...... + +,. + 

-!f + + + + 

/+ + + 

i+ +! 

+ .. ·· ... ·· 

I I I 

+ 

+ 

+ 

I 

400 800 

• ASH-FLOW TUFF 

+ LAVA 

=l=t- + 

+ + .6j.. + + + 

+ 

I I 

1200 

STRONTIUM, IN PARTS PER MILLION 

+ 

Figure 5. Variation diagram showing rubidium and strontium 

abundances (table 1) in volcanic rock samples from the Bolivian 

Altiplano. Dotted line outlines the area in which data for the 59 

samples of Altiplano volcanic rock of Fernandez and others (1973) 

and Kussmaul and others ( 1977) plot. 

subduction-related settings. Rubidium-strontium ratios in 

most of the Altiplano volcanic rocks are between 0.1 and 0.9 

and are approximately normally distributed, though slightly 

skewed toward higher values, about the mean value (fig. 6). 

The degree of magmatic evolution displayed by volcanic rocks of the Altiplano is depicted by their relative rubidium, potassium, and strontium abundances (fig. 7). 

Abundances of these elements are principally controlled by 

feldspar (Hanson, 1978); abundances of strontium and 

rubidium are most and least, respectively, depleted by feldspar fractionation. Thus, as feldspar fractionation and 

differentiation proceed, potassium and, to an even greater 

extent, rubidium are concentrated in the residual liquid 

relative to strontium. Compositions plotting nearest the 

strontium apex of the rubidium-potassium/100-strontium 

ternary diagram represent the least evolved magmas. Volcanic rocks of the Altiplano are very slightly less evolved 

than middle Tertiary, subduction-related ash-flow tuffs of 

southern Nevada (for instance, du Bray, in press) and are 

significantly less evolved than strongly rubidium-enriched, 

within-plate igneous rocks (for instance, du Bray and 

others, 1988). 

Pearce and others (1984) recognized that intrusive 

rocks generated in various tectonic settings have distinctive 

geochemical signatures, and they developed trace element 

discriminant diagrams from which tectonic setting can be 

inferred. Trace element abundance variations in coeval volcanic and plutonic rocks generated in a given terrane should 

be similar. Consequently, compositions of the Altiplano 

(/) 

w 

20 

~ 15 :::::!: 

<( 

(/) 

LL.. 

0 

a:: 

~ 10 :::::!: 

::> 

z 

5 

0 

-= : 

••••••••••••• : 

:: 

- :: 

,__ 

~ 

0.5 

-

-

-

-

-'tc=l 

I I I f:7:l ~I I 

1 .5 2 

RUBIDIUM/STRONTIUM 

Figure 6. Histogram showing rubidium-strontium ratios for volcanic rock samples from the Bolivian Altiplano. 

volcanic rocks can be compared to the tectonic setting-trace 

element grids developed by Pearce and others (1984 ). Trace 

element data for nearly all of these samples plot in the volcanic arc field on these diagrams (fig. 8). Gill (1981) indicated 

that barium-niobium ratios of modern arc rocks are greater 

than 26; negative niobium anomalies on extended trace element diagrams are a diagnostic geochemical characteristic of 

continental volcanic arc rocks. The average barium to niobium ratio for the Altiplano volcanic rocks is 66, and negative niobium anomalies are a ubiquitous feature of the 

Altiplano volcanic rocks. Barium to niobium ratios for the 

Altiplano volcanic rocks range from 10 to 192 and are 

approximately normally distributed around the mean; only 

two samples have ratios less than 30, and only six samples 

have ratios greater than 130. In addition, major oxide compositions for the Altiplano volcanic rocks follow a calc-alkaline trend parallel to but displaced below the Cascade trend 

on an AFM (Na20+K20, FeO*, MgO) diagram (fig. 9). 

These compositional features support the observation that 

middle to upper Tertiary Altiplano volcanic rocks are subduction-related, continental volcanic arc magmas and corroborate the utility of this type of diagram in tectonic 

discriminant analysis. 

ALTERED ROCKS 

The abundances of a number of the major oxides in 23 

altered volcanic rock samples are atypical of the average 

composition of the Altiplano volcanic rocks in particular and 

igneous rocks in general; the anomalous compositions of 
GEOCHEMISTRY 19 

POTASSIUM/100 

• 

r···· ... ++ • • 

···o:~:: ............... ..., ... ···\ 

A ASH-FLOW TUFF 

RUBIDIUM STRONTIUM 

Figure 7. Ternary variation diagram showing the relative proportions of rubidium, potassium, and strontium (table 1) in volcanic 

rock samples from the Bolivian Altiplano. Dotted line outlines the 

area in which data for the 59 samples of Altiplano volcanic rock of 

Fernandez and others (1973) and Kussmaul and others (1977) plot. 

these samples probably result from geochemical remobilization caused by hydrothermal alteration (table 2). In most of 

the altered Altiplano volcanic samples, Na20 abundances 

are low to very low (average, 1.41 weight percent) and K20 

abundances are high (average, 6.91 weight percent) relative 

to average Altiplano volcanic rocks and to other calc-alkaline igneous rocks; most of these samples also have unusually low to very low CaO (average, 1.21 weight percent) 

contents and high LOI values (average, 4.22 weight percent). 

Si02 abundances in several samples (DROOl A, BG024, 

and SL003) exceed 78 weight percent, the maximum value 

for normal igneous rocks. In addition, Si02 abundances in 

several other samples (PNZ10, SL002, and ES016), which 

similar to the previous three samples were identified as dacite during field investigations, are high relative those characteristic of Altiplano dacites. The compositions of these six 

samples are similar, with regard to low Na20 and CaO and 

high K20 abundances, to those of samples described in the 

preceding paragraph except they also have high Si02 abundances. LOI values in most of these same samples are high, 

relative to the value of 2 weight percent characteristic of 

unaltered Altiplano volcanic rocks, and are as high as more 

than 7 weight percent. 

Abundances of a number of the trace elements in the 

altered rocks are systematically different from those of the 

average Altiplano volcanic rock. As befits their spatial association with mineralized rock related to polymetallic mineral 

deposits, many of the 23 altered samples contain variously 

elevated abundances of combinations of arsenic, lead, 

• ASH-FLOW TUFF z 

0 + LAVA _J WITHIN PLATE 

= 1000 :::E 

0:: 

w 

0... 

(/) 

1-

0:: 

<( 100 0... 

z 

. 

:::E 

::::) 

0 10 

m 

::::) 

0:: 

VOLCANIC ARC OROGENIC 

1L-------~------~~--------~L-------~ 

1 10 100 1000 

YTTRIUM AND NIOBIUM, IN PARTS PER MILLION 

A 

1000~------------------------~--------L-~ 

z WITHIN PLATE 0 

_J 

_J 

:::E 100 0:: 

w 

0... VOLCANIC ARC (/) 

1-

0:: 

<( 

0... 

z OROGENIC 

10 :::E 

::::) 

m 

0 

z 

• ASH-FLOW 

+ LAVA 

10 100 

B YTTRIUM, IN PARTS PER MILLION 

Figure 8. Trace element-tectonic setting discrimination variation 

diagrams showing compositions (table 1) volcanic rock samples 

from the Bolivian Altiplano. Tectonic setting-composition boundaries are from Pearce and others (1984). A, Rubidium versus yttrium and niobium. B, Niobium versus yttrium. 

antimony, tin, and zinc (U.S. Geological Survey and Servicio Geologico de Bolivia, 1992). In addition, rubidium 

abundances in the altered rocks are high relative to the average Altiplano volcanic rock (table 1 ), whereas strontium 

abundances are depleted. Barium abundances are erratically 

distributed; some of the altered samples are characterized by 

dramatically elevated barium abundances, whereas others 

have depleted abundances. Most altered samples having 

high Si02 abundances have slightly high tin abundances 
20 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

A 

F 

HAWAII AN 

........... ········CASCADE 

CALC-ALKALINE 

TUFF 

M 

Figure 9. Ternary AFM (Na20+K20, FeO*, MgO) diagram 

showing compositions of volcanic rock samples from the Bolivian 

Altiplano. Cascade calc-alkaline trend line from Irvine and Baragar 

(1971). Dotted line outlines the area in which data for the 59 samples of Altiplano volcanic rock of Fernandez and others (1973) and 

Kussmaul and others ( 1977) plot. 

relative to the average Altiplano volcanic rock and to the 

other altered Altiplano samples. Abundances of yttrium, zirconium, niobium, and the light rare earth elements in the 

altered samples are virtually indistinguishable from those of 

the average Altiplano volcanic rock, supporting the observation that these elements are relatively immobile during 

weathering and alteration processes. 

DISCUSSION AND CONCLUSIONS 

UNALTERED ROCKS 

The most primitive (baseline composition) volcanic 

rocks of the western South America continental margin volcanic arc are compositionally distinct relative to those 

erupted from intraoceanic volcanic arcs (Davidson and others, 1991). Initially, baseline compositions of central volcanic zone magmas were thought to be inherited from 

subcontinental mantle lithosphere, but Davidson and others 

( 1991) rejected the hypothesis because isotopic data ( especially oxygen) for the central volcanic zone magmas do not 

support their derivation from that source. Hildreth and 

Moorbath (1988) and Davidson and others (1991) suggested 

that the compositional distinctiveness of the Andean arc 

magmas resulted from extensive interaction between these 

magmas, probably mostly mantle derived, and crustal material during magma ascent through exceptionally thick continental crust beneath the Andean arc; the primary, mantle 

magmas experienced major chemical modification through 

crustal interaction. This interpretation suggests that the predominantly dacitic composition of middle to upper Tertiary 

volcanic rocks of the Bolivian Altiplano reflects, in part, 

considerable modification of primitive asthenospheric mantle-derived melts by assimilation of crustal material, including partial melts, along their ascent paths. Alumina 

saturation indices of the Altiplano volcanic rocks (average, 

0.958), however, preclude the involvement of significant 

amounts of sedimentary rock in the crustal assimilation-partial melting assemblage (Chappell and White, 1992), which 

suggests that the assimilated crustal component was mostly 

igneous. 

Linear arrays on some variation diagrams (fig. 4) are 

consistent with geochemical evolution involving, via restite 

unmixing or crystal fractionation, the phenocryst assemblage observed in dacitic rocks of the Altiplano; however, 

the relative importances of crystal fractionation versus restite unmixing involving this mineral assemblage are uncertain. These data arrays are also characterized by very low 

correlation coefficients (large amounts of data scatter), 

which probably result from assimilation of varying amounts 

of compositionally diverse crustal materials. The importance 

of these various processes is probably highly variable among 

the volcanic centers of the Altiplano. Primary, asthenospheric mantle-derived basaltic partial melts and their differentiates probably represent baseline compositions from 

which more evolved (dacitic to rhyolitic) magmas were 

derived by assimilation and fractional crystallization. 

Kussmaul and others (1977) considered the K-h relationship (increasing K20 content of arc-derived volcanic 

rocks with increasing distance above their Benioff zone) of 

Dickinson and Hatherton ( 1967) and concluded that such a 

relation does not exist for middle to upper Tertiary volcanic 

rocks of the Bolivian Altiplano. As Kussmaul and others 

(1977) indicated, south of lat 20° S. the Peru-Chile trench 

strikes approximately north. Consequently, assuming that 

the inclination of the Benioff zone does not vary beneath the 

southern Altiplano, the K-h relationship can be evaluated by 

considering K20 content of volcanic rocks as a function of 

longitude. 

Our data suggest that K20 contents of middle to upper 

Tertiary volcanic rocks of the Bolivian Altiplano are weakly 

correlated with longitude; that is, with distance above the 

Benioff zone. Of the 82 unaltered samples collected as part 

of this study, 39 are from sites south of lat 20° S., where the 

trench strikes approximately north. The mean and standard 

deviation (number of samples for each average given in 

parentheses) of K20 content of samples collected in four 

0.5°-wide longitude strips between long 68° and 66° W. are 

3.30±0.59 (13), 3.28±1.04 (5), 3.57±1.05 (8), and 3.86±0.72 

(7), respectively. Although these average values are indistinguishable in light of their associated standard deviations, the 

averages, 3.30-3.28-3.57-3.86 increase to the east, with 

increasing distance above the Benioff zone, and the overall 
REFERENCES CITED 21 

trend of K20 abundances for the 39 samples also increases 

to the east. The average %s value (Dickinson and Hatherton, 

1967) for the four longitude-based samples groups, about 3.5 

percent K20, indicates a depth to Benioff zone of 250±100 

km (Dickinson, 1970). This depth estimate is in accord with 

the estimate of Barazangi and !sacks (1976), determined by 

considering the spatial distribution of subduction-related 

earthquake hypocenters, for depth to the modem Benioff 

zone below the Altiplano at approximately lat 20° S. 

Consequently, assuming that the inclination of the 

Oligocene-Miocene Benioff zone beneath the Altiplano 

region was similar to its present-day inclination, it is likely 

that the petrogenetic factors that have caused K20 abundances in volcanic rocks to be correlated with distance above 

Benioff zones in many other subduction-related volcanic 

arcs (Dickinson, 1970) may also have influenced the K20 

content of Andean arc Altiplano volcanic rocks. 

Feeley ( 1993) noted similar systematic, across-arc 

geochemical trends in Quaternary volcanic rocks of the 

southern Salar de Uyuni region. Specifically, he suggested 

that systematic variations in strontium, rubidium, and K20 

abun~ances are related to the subduction process itself and 

reflect extensive lower crust hybridization by interaction 

with primary basaltic magmas beneath the active volcanic 

front. Magmas ascending somewhat inboard of the active 

volcanic front will be contaminated by less hybridized lower 

crust and will consequently contain higher abundances of 

rubidium and K20 and lower abundances of strontium. 

ALTERED ROCKS 

The largest group of altered Altiplano volcanic rocks 

are those having low Na20 and CaO contents and high K20 

and LOI contents; these rocks have been affected by varying 

degrees of sericitic alteration. The distinctive major oxide 

compositions of these rocks are entirely a function of 

sericitic alteration that caused feldspar replacement by 

potassium- and hydroxyl-rich sericite. In this replacement 

process, Na20 and CaO were mobilized out of these rocks by 

circulating hydrothermal fluids. In order for plagioclase to 

be replaced by sericite, the altering fluid must have been 

potassium rich. Elevated K20 abundances in these samples 

do not represent closed-system, relative K20 enrichment 

caused by Na20 and CaO depletion because the abundances 

of the other oxides are not proportionally elevated. Consequently, the absolute abundances of K20 in these samples 

have been enhanced by the hydrothermal fluids responsible 

for sericitic alteration. Alteration proceeding elsewhere in 

these systems must have involved the breakdown of potassium-rich minerals such as potassium feldspar and biotite 

and the subsequent partitioning of potassium into the hydrothermal fluid. High rubidium abundances, low strontium 

abundances, and highly erratic barium abundances in these 

rocks probably reflect the growth of sericite at the expense of 

plagioclase because plagioclase is a principal mineralogic 

site for strontium and barium (to a lesser extent), whereas 

micas such as sericite are a principal mineralogic site of 

rubidium and barium. Sericitic alteration, inferred on the 

basis of compositional data, is borne out by petrographic 

identification of sericite replacing feldspar. Similarly, elevated K20 and rubidium abundances have been noted in 

mineralized volcanic rocks of the Julcani district in Peru 

(Scherkenbach and Noble, 1984). 

Similarly, silicification inferred on the basis of compositional data is in accord with petrographic identification of 

secondary silica in half a dozen samples. These six Altiplano 

dacite samples have high Si02 contents and have been silicified to varying degrees. In addition, similar to the rocks 

described previously, the major oxide abundances of these 

samples suggest sericitic alteration of feldspars, especially 

plagioclase. 

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of earthquakes and subduction of the Nazca plate beneath 

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Chappell, B.W., and White, A.J.R., 1992, 1- and S-type granites in 

the Lachlan Fold Belt, in Brown, P.E., and Chappell, B.W., 

eds., Second Hutton symposium, the origin of granites and 

related rocks: Transactions of the Royal Society of Edinburgh, 

V. 83, p. 1-26. 

Davidson, J.P., and de Silva, S.L., 1992, Volcanic rocks from the 

Bolivian Altiplano-Insights into crustal structure, contamination, and magma genesis in the central Andes: Geology, v. 20, 

p. 1127-1130. 

Davidson, J.P., Harmon, R.S., and Womer, Gerhard., 1991, The 

source of central Andean magmas; some considerations: Geological Society of America Special Paper 265, p. 233-243. 

de Silva, S.L., 1991, Styles of zoning in central Andean ignimbrites; insights into magma chamber processes: Geological 

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Dewey, J.F., and Bird, J.M., 1970, Mountain belts and the new global tectonics: Journal of Geophysical Research, v. 75, p. 

2625-2647. 

Dickinson, W.R., 1970, Relations of andesites, granites, and derivative sandstones to arc-trench tectonics: Reviews in Geophysics and Space Science, v. 8, p. 813-860. 

Dickinson, W.R., and Hatherton, Trevor, 1967, Andesitic volcanism and seismicity around the Pacific: Science, v. 157, p. 

801-803. 

du Bray, E.A., in press, Geochemistry and petrology of Oligocene 

and Miocene ash-flow tuffs of the southeastern Great Basin: 

U.S. Geological Survey Professional Paper 1559, 44 p. 

du Bray, E.A., Elliott, J.E., and Stuckless, J.S., 1988, Proterozoic 

peraluminous granites and associated Sn-W deposits, Kingdom of Saudi Arabia, in Taylor, R.P., and Strong, D.F., eds., 

Recent advances in the geology of granite-related mineral 
22 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

deposits: Canadian Institute of Mining and Metallurgy Special 

Volume 39, p. 142-156. 

Elsass, F.E., and du Bray, E.A., 1982, Energy-dispersive X-ray 

fluorescence spectrometry with the Kevex 7000 system: Saudi 

Arabian Deputy Ministry Mineral Resources Open File Report 

USGS-OF-02-52, 53 p. 

Ewart, A., 1982, The mineralogy and petrology of Tertiary-Recent 

orogenic volcanic rocks with special reference to the andesitic-basaltic compositional range, in Thorpe, R.S., ed., Andesites: Chichester, Wiley, p. 25-87. 

Feeley, T.C., 1993, Crustal modification during subduction-zone 

magmatism-Evidence from the southern Salar de Uyuni 

region (22°-22°S), central Andes: Geology, v. 21, p. 

1019-1022. 

Fernandez, C.A., Hormann, P.K., Kussmaul, Siegfried, Meave, J., 

Pichler, H., and Subieta, T., 1973, First petrographic data on 

young volcanic rocks of SW-Bolivia: Tschermaks Mineralogische und Petrographische Mittheilungen, v. 19, p. 149-172. 

Gill, James, 1981, Orogenic andesites and plate tectonics: New 

York, Springer-Verlag, 390 p. 

Hanson, G.N., 1978, The application of trace elements to the petrogenesis of igneous rocks of granitic composition: Earth and 

Planetary Science Letters, v. 38, p. 26--43. 

Harmon, R.S., and Rapela, C.W., 1991, Andean magmatism and 

its tectonic setting: Geological Society of America Special 

Paper 265. 

Hildreth, W.E., and Moorbath, Stephen, 1988, Crustal contributions to arc magmatism in the Andes of central Chile: Contributions to Mineralogy and Petrology, v. 98, p. 455--499. 

Irvine, T.N., and Baragar, W.R.A., 1971, A guide to the chemical 

classification of volcanic rocks: Canadian Journal of Earth Sciences,v. 8,p.523-548. 

Jackson, L.L., Brown, F.W., and Neil, S.T., 1987, Major and minor 

elements requiring individual determination, classical whole 

rock analysis, and rapid rock analysis, in Baedecker, P.A., ed., 

Methods for geochemical analysis: U.S. Geological Survey 

Bulletin 1770, p. G1-G23. 

James, D.E., 1971, Plate tectonic model for the evolution of the 

Central Andes: Geological Society of America Bulletin, v. 82, 

p. 3325-3346. 

Krauskopf, K.B., 1967, Introduction to geochemistry: New York, 

McGraw-Hill, 721 p. 

Kussmaul, Siegfried, Hormann, P.K., Ploskonka, E., and Subieta, 

T., 1977, Volcanism and structure of SW Bolivia: Journal of 

Volcanology and Geothermal Research, v. 2, p. 73-111. 

Le Bas, M.J., Le Maitre, R.W., Streckeisen, A.L., and Zannetin, 

Bruno, 1986, A chemical classification of volcanic rocks based 

on the total alkali-silica diagram: Journal of Petrology, v. 27, p. 

745-750. 

Published in the Central Region, Denver, Colorado 

Manuscript approved for publication November 17, 1994 

Edited by Judith Stoeser 

Graphics prepared by the authors, Denny Welp, and Alex Donatich 

Photocomposition by Mari L. Kauffmann 

Macdonald, Ray, Smith R.L., and Thomas, J.E., 1992, Chemistry of 

the subalkalic silicic obsidians: U.S. Geological Survey Professional Paper 1523, 214 p. 

McBride, S.L., 1977, A K-Ar study of the Cordillera Real, Bolivia, 

and its regional setting: Kingston, Canada, Queen's University, 

Ph.D. thesis, 230 p. 

Middlemost, E.A.K., 1989, Iron oxidation ratios, norms and the classification of volcanic rocks: Chemical Geology, v. 77, p. 19-26. 

Mitchell, A.H., and Reading, H.G., 1969, Continental margins, 

geosynclines, and ocean floor spreading: Journal of Geology, 

v. 77, p. 629-646. 

Pearce, J.A., Harris, N.B.W., and Tindle, A.G., 1984, Trace element discrimination diagrams for the tectonic interpretation of 

granitic rocks: Journal of Petrology, v. 25, p. 956-983. 

Redwood, S.D., and Macintyre, R.M., 1989, K-Ar dating of 

Miocene magmatism and related epithermal mineralization of 

the northeastern Altiplano of Bolivia: Economic Geology, v. 

84, p. 618-630. 

Richter, D.H., Ludington, S.D., and Sofia-Escalante, Eduardo, 

1992, Geologic setting, in Geology and mineral resources of 

the Altiplano and Cordillera Occidental, Bolivia: U.S. Geological Survey Bulletin 1975, p. 14-24. 

Sawyer, D.A., and Sargent, K.A., 1989, Petrologic evolution of 

divergent peralkaline magmas from the Silent Canyon caldera 

complex, southwestern Nevada volcanic field: Journal of Geophysical Research, v. 94, p. 6021-6040. 

Scherkenbach, D.A., and Noble, D.C., 1984, Potassium and rubidium metasomatism at the Julcani district, Peru: Economic 

Geology, v. 79, p. 565-572. 

Sempere, Thierry, Herail, Gerard, Oller, Jaime, and Bonhomme, 

M.G., 1990, Late Oligocene-early Miocene major tectonic crisis and related basins in Bolivia: Geology, v. 18, p. 946-949. 

Taggart, J.E., Lindsay, J.R., Scott, B.A., Vivit, D.V., Bartel, A.J., 

and Stewart, K.C., 1987, Analysis of geologic materials by 

X-ray fluorescence spectrometry, in Baedecker, P.A., ed., 

Methods for geochemical analysis: U.S. Geological Survey 

Bulletin 1770, p. E1-E19. 

Thorpe, R.S., Francis, P.W., Hammill, M., and Baker, M.C.W., 

1982, The Andes, in Thorpe, R.S., ed., Andesites: John Wiley 

and Sons, New York, p. 187-205. 

U.S. Geological Survey and Servicio Geologico de Bolivia, 1992, 

Geology and mineral resources of the Altiplano and Cordillera 

Occidental, Bolivia: U.S. Geological Survey Bulletin 1975, 

365 p. 

Watson, E.B., and Harrison, T.M., 1983, Zircon saturation 

revisited-Temperature and composition effects in a variety 

of crustal magma types: Earth and Planetary Science Letters, 

V. 64, p. 295-304. 
APPENDIXES 
24 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study. 

[Percentages of indicated minerals are estimates made by examination of thin sections] 

Sample no. 

90BDR001B 

90BDR005 

90BDR006 

90BDR012 

90BDR015 

90BDR016 

90BDR034 

90BDR035 

90BDR037 

90BDR038 

90BDR039 

90BDR041 

90BDR041A 

90BDR042 

90BDR043 

90BDR044 

90BDR046 

Description 

Escantaque. Dacite lava. 2-5 percent fresh biotite, 1-3 percent fresh plagioclase, and 1-3 percent fresh hornblende 

in glassy pumiceous matrix. Redwood and Macintyre (1989) presented K-Ar (biotite) ages of 5.4±0.2 and 5.7±0.2 

Ma for the uppermost Escantaque flow. 

Cerro Gordo. Dacite porphyry dome. 3-5 percent fine-grained plagioclase and 2-4 percent hornblende with altered 

rims in cryptocrystalline matrix. 

Los Frailes. Dacite ash-flow tuff. 8-10 percent fine-grained, broken, resorbed quartz, 5-10 percent plagioclase, 3-

6 percent fresh biotite, and pumice clasts. 

Sora Puncu. Dacite tuff of Ignimbrite Formation. 5-10 percent plagioclase, 2-4 percent red hornblende and 1-2 

percent resorbed quartz, with rims of opaque oxide minerals, and 1 percent biotite in a densely welded glassy 

matrix. Baker and Francis (1978) presented a K-Ar (biotite) age of 3.2±0.2 Ma for an ignimbrite (possibly the same 

one represented by 90BDR012) 2 km southwest of Sora Punca. 

Cerro Pabellon. Andesite tuff of Ignimbrite Formation. 5-8 percent broken plagioclase, 3-5 percent green 

hornblende, 1-2 percent fresh biotite, trace to 2 percent orthopyroxene, trace to 1 percent clinopyroxene, and 

pumice in a dense glassy matrix. Baker and Francis (1978) presented a K-Ar (hornblende) age of 1.7±0.5 Ma for an 

ignimbrite (possibly the same one represented by 90BDR015) 4 km north of Cerro Pabellon. 

Cerro Panizos. Dacite tuff of Ignimbrite Formation. 5-10 percent plagioclase, 5-6 percent clinopyroxene and 

possible orthopyroxene, in a densely welded cryptocrystalline matrix. 

San Francisco mine. Crystal-rich dacite ash-flow tuff. 20-25 percent plagioclase, 2-3 percent rounded quartz, 2-5 

percent fresh biotite, 1-2 percent altered hornblende, and pumice in glassy matrix. 

Mina Eskapa. Dacite porphyry flow or intrusion. 5-8 percent plagioclase and 2-5 percent fresh biotite in trachytic 

matrix of plagioclase and biotite microlites and cryptocrystalline material. U.S. Geological Survey and Servicio 

Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 6.3±0.1 Ma. 

Cerro Caquella. Andesite porphyry flow. 5-10 percent plagioclase, 3-5 percent orthopyroxene, and 1-2 percent 

fresh clinopyroxene in cryptocrystalline matrix. 

Cerro Cachi Laguna. Dacite porphyry flow. 10-15 percent plagioclase, 1-3 percent fractured quartz, 1-2 percent 

completely altered hornblende, 1-2 percent completely altered biotite, and trace? clinopyroxene in trachytic matrix 

containing plagioclase microcrystallites and cryptocrystalline material. 

Cerro Apacheta. Andesite porphyry flow. 10-15 percent plagioclase, 2-3 percent fresh biotite, 1-2 percent quartz, 

1-2 percent fresh hornblende, trace to 1 percent orthopyroxene, and trace clinopyroxene in cryptocrystalline matrix. 

Cerro Amarillo. Dacite porphyry flow. 

Cerro Poderosa. Andesite porphyry flow. 

Rio Chunchillerito. Crystal-rich dacite ash-flow tuff. 10-15 percent broken plagioclase, 2-5 percent rounded 

quartz, 2-5 percent biotite, and 1-2 percent hornblende in nonflattened pumice matrix. 

Cerro Pabellon. Dacite porphyry flow. 5-10 percent plagioclase, 1-3 percent orthopyroxene, 1-2 percent fresh 

hornblende, and xenocryst clots in cryptocrystalline matrix. 

Cerro Panizos. Dacite ash-flow tuff. 10-15 percent plagioclase, 2-3 percent clinopyroxene, 1-2 percent 

orthopyroxene, 1 percent hornblende, 1 percent biotite, and xenocrysts in densely welded glassy matrix. 

Cerro Panizos. Dacite ash-flow tuff. 8-12 percent plagioclase, 3-5 percent orthopyroxene, 3-5 percent highly 

altered hornblende and biotite, 2-3 percent clinopyroxene, and trace quartz in a cryptocrystalline matrix. 
REFERENCES CITED 25 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study-Continued. 

Sample no. 

90BDR053 

90BDR054 

90BDR055 

90BDR057 

90BDR060B 

90BG001A 

90BG003 

90BG004 

90BG013C 

90BG059 

90BR008 

90BR010 

90BR019 

90BR020 

Description 

Mina Escala. Dacite porphyry debris flow. Clasts of densely welded ash-flow tuff. 10-20 percent plagioclase, 1-3 

percent fresh hornblende, 1-3 percent fresh biotite, and 1-2 percent rounded quartz in glassy matrix. U.S. 

Geological Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 18.2±0.3 Ma. 

Mina Rosario. Basalt flow. 10-15 percent plagioclase, 5-8 percent clinopyroxene in rounded clots, and 1-3 

percent opaque oxide minerals in intergranular matrix of plagioclase and clinopyroxene. 

Mina Escala. Rhyolite porphyry intrusion. 3-5 percent plagioclase, 2-3 percent rounded quartz, 1-2 percent fresh 

biotite, and 1-2 percent opaque oxide minerals in cryptocrystalline matrix. U.S. Geological Survey and Servicio 

Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 18.0±0.2 Ma. 

Cerro Aguilar. Dacite porphyry flow. 5-10 percent saussuritized plagioclase, 2-3 percent fresh to altered biotite, 

1-2 percent opaque oxide minerals, 1 percent altered hornblende, and trace to 1 percent rounded quartz in 

cryptocrystalline matrix. 

Bolivar mine. Dacite porphyry dome. 10-15 percent fresh plagioclase, 2-5 percent fresh to locally altered biotite, 

and 1-2 percent embayed quartz in cryptocrystalline matrix. 

Several low hills about 7 km north of Cerro Tata Sabaya. Undeformed, reddish, fine- to medium-grained, seriate 

(monzo?) granite. Slightly more quartz than plagioclase and slightly more plagioclase than alkali feldspar; 

accessory zircon and thulite. Graphic intergrowths common. About 8 percent brick-red altered unknown mafic 

silicate minerals. 

Todos Santos. Rhyolite dome. Brown vitrophyre breccia. Vitrophyre about 30m thick. Clasts are angular, 

silicified flow-banded rhyolite; matrix is brown glass with ~1 percent small biotite phenocrysts. U.S. Geological 

Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 6.1±0.2 Ma for sample 

90BR004 (no chemistry), a sample collected near 90BG003, of rhyodacite from Todos Santos. 

Todos Santos. Rhyolite dome. White, flow-banded with <<1 percent biotite and sparse quartz and sanidine 

phenocrysts. U.S. Geological Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 

6.1±0.2 Ma for sample 90BR004 (no chemistry), a sample collected near 90BG004, of rhyodacite from Todos 

Santos. 

Saca Sacani. Andesite flow. Collected as float; assumed to be host rock to native sulfur prospects on Cerro Saca 

Sacani. Most rocks near here strongly altered by some combination of argillization, iron oxide staining, 

alunitization, and secondary gypsum deposition. 

Cerro Husachata, Salinas de Garci Mendoza. Andesite porphyry dike (N. 10° E., vertical) in andesite breccia near 

Guadalupe mine. 20 percent feldspar phenocrysts as long as 4 mm, and <1 percent fine mafic silicate minerals 

(including biotite). 

About 1.5 km west of Negrillos. Andesite breccia. Gray plagioclase-phyric, fine-grained flank flows from a 

stratovolcano west of Negrillos but could be part of Carangas volcanic sequence. 

About 2.5 km south ofNegrillos. Rhyolite ash-flow tuff. 10-15 percent phenocrysts, mainly plagioclase and 

biotite and minor sanidine and opaque oxide minerals, in reddish-brown vitroclastic matrix. U.S. Geological 

Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 21.7±0.7 Ma. 

South flank of Cerro Curumaya, about 10 km west of Todos Santos. Andesite lava. Flow-aligned plagioclase and 

hornblende in a very fine grained matrix of plagioclase rnicrolites and cryptocrystalline, subvitreous mesostasis. 

Middle-lower slopes on south side of Cerro Curumaya. Dacite lava. Frothy, glassy, light-gray porphyritic flow 

interlayered with dark hornblende andesite or dacite flows represented by 90BR019. 30-35 percent phenocrysts, 

microphenocrysts, and crystal fragments in a nearly colorless glass with some perlitic fractures. Phenocrysts of 

mainly zoned plagioclase, euhedral hornblende, clinopyroxene, and biotite and accessory apatite, zircon, and 

opaque oxide minerals. Biotite >hornblende-clinopyroxene. 
26 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study-Continued. 

Sample no. 

90BR022 

90BR031 

90BR036G 

90BR037 

90BR041 

90BR044 

90BR044A 

90BPNZ01 

90BPNZ03 

90BPNZ05 

90BPNZ06 

90BPNZ07 

90BSL004 

90BSL034 

90BSL040 

90BSL046 

90BSL047 

Description 

North of La Rivera, about 10 km(?) east ofTodos Santos. Rhyolite ash-flow tuff. Very light gray. 5-10 percent 

fine-grained phenocrysts of quartz, sanidine, biotite, and hornblende. Phenocrysts similar to those in tuff of the 

Mauri Formation from west of Turco (90BR037), but not as abundant; "La Rivera" tuff contains less titanite than 

the tuff west of Turco. 

Estancia Jarumani. Pink rhyolite ash-flow tuff. 5-10 percent fine-grained phenocrysts: quartz=sanidine>> 

plagioclase; sparse biotite. Accessory opaque oxide minerals, tiny zircon; rare lithic fragments. 

About 1 km south of Cerro Phasa Willkhi. Fine-grained hornblende dacite breccia. 

Pumiri Lorna, about 15 km southwest of Turco. Rhyolite ash-flow tuff. Nearly white, crystal-rich tuff. Identified 

on Turco 1: 100,000-scale geologic map as tuff of the Mauri Formation but looks like Perez Tuff. Distinctive 

bipyramidal quartz, sanidine, plagioclase, orangish biotite, red-brown hornblende. Apatite present; zircon not 

identified. Abundance of euhedral titanite conspicuous. Rare small lithic fragments. 

Salinas de Garci Mendoza. Porphyritic basalt intrusion. Large 1-2 em feldspar phenocrysts; plagioclase>> 

orthoclase. Mafic phenocrysts of hornblende and biotite. 

Salinas de Garci Mendoza. Dacite porphyry intrusive(?) or dome northwest of 90BR041. Rock essentially the 

same as 90BR041 but contains fine clay alteration that obscures much of matrix. Large 1-2 em feldspar 

phenocrysts; plagioclase>>orthoclase. Mafic phenocrysts, hornblende, and biotite, quite oxidized. 

Salinas de Garci Mendoza. Weakly altered dacite porphyry intrusive(?) similar to 90BR044. 

Panizos caldera. Dacite ash flow tuff. 

Panizos caldera. Dacite ash flow tuff. 

Panizos caldera. Dacite ash flow tuff. 

Panizos caldera. Dacite ash flow tuff. 

Panizos caldera. Dacite ash flow tuff. 

La Joya. Dacite porphyry; about 20 percent crystals. Phenocrysts are 10 percent plagioclase (moderately altered to 

sericite), 3 percent biotite (altered to chlorite), and 2 percent embayed quartz in a cryptocrystalline matrix; accessory 

zircon and trace pyrite. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 14.3±0.4 Ma. 

La Barca. Holocrystalline mafic enclave in La Barca dacite. About 20 percent phenocrysts composed of oxidized 

mafic silicates (probably mostly biotite but including some hornblende) and occasional plagioclase phenocrysts; 

accessory zircon. Groundmass principally fine-grained plagioclase and interstitial chlorite. Redwood and 

Macintyre (1989) presented a K-Ar (biotite) age of 14.3±0.4 Ma. 

Llallagua. Dacite porphyry; about 15 percent crystals. Phenocrysts are 5 percent hornblende (altered to chlorite, 

biotite, and opaque oxide minerals), 4 percent biotite (altered to chlorite and opaque oxide minerals) 4 percent 

plagioclase (moderately altered to sericite), 1 percent opaque oxide minerals, and 1 percent embayed quartz in a 

cryptocrystalline matrix; accessory apatite. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 

14.3±0.4 Ma. 

Llallagua. Dacite porphyry; about 20 percent crystals. Phenocrysts are 10 percent oxidized biotite, 5 percent 

plagioclase (weakly sericitized), 3 percent quartz, and 2 percent potassium feldspar in a devitrified cryptocrystalline 

sericitized matrix; accessory apatite, zircon, opaque oxide minerals. Redwood and Macintyre (1989) presented a KAr (biotite) age of 14.3±0.4 Ma. 

La Joya. Dacite porphyry; about 25 percent crystals. Phenocrysts are 12 percent oxidized biotite, 5 percent 

plagioclase (weakly sericitized), 3 percent quartz, 3 percent altered hornblende, and 2 percent potassium feldspar 

(weakly sericitized) in a devitrified cryptocrystalline sericitized matrix; accessory apatite, zircon, opaque oxide 

minerals. Secondary calcite and chlorite. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 

14.3±0.4 Ma. 
REFERENCES CITED 27 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study-Continued. 

Sample no. 

90BSL048 

90BSL050 

90BSL051 

90BSL054 

90BSL057 

90BSL060 

90BSL067 

90BSL073 

90BSL074 

90BSL079 

90BSL102 

90BSL104 

90BSL105 

90BSL106 

90BSL107 

Description 

La Joya. Dacite porphyry; about 30 percent crystals. Phenocrysts are 12 percent oxidized biotite, 11 percent 

plagioclase (weakly altered to sericite), 5 percent hornblende, 4 percent potassium feldspar, and 3 percent quartz in 

a devitrified cryptocrystalline matrix altered to sericite; accessory apatite, titanite, zircon, opaque oxide minerals, 

and clinopyroxene. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 14.3±0.4 Ma. 

Cerro Llallagua. Rhyolite porphyry; about 30 percent crystals. Phenocrysts are 14 percent plagioclase, 14 percent 

potassium feldspar, 1 percent ernbayed quartz, and 1 percent oxidized biotite; accessory zircon and opaque oxide 

minerals. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 14.3±0.4 Ma. 

Cerro Quirnsa Chata. Weakly welded, porphyritic rhyolite ash-flow tuff; about 15 percent crystals. Phenocrysts are 

6 percent biotite, 4 percent plagioclase, 3 percent potassium feldspar, 1 percent quartz, and 1 percent hornblende in 

incipiently devitrified matrix of pumice shards; accessory titanite, zircon, apatite, and opaque oxide minerals. 

Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 8.8±0.3 Ma. 

Laurani. Dacite porphyry; about 20 percent crystals. Phenocrysts are 8 percent oxidized biotite, 7 percent feldspar 

(altered to sericite and calcite), 3 percent ernbayed quartz, and 2 percent altered hornblende in devitrified 

cryptocrystalline matrix; accessory apatite and titanite. Some feldspar megacrysts as large as 3 ern. Redwood and 

Macintyre (1989) presented a K-Ar (biotite) age of 8.8±0.3 Ma. 

Condor Huasi. Fine grained, porphyritic, hypidiornorphic granular granodiorite with abundant amphibolite 

xenoliths. Phenocrysts are 10 percent completely sericitized plagioclase, 7 percent hornblende, 3 percent opaque 

oxide minerals, and 1 percent quartz in completely sericitized matrix; accessory apatite. 

Condor Huasi. Dacite porphyry dike; about 20 percent crystals. Phenocrysts are 12 percent plagioclase, 4 percent 

potassium feldspar, 3 percent biotite, 1 percent quartz, and 1 percent opaque oxide minerals in devitrified 

cryptocrystalline matrix; accessory zircon. 

Todos Santos. Porphyritic dacite; phenocrysts are biotite, plagioclase, and quartz. 

Todos Santos. Porphyritic andesite; phenocrysts are hornblende, plagioclase, and quartz. 

San Antonio de Lipez. Porphyritic dacite; phenocrysts are biotite, plagioclase, and quartz. 

Jaquega. Dacite ash-flow tuff; about 30 percent crystals. Phenocrysts are 10 percent biotite, 8 percent plagioclase, 

6 percent potassium feldspar, 5 percent quartz, and 1 percent opaque oxide minerals in devitrified cryptocrystalline 

matrix; accessory zircon. Occasional unflattened pumice blocks and lithic fragments. Groundrnass extensively 

replaced by secondary calcite. 

Morokho. Porphyritic dacite; phenocrysts are biotite, plagioclase, and quartz. 

Lorna Grande. Eutaxitic dacite ash-flow tuff with about 15 percent crystals; sample from near top of tuff. Crystals 

are 7 percent biotite, 4 percent plagioclase, 3 percent potassium feldspar, and 1 percent opaque oxide minerals in a 

partially devitrified cryptocrystalline matrix of glass shards; accessory apatite, zircon, and quartz. Abundant weakly 

flattened pumice blocks. 

Lorna Grande. Eutaxitic dacite ash-flow tuff; about 20 percent crystals; sample from stratigraphically lower 

(relative to previous sample) position in tuff. Crystals are 7 percent plagioclase, 5 percent variably oxidized biotite, 

5 percent potassium feldspar, 2 percent quartz, and 1 percent opaque oxide minerals in partially devitrified 

cryptocrystalline matrix of glass shards; accessory apatite and zircon. Abundant unflattened pumice blocks. 

Lorna Grande. Eutaxitic dacite ash-flow tuff with about 20 percent crystals; sample from stratigraphically lower 

(relative to previous sample) position in tuff. Crystals are 7 percent variably oxidized biotite, 6 percent plagioclase, 

5 percent potassium feldspar, 1 percent quartz, and 1 percent opaque oxide minerals in partially devitrified 

cryptocrystalline matrix of glass shards; accessory apatite and zircon. Abundant unflattened pumice blocks. 

Lorna Grande. Eutaxitic dacite ash-flow tuff; about 15 percent crystals; ·sample from near base of tuff represented 

by previous three samples. Crystals are 5 percent plagioclase, 4 percent biotite, 4 percent potassium feldspar, 1 

percent quartz, and 1 percent opaque oxide minerals in partially devitrified cryptocrystalline matrix of glass shards; 

accessory apatite and zircon. Abundant weakly flattened pumice blocks and some secondary calcite. 
28 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study-Continued. 

Sample no. 

90BDB001 

90BDB003 

90BDB004 

90BDB005 

90BDB006 

90BDB007 

90BDB008 

90BDB009 

90BDB010 

90BDB011 

90BDB012 

90BDB013 

90BES011 

90BES012 

90BES013 

Description 

Sica Sica. Dacite porphyry; about 15 percent crystals. Phenocrysts are 10 percent plagioclase, 2 percent oxidized 

biotite, and 1 percent each of hornblende, quartz, and opaque oxide minerals in cryptocrystalline matrix of 

devitrified glass; accessory titanite. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 10.1±0.4 Ma. 

Sica Sica. Dacite porphyry; about 10 percent crystals. Weakly trachytically layered phenocrysts are 8 percent 

plagioclase, 1 percent oxidized biotite, 1 percent quartz, and trace hornblende in cryptocrystalline matrix of 

devitrified glass. Rock is weakly propylitically altered and contains chlorite. Redwood and Macintyre (1989) 

presented a K-Ar (biotite) age of 10.1±0.4 Ma. 

Viscachani. Dacite porphyry; about 25 percent crystals. Phenocrysts are 15 percent plagioclase as large as 1 em, 5 

percent hornblende, 3 percent biotite, 1 percent embayed quartz, and 1 percent opaque oxide minerals in 

cryptocrystalline matrix of devitrified glass; accessory titanite and apatite. Redwood and Macintyre (1989) 

presented a K-Ar (biotite) age of 11.1±0.3 Ma. 

Viscachani. Dacite porphyry; about 20 percent crystals. Phenocrysts are 15 percent plagioclase, 4 percent biotite, 1 

percent opaque oxide minerals, and trace quartz in cryptocrystalline matrix; accessory titanite and apatite. 

Secondary calcite. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 11.1±0.3 Ma. 

Viscachani. Andesite porphyry; about 20 percent crystals. Phenocrysts are 15 percent plagioclase, 3 percent 

oxidized biotite, and 2 percent oxidized hornblende in cryptocrystalline matrix with plagioclase microlites. 

Secondary epidote. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 11.1±0.3 Ma. 

Viscachani. Dacite porphyry; about 25 percent crystals. Phenocrysts are 15 percent plagioclase, 5 percent biotite, 

and 4 percent embayed quartz in cryptocrystalline matrix; accessory apatite. Redwood and Macintyre (1989) 

presented a K-Ar (biotite) age of 12.4±0.4 Ma. 

Colquencha. Dacite porphyry; about 30 percent crystals. Phenocrysts are 17 percent plagioclase, 10 percent 

oxidized biotite, and 3 percent quartz in devitrified tryptocrystalline matrix; accessory apatite. Occasional 

potassium feldspar phenocrysts as large as 1 em. Redwood and Macintyre (1989) presented a K-Ar (biotite) age of 

16.6±0.4 Ma. 

Viscachani. Dacite porphyry; about 25 percent crystals. Phenocrysts are 12 percent plagioclase, 7 percent 

oxyhornblende, 4 percent biotite, 1 percent opaque oxide minerals, 1 percent quartz, and trace potassium feldspar in 

devitrified cryptocrystalline matrix with plagioclase microlites; accessory apatite. Phenocrysts are trachytically 

layered. 

Miriquiri. Dacite porphyry; about 20 percent crystals. Phenocrysts are 12 percent plagioclase, 5 percent potassium 

feldspar, 1 percent biotite, 1 percent opaque oxide minerals, and 1 percent embayed quartz in oxidized devitrified 

cryptocrystalline matrix. 

Comanche. Andesite porphyry. Fine- to medium-grained hypabyssal intrusion with hypidiomorphic granular 

texture. Phenocrysts are 30 percent strongly zoned plagioclase and 5 percent hornblende in fine-grained matrix of 

plagioclase, opaque oxide minerals, and hornblende. Accessory titanite and apatite. McBride ( 1977) presented a 

K-Ar (biotite) age of 17.9±1.0 Ma. 

Viacha. Dacite porphyry; about 15 percent crystals. Phenocrysts are 7 percent plagioclase, 7 percent oxidized 

biotite, and 1 percent quartz in oxidized devitrified cryptocrystalline matrix with plagioclase microlites. Accessory 

apatite, zircon, and titanite; occasional potassium feldspar phenocrysts. Redwood and Macintyre (1989) presented a 

K-Ar (biotite) age of 15.8±0.4 Ma. 

Viacha. Columnar-jointed andesite porphyry; about 25 percent crystals. Phenocrysts are 10 percent plagioclase, 10 

percent oxidized biotite, 4 percent hornblende, and 1 percent clinopyroxene in devitrified cryptocrystalline matrix 

with plagioclase microlites. Accessory apatite. 

La Espanola. Dacitic ash-flow tuff. 

La Espanola. Andesite lava. 

La Espanola. Dacite lava. 
REFERENCES CITED 29 

Appendix 1. Brief descriptions of unaltered samples collected as part of this study-Continued. 

Sample no. Description 

90BES031 La Espanola. Andesite lava. 

90BES033 Golden Hill. Dacite lava. 

90BES035 Golden Hill. Dacite lava. 

90BES036 Golden Hill. Andesite lava. 

Appendix 2. Brief descriptions of altered samples collected as part of this study. 

[Percentages of indicated minerals are estimates made by examination of thin sections] 

Sample no. 

90BDR001A 

90BDR008A 

90BDR008B 

90BDR010 

90BDR025 

90BDR030 

90BDR031 

90BDR058C 

90BDR061C 

90BG022B 

90BG024 

90BPNZ10 

Description 

Cerro La Joya. Dacite porphyry intrusion. 3-6 percent altered biotite, 2-5 percent saussuritized plagioclase, 

possibly some altered hornblende, minor opaque oxide minerals, and one large resorbed quartz in cryptocrystalline 

matrix. Redwood and Macintyre (1989) presented K-Ar (biotite) age of 14.3±0.4 Ma. 

Los Toldos mine. Dacite porphyry intrusion. <5 percent saussuritized plagioclase, 2-3 percent fresh and altered 

biotite, and 1-2 percent opaque oxide minerals in altered cryptocrystalline matrix. U.S. Geological Survey and 

Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 8.5±0.3 Ma for sample 90BR010, a sample 

collected near 90BR008A. 

Inca mine. Dacite porphyry intrusion. <5 percent saussuritized plagioclase, 3 percent highly altered hornblende, 

and 1 percent green biotite in altered cryptocrystalline matrix. U.S. Geological Survey and Servicio Geologico de 

Bolivia (1992) presented a K-Ar (biotite) age of 8.5±0.3 Ma for sample 90BR010, a sample collected near 

90BR008B. 

Los Toldos mine. Dacite porphyry intrusion. 3-5 percent saussuritized plagioclase, 3-4 percent altered 

hornblende, 1 percent fresh biotite, and abundant zoisite in cryptocrystalline matrix. U.S. Geological Survey and 

Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 8.5±0.3 Ma. 

Chocaya mines. Ash-flow tuff. 

San Cristobal. Ash-flow tuff. Crystal-rich dacite tuff. 15-20 percent plagioclase, 2-3 percent fresh biotite, 1-2 

percent(?) potassium feldspar, 1 percent resorbed quartz, and pumice in glassy matrix. U.S. Geological Survey and 

Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 8.0±0.1 Ma. 

San Cristobal. Andesite porphyry intrusion. Highly altered; relicts of hornblende and saussuritized plagioclase. 

U.S. Geological Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 8.0±0.1 Ma for 

sample 90BR030, a sample collected near 90BR031. 

Salvadora mine. Dacite porphyry dome. 1-2 percent quartz; all other phenocrysts (plagioclase, hornblende, ?) 

completely altered. 

Candelaria mine. Dacite porphyry intrusion. About 1 percent quartz, and highly altered plagioclase, biotite, and 

hornblende. 

Cerro Espiritu Santos, Carangas. Rhyolite clast in hydrothermal breccia. Sparse quartz and sanidine phenocrysts in 

a white, siliceous groundmass. U.S. Geological Survey and Servicio Geologico de Bolivia (1992) presented a K-Ar 

(biotite) age of 15.4±0.5 Ma for sample 90BG024, a sample collected near 90BG022B. 

Cerro Espiritu Santos, Carangas. Rhyolite "dike" (tabular body). Biotite-quartz-sanidine rhyolite; same rock as 

clasts in breccia (90BG022B). Flow banding parallels dike orientation. U.S. Geological Survey and Servicio 

Geologico de Bolivia (1992) presented a K-Ar (biotite) age of 15.4±0.5 Ma. 

Panizos caldera. Altered ash-flow tuff. 
30 TERTIARY VOLCANIC ROCKS OF THE BOLIVIAN ALTIPLANO 

Appendix 2. Brief descriptions of altered samples collected as part of this study-Continued. 

Sample no. 

90BSL002 

90BSL003 

90BSL005 

90BSL010 

90BSL083 

90BSL09d 

90BSL103 

90BES002 

90BES003 

90BES005 

90BES016 

Description 

Kori Kollo. Silicified and sericitized dacite ash-flow tuff; abundant secondary quartz. About 5 percent embayed 

and broken quartz crystals and some plagioclase pseudomorphs in a weakly eutaxitic matrix; abundant pyrite. 

Pumice blocks abundant. · 

Kori Kollo. Silicified dacite ash-flow tuff; about 13 percent crystals. Phenocrysts are 10 percent embayed and 

broken quartz and 3 percent biotite (altered to sericite) in a eutaxitic matrix. Weakly welded; pumice blocks 

essentially unflattened. 

La Joya. Altered aplite. Very fine grained and flow-banded dike; extensively altered to very fine grained sericite. 

Redwood and Macintyre (1989) presented K-Ar (biotite) age of 14.3±0.4 Ma. 

San Jose. Altered dacite porphyry intrusion; about 15 percent crystals. Phenocrysts are 5 percent completely 

sericitized feldspar, 5 percent embayed quartz, and 5 percent biotite (completely altered to sericite) in 

microcrystalline sericitized matrix; abundant pyrite and galena. 

Jaquega. Altered flow-laminated dacite porphyry; about 20 percent crystals. Phenocrysts are 10 percent variably 

oxidized biotite, 4 percent plagioclase, 4 percent hornblende (replaced by hematite and quartz) pseudomorphs, and 

2 percent potassium feldspar in devitrified cryptocrystalline matrix; accessory apatite. 

Esmoraca. Altered dacite porphyry; about 15 percent crystals. Phenocrysts are 7 percent biotite (altered to chlorite 

and minor epidote), 5 percent feldspar (mostly altered to sericite), 2 percent opaque oxide minerals and sulfides, and 

1 percent rounded quartz in microcrystalline matrix composed of quartz, feldspar, and sericite; accessory apatite and 

zircon. 

Morokho. Altered ash-flow tuff; about 25 percent crystals. Phenocrysts are 10 percent biotite, 9 percent feldspar 

(mostly replaced by calcite), 5 percent quartz, and 1 percent opaque oxide minerals in devitrified microcrystalline 

matrix; accessory zircon. 

El Norteno. Altered volcanic rock. 

El Norteno. Silicified lava. 

El Norteno. Silicified volcanic rock. 

Golden Hill. Silicified lava. 

-tr U.S. ~ ~ OFFICE: 1995-673-046/86080 


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