Data of Geochemistry

Sixth Edition

Chapter F. Chemical Composition of Subsurface Waters

GEOLOGICAL SURVEY PROFESSIONAL PAPER 440-F

+JrW/M^

\rt$? %<mm/ ^°^ V^oData of Geochemistry

Sixth Edition

MICHAEL FLEISCHER, Technical Editor

Chapter F. Chemical Composition of Sub

surface Waters

By DONALD E. WHITE, JOHN D. HEM, and G. A. WARING

GEOLOGICAL SURVEY PROFESSIONAL PAPER 440-F

Tabulation and discussion of chemical analyses

.

many previously unpublished, representing

subsurface watersfrom many geologic

environments', with descriptions ofthe sources

ofthe waters

UNITED STATES GOVERNMENT PRINTING OFFICE, WASHINGTON : 1963
UNITED STATES DEPARTMENT OF THE INTERIOR

STEWART L. UDALL, Secretary

GEOLOGICAL SURVEY

Thomas B. Nolan, Director

REPRINTED

1964

For sale by the Superintendent of Documents, U.S. Government Printing Office

Washington, D.C., 20402 - Price 50 cents
DATA OF GEOCHEMISTRY, SIXTH EDITION

Michael Fleischer, Technical Editor

The first edition of the Data of Geochemistry, by F. W. Clarke, was published in 1908 as U.S. Geological Survey Bulletin 330. Later editions, also by Clarke, were published in 1911, 1916, 1920, and 1924 as

Bulletins 491, 616, 695, and 770. This, the sixth edition, has been written by several scientists in the Geological Survey and in other institutions in the United States and abroad, each preparing a chapter on his special field. The current edition is being published in individual chapters, titles of which are listed below. Chapters already published are indicated by boldface. Chapter A. The chemical elements

B. Cosmochemistry

C. Internal structure and composition of the earth D. Composition of the earth's crust E. Chemistry of the atmosphere

F. Chemical composition of subsurface waters, by Donald E. White, John D. Hem, and G. A. Waring

G. Chemical composition of rivers and lakes, by Daniel A. Livingstone H. Chemistry of the oceans

I. Geochemistry of the biosphere

J. Chemistry of rock-forming minerals K. Volcanic emanations, by Donald E. White and G. A. Waring

L. Phase equilibrium relations of the common rock-forming oxides except water M. Phase equilibrium relations of the common rock-forming oxides with water and (or) carbon

dioxide N. Chemistry of igneous rocks

O. Chemistry of rock weathering and soils P. Chemistry of bauxites and laterites Q. Chemistry of nickel silicate deposits R. Chemistry of manganese oxides

S. Chemical composition of sandstones—excluding carbonate and volcanic sands, by F. J. PettiJohn T. Nondetrital siliceous sediments, by Earle R. Cressman

U. Chemical composition of shales and related rocks V. Chemistry of carbonate rocks W. Chemistry of iron-rich rocks X. Chemistry of phosphorites Y. Marine evaporites, by Frederick H. Stewart

Z. Continental evaporites

AA. Chemistry of coal BB. Chemistry of petroleum, natural gas, and miscellaneous carbonaceous substances CC. Chemistry of metamorphic rocks DD. Abundance and distribution of the chemical elements and their isotopes

EE. Geochemistry of ore deposits

FF. Physical chemistry of sulfide systems

GG. The natural radioactive elements HH. Geochronology

II. Temperatures of geologic processes

JJ. Composition of fluid inclusions in
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CONTENTS

Page Abstract. - Fl

Introduction 1 Objectives 1 Genetic classification of subsurface waters 1 Other aspects 2 Chemistry of individual constituents 3

Silica. 3 Iron 3

Calcium, bicarbonate, carbonate, and pH 3 Magnesium . 4

Varieties of ionic species 4

Source and selection of tabulated data 4

Units and terminology 5 Waters of low mineral content associated with com- mon rock types 5 Waters from igneous terranes 5

Granite, rhyolite, and similar rock types 5 Gabbro, basalt, and ultramafic rocks 6 Andesite, diorite, and syenite 6 Waters from sedimentary terranes 6 Sandstone, arkose, and graywacke 6

Siltstone, clay, and shale 6 Limestone 7 Dolomite 7 Miscellaneous sedimentary rocks 7

Page Source and selection of tabulated data—Continued Waters of low mineral content associated with com- mon rock types—Continued Waters from metamorphic terranes F8

Quartzite 8 Marble. 8

Slate, schist, and gneiss 8 Waters from unconsolidated sand and gravel 8 Waters that may be, in part, connate 9

Oil-field waters 9

Spring waters similar in composition to oil-field waters 9 Waters that may be, in part, magmatic 10 Waters that may be, in part, metamorphic 11 Other special groups 11 Thermal waters associated with epithermal

mineral deposits 11 Nonthermal saline and acid mine waters 12 Other nonthermal acid mineral waters 12

Springs with large spring deposits 12 Thermal meteoric waters of deep circulation 13 Waters of salt deposits 13 References cited 59 Index 65

TABLES

Tables 1-11. Chemical analyses of ground waters: Page

1. From granite, rhyolite, and similar rock types F14

2. From gabbro, basalt, and ultramafic rock types 16

3. From andesite, diorite, and syenite 17

4. From sandstone, arkose, and graywacke 18

5. From siltstone, clay, and shale 20

6. From limestone 22

7. From dolomite 23

8. From miscellaneous sedimentary rocks 24

9. From quartzite and marble 25

10. From slate, schist, gneiss, and miscellaneous metamorphic rocks 26

11. From unconsolidated sand and gravel 28 v
VI CONTENTS

Tables 12-27. Chemical analyses of subsurface waters from specialized environments

:

Pf

12. Oil-field and gas-field waters dominated by sodium chloride F30

13. Oil-field waters and other deep-well brines high in sodium and calcium chlorides 32

14. Waters high in sulfate and bicarbonate associated with oil fields 34

15. Spring waters similar in composition to oil-field brines of the sodium chloride type 36

16. Spring waters similar to oil-field brines of the sodium calcium chloride type 38

17. Thermal waters from geyser areas in volcanic environments 40

18. Thermal sodium chloride bicarbonate waters from nongeyser areas associated with volcanism 42

19. Acid sulfate-chloride springs in volcanic environments and crater lakes 44

20. Acid sulfate spring waters associated with volcanism 46

21. Thermal bicarbonate sulfate waters in volcanic environments 47

22. Spring waters high in sodium bicarbonate and boron 48

23

.

Thermal waters closely associated with epithermal mineral deposits 50

24. Nonthermal saline and acid waters from mines and from acid-forming areas 52

25. Spring waters depositing travertine 54

26. Thermal waters that are probably entirely meteoric in origin 55

27. Waters associated with salt deposits and miscellaneous waters of high salinity 56

28. Chemical analyses of gases accompanying or related to waters of tables 12 to 27 58

29. Approximate median ratios and contents of analyses in tables 12 to 26, compared to ocean water 59
DATA OF GEOCHEMISTRY

CHEMICAL COMPOSITION OF SUBSURFACE WATERS

By Donald E. White, John D. Hem, and G. A. Waring

ABSTRACT

Chemical analyses, including many previously unpublished,

of about 300 subsurface waters from many different geological

environments throughout the world are tabulated, and descrip- tions of the sources of the waters are given. Analyses of the

dilute ground waters are arranged according to the types of rocks in which they occur; the composition of the waters is affected by many other factors, geological, climatic, chemical,

and biological. Analyses of other types of waters, such as various types of thermal waters and brines, are grouped in a

genetic classification. The compositions of the waters are dis- cussed, with special emphasis on median values of ratios of various constituents as a guide to the recognition of different genetic types of waters.INTRODUCTION

This report is concerned with the chemical composition of waters of different origin that occur below the

land surface in different geologic environments. Ground

water, as usually denned, is the part of the subsurface

water that is in the zone of saturation. Some water occurs

also in the zone of aeration between the earth's surface

and the zone of saturation and is, in part, in transit to the ground-water body. Other water, commonly not

considered as ground water, occurs in disconnected

fluid inclusions in rocks and within mineral grains, and

is considered separately in another chapter. H2 or OH ions occur also in the crystal lattices of hydrous

minerals, and in solution in magma.

Most of the data of this report are concerned with

the common types ordinarily considered as ground

waters. A few special types of waters formed at the

surface, at least in part from subsurface emanations in

volcanic and hot spring environments, are appropriately

considered here with waters entirely of subsurface

origin.

OBJECTIVES

Clarke (1924b, p. 181-217) was concerned primarily

with mineral waters; this is a loose but useful term for

all waters that differ appreciably in composition or concentration from the common potable types. His

classification was primarily by chemical type, and he

grouped together waters of obviously very different

origins.

This chapter deals with the characteristics of different

types of subsurface water but does not attempt to consider all types of subsurface water. Many gradations exist from very dilute waters, differing little from

atmospheric precipitation, to mineral waters of many

chemical types. In the first part of this paper, the

relatively dilute waters in contact with different kinds

of rocks are considered in the hope that tentative

criteria can be developed for identification of some

meteoric ground waters of the most simple histories.

In the second part, many groups of mineral waters of

different geologic environment, chemical type, and

probable origin are considered.

In table 29, median ratios of some important components are shown for 14 types of mineral waters, as well as the median content, in parts per million (ppm),

of total reported constituents, Si02 , and total combined

nitrogen (calculated as NH4). The choice of analyses was guided by principles other than those of rigid

statistical treatment; many analyses differ greatly from

the median values of the type. These differences

may be caused by normal variations in a genetic type,

by analytical errors, and by failure to recognize dif- ferences in genesis in waters included in a single table. The median values, however, are believed to constitute

potential criteria for recognizing waters of different

genetic types; they have been published previously

with only slight differences by White (1960, p. 452).

The specific numbers in table 29 are probably not

significant, but the order of magnitude of each abundance ratio is believed to be significant for most waters

of each type.

GENETIC CLASSIFICATION OF SUBSURFACE WATBBS

Ground waters can be classified by genesis, by type

of associated rock, by physical and chemical characteristics, or by use. A genetic classification is for

many purposes the most desirable, but specific and

Fl
F2 DATA OF GEOCHEMISTRY

applicable criteria are essential and can be developed

only slowly and with thorough testing.

A tentative genetic classification is shown below,

correlated with the tables that give probable examples.

A genetic classification has many possibilities of error and incorrect interpretation, but each table contains

analyses of waters from a specific geologic environment

or of a chemical type that is significant even if the

genetic correlation proves incorrect. Most of the

suggested examples of nonmeteoric waters are probably

slightly to greatly diluted with meteoric water. A. Juvenile waters (not previously involved with at- mospheric circulation ; no good criteria are known

for distinguishing them from B-5 waters).

1. Magmatic water (some diluted waters given in

tables 17 to 21).

2. Other juvenile waters?

B. Recycled or resurgent waters (previously involved

with atmospheric circulation).

1. Meteoric waters.

a. Precipitation and surface water. (See

chapters E and G.)

b. Soil water (few quantitative data; see text).

c. Most near-surface ground water (tables 1 to

11, 26, and some analyses of table 27).

2. Ocean water directly invading aquifers (no detailed analyses of proved examples).

3. Connate or fossil waters.

a. Waters of marine origin (most analyses of

tables 12 to 16; analysis 7, and possibly

analyses 8 and 11, of table 27).

b. Nonmarine types (analyses 1 and 2 of table

27; possibly analysis 5 of table 15 and

analysis 3 of table 16). 4. Metamorphic waters.

a. Water high in C02 and boron (?) (Some

analyses of tables 22 and 23?).

b. Other types that may exist.

5. Magmatic waters (no good criteria are known

for distinguishing them from A-l waters;

many diluted waters given in tables 17 to 21).

The arrangement of analyses in tables 1 to 11 does

not imply that chemical composition of the rocks is the

only decisive factor in determining composition of the

meteoric ground waters. Climate obviously affects rate of chemical weathering and degree of dilution of

the soluble products. Micro-organisms and plants

influence the composition of ground water, as do man's

activities. Most of the analyses given in the first 11

tables represent unpolluted water from temperate

climates, ranging from humid to arid. Some of the more highly mineralized waters given in these tables

probably contain small amounts of saline nonmeteoric

waters. OTHER ASPECTS

Many physical and chemical properties of water are reviewed by Hutchinson (1957, p. 195-220); isotopic

data published through 1955 also are reviewed by

Hutchinson, and recent isotopic data are planned for

chapter DD of Data of Geochemistry.

A major part of the water of underground reservoirs

passes through the soil on its way to the water table. On the other hand, much meteoric water penetrates the

ground directly from surface streams, particularly in

desert areas where recharge from streams is the principal means. Many of the processes involved in weathering of rocks and the formation of soil produce soluble

mineral matter. The physical characteristics of soil water have been studied (Terzaghi and Baver, 1942,

p. 331-384; Baver, 1956), but almost no quantitative

data are available on compositions of moisture in the zone of weathering and soil formation. Plants synthesize organic compounds from water and C02 obtained

largely from the atmosphere and give off C02 during

respiration. Decomposition of organic matter, in

major part by micro-organisms, also provides much

C02 in the soil zone. Boynton and Reuther (1938,

p. 37-42) found that the C02 content of soil gases

increased downward in the soil zone; as much as 15

percent of C02 was found in the total gases. According

to Thome and Peterson (1954, p. 22), 2 to 10 liters of

C02 per square meter of surface per day is produced in

soil where plants are growing vigorously. These

amounts of C02 if dissolved in water and available for reaction would account for 550 to 2,750 ppm of HC03 in water passing through the soil zone at a rate of 10

liters per square meter of surface per day and reacting

with rocks to form soluble bicarbonates. In contrast,

meteoric water in equilibrium with the C02 pressure of

the atmosphere can contain only 60 to 100 ppm of

HC03 (Hutchinson, 1957, p. 654-670). Many, if not

most, ground waters contain more than 100 ppm of

HC03 ; much C02 has apparently gone into solution

in the soil zone, lowering the pH of soil solutions and

increasing chemical activity.

Zonn (1945, p. 197-199) has studied the relation of

ground water quality to soil type, and Maksimovich

(1949, p. 26-32; 1950, p. 75-85) has attempted to relate

composition of ground water to composition of soil moisture in soils of different types. Similar investigations seem not to have been made outside of the

U.S.S.R.

The movement of water from the land surface to the

main body of ground water is simple in concept but

complicated in detail (see Meinzer, 1942, p. 397-412).
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F3

CHEMISTRY OF INDIVIDUAL CONSTITUENTS

The writers believe that a detailed discussion of the

chemistry of individual constituents is not needed here. In any event, because research in the general field of

water chemistry has been increasing in recent years, new knowledge of the field would soon make such a

discussion obsolete. Some of the results of recent

research relating to the chemistry of certain constituents

are briefly outlined here. Additional information on

these and other constituents can be found in discussions

by Hutchinson (1957, p. 541-902) and Hem (1959a,

p. 35-149).

SILICA

In former years the silicon dissolved in natural water was generally considered to be "colloidal silica" and

the practice of reporting the element in terms of Si02 in water analyses has persisted. Recent research on

the state of silicon in solution and its chemical behavior

has given a basis of understanding not formerly available. Krauskopf (1956) suggested that silica in most

natural water occurs as dispersed silicic-acid molecules

and should be assigned the formula H4 Si04

. The solubility of amorphous silica was found by

Alexander (1957) to increase as the particle size of the

silica decreased. He reported a minimum solubility of

91 ppm for silica in massive form as Si02 at 25°C. The

value given by Greenberg and Price (1957) for solubility of amorphous silica is 108 ppm at 25°C. A

similar value is given by Okamoto, Okura, and Goto

(1957); and White, Brannock, and Murata (1956) found an equilibrium value of about 110 ppm in high-silica

hot-spring waters stored for sufficient time at 25°C

These investigators found that the solubility increased

rapidly with increasing pH above about pH 9.0 because

of the dissociation of the acid. The first dissociation

constant for H^SiO^ was given by Greenberg and Price

(1957) as 10~9 - 77

. Silica also becomes more soluble at temperatures above 25°C.

Van Lier, de Bruyn, and Overbeek (1960) reported

that as much as about 11 ppm quartz was soluble in

water at 25°C and that saturation was attained slowly.

The rate of silica solution also was studied by O'Connor

and Greenberg (1958) and reported to be proportional

to the surface area of solid exposed.

The silicic acid present in quantities above equilibrium values in highly siliceous waters, such as those

represented in table 17, was found by White, Brannock,

and Murata (1956) to polymerize slowly to yield colloidal

suspensions of silica. The rate of polymerization is influenced by pH, temperature, degree of supersaturation, and presence of previously formed colloidal or

crystalline silica.

IRON

The form and amount of iron in solution in ground

water at chemical equilibrium is controlled by the

nature of the iron minerals present, the pH and redox

potential (Eh), and the activity of other ions in the

solution. Graphical representation of these variables

by means of Eh-pH, or stability-field, diagrams clearly

shows the interrelationships. Such diagrams also are

useful in studies of the chemistry of many other

elements that may occur in solution. The stabilityfield diagram was extensively developed and utilized

by Pourbaix (1949) in his studies of corrosion, and has

been extensively applied in geochemistry by Garrels

(1960).

Many of the water analyses in tables 1 to 27 report

iron concentrations of 1 ppm or more. In almost all these waters the iron must be present in the ferrous

form. For an amount this great to be retained in

solution, however, a pH well below 7.0 or a low redox

potential is required. The latter commonly occurs in

ground-water bodies that are not in contact with air. When ground water containing ferrous iron is exposed to

air, oxygen raises the Eh of the solution and the iron is oxidized to the ferric form and precipitated. The

solubility of ferric iron exceeds 1.0 ppm only at a pH

below 3.8 and at a high Eh. The solubilities and rates

of oxidation of iron are affected by complexing with

organic and inorganic ions and by other factors. Studies

by Hem (1959b; 1960a; 1960b; 1961) discuss these

factors in detail. The rate of oxidation of ferrous iron

in aerated water has been studied by Stumm and Lee

(1960; 1961).

CALCIUM, BICARBONATE, CARBONATE, AND pH

Chemical equilibria involving solid carbonate minerals, and dissolved calcium, hydrogen, and bicarbonate

or carbonate ions are very important controls over the

concentration of calcium in ground water. The system

involving calcite may be simply represented

CaC03 +H+^HC03-1 +Ca+2

.

If a gas phase is present, the acitvities of H+1 and

HC03-1 may also be controlled by the partial pressure

of carbon dioxide. Some of the carbon dioxide combines with water to form carbonic acid, which is partly

dissociated in solution. Hutchinson (1957, p. 653-690)

has discussed carbon dioxide-bicarbonate equilibria, in some detail. In most ground waters no gas phase is present. However, some dissolved carbon dioxide and related species are present. The reactions among water, dissolved

materials, and solid minerals control the hydrogen-ion

activity. An important source of dissolved carbon
F4 DATA OF GEOCHEMISTRY

dioxide is the air in soil pores, which is often strongly

enriched in carbon dioxide. In some ground waters,

however, a volcanic or metamorphic source of carbon

dioxide may be important (White, 1957b, p. 1670-1671,

1678); Orfanidi (1957) also has noted the possibility for

metamorphic C02 in certain waters of the Caucasus.

Carbon dioxide may also be produced at depth by

biochemical reduction of sulfate. Hydrogen ions also are available in small quantities

by dissociation of water itself. When pure water is equilibrated with calcite at 25 °C, the pH of the solution is raised to a value between 9.9 and 10 (Garrels,

1960, p. 50), and the calcium content is about 5 ppm.

If water is first allowed to dissolve carbon dioxide by

contact with air and then is equilibrated with calcite

in the absence of a gas phase, Garrels (1960, p. 57)

has calculated that the final calcium content in solution

will be only about 5.6 ppm. Rainwater moving directly to the ground-water reservoir with no opportunity for

further enrichment in dissolved carbon dioxide is thus

only a little more effective as a solvent for calcite than

is pure water. A graphical representation of calcium,

bicarbonate, and pH relationships in solutions at equihbrium with calcite has been published by Hem

(1960c).

Weyl (1958) concluded that under normal conditions

the solution of calcite occurs rapidly enough so that

water in limestone below the water table is always

saturated with calcite. The reverse reaction, precipitation of calcite, is considerably slower. A condition of

equilibrium should, however, exist in most ground

water. Field data that might be used to evaluate

equilibria in ground water are difficult to obtain.

Determinations of pH and perhaps of bicarbonate

must be made in the field when samples are collected,

if they are to represent accurately the conditions in the

aquifer. Practically no data of this type are available.

Analyses in table 6 represent the usual laboratory

determinations made after the samples had been

stored for several days or weeks.

The hydrogen-ion activity of ground water is in- volved in many other chemical equilibria besides those

of carbon' dioxide and carbonates. In extreme examples,

as those in tables 19 and 20, the water may become

strongly acid by solution of gases such as S03 or HC1.

MAGNESIUM

The reactions involved in solution of magnesium from

carbonate minerals are similar to those for solution of

calcite. However, as Garrels, Thompson, and Siever

(1960) have noted, the precipitation of magnesium

carbonate or dolomite from solution is extremely slow

and equilibrium conditions with respect to magnesite or dolomite probably are not to be expected at low

temperature and pressure. Some of the analyses in

table 7 show the approximately equivalent amount of

magnesium and calcium to be expected at saturation

with dolomite. Some precipitation of calcium car- bonate from such solutions, however, appears to occur and leads to a considerable excess of magnesium over

calcium in solution.

VARIETIES OF TONIC SPECIES

The actual forms in which some ions occur in ground

water are still incompletely known. The importance

of ion-pairs or complexes undoubtedly increases as the

total content of dissolved material increases. The

degree of dissociation of dissolved carbon dioxide and

the resulting ionic species is well recognized to be a

function of pH, but the relationship of other anions

to pH is not always recognized. Below a pH of 2, for

example, sulfuric acid is only partly dissociated and

HS04_1 needs to be considered.

The chemistry of major constituents of water is much better understood than is the chemistry of minor

constituents. As a matter of fact, the literature contains almost no information on the minor-element

content of the more dilute ground waters. Although

the large number of water analyses in existence suggests that there is scientific and orderly precision

in the study of chemistry of natural water, actually

much research is needed before the field can be considered as well explored.

SOURCE AND SELECTION OF TABULATED DATA

The analyses in this chapter were obtained from

published reports and from unpublished data in the

files of the U.S. Geological Survey.

Effort has been made to achieve a wide geographic

distribution of analyses, but because many more

waters have been analyzed in some countries than in

others, the distribution is necessarily uneven. Thousands of mineral waters and tens of thousands of

"potable" ground waters have b.een analyzed; selection was made, in part, for geographic distribution, but

in major part was based on geologic environment,

the number of components that were determined, and

the apparent accuracy of the entire analysis to the

limited degree that quality can be judged. Components of special interest that commonly are not

determined are K, Li, NH4 , F, Br, I, N03, and B

(White, 1957b, p. 1661, 1666). Most of these components are not determined in dilute ground waters

but are present in minor yet determinable quantities

in many mineral waters. They are highly soluble in

most chemical environments, and the quantity of each

component that is present in a natural water is determined by the history of the water and the available
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F5

supply of the component. Many mineral waters

have been analyzed for one or two of these components,

but few have been analyzed for most or all of them.

Components such as the alkaline-earth elements

and the heavy metals are of considerable interest, but

the quantities present are much more likely to be

determined by solubility in the particular water rather

than by available supply. Water samples obtained

from wells may contain small amounts of metals, such

as zinc, copper, or iron, dissolved from pump parts of

plumbing. Analyses suspected of being affected by

this type of contamination were rejected, but the effect may not be entirely absent from the tabulated data.

A large proportion of analyses are not accompanied

by satisfactory data on geologic environment of the

waters. Many analyses of mineral waters are published

in chemical or balneological journals without accompanying geological data, but effort was made to determine the geological environments of the samples whose

analyses were selected. In tables 1 to 11, analyses of waters from each rock

type are given numerically in order of increasing

dissolved matter, because, in general, the dilute waters

are less likely to be affected by contamination with

saline waters of nonmeteoric origin. In tables 12 to

27, analyses are arranged geographically.

UNITS AND TERMINOLOGY

Virtually all the analytical data are reported in the

standard form of the U.S. Geological Survey. Concentrations of components in the waters have been

reported in various publications in a wide variety of

forms and chemical combinations; in this chapter all are expressed as parts per million, which for waters

of or near unit density are also equivalent to milligrams

per liter. Constituents that are present largely or

entirely in dissociated form are reported also as equivalents per million (epm, or milligram equivalents

per kilogram) computed from parts per million and

combining weights of the ions. Some elements, such as Si, B, As, P, and Al, have

been reported in several different ionic and molecular

species by different analysts. These are uniformly

reported here as Si02 , B, As, P04, and Al; equivalents

per million are not calculated for these components

or for Fe and some other metals, except in acid waters.

Sulfide is reported as H2S, except for a very few analyses

where both H2S and HS"1 were originally reported or where the water is very alkaline and sulfide ion is probably dominant. A minor element that has been

determined in only a few analyses of a table is not shown

in the tabulated data but is mentioned in the explanation

of the table. Specific conductance is expressed as micromhos at

a standard temperature of 25° C. A mho is a unit

of electrical conductance and is the reciprocal of ohm.

"Specific" here implies the conductance of a 1-cm

cube of the solution; the ability of a water to conduct

electricity is increased as the concentration of dissociated

ions increases, but there is no simple relationship

between specific conductance and dissolved solids in

parts per milli on- Uranium is reported in micrograms

per liter (or parts per thousand million in waters of unit

density) and radioactivity is reported in micromicrocuries per liter (curies X 10"12 per 1). In some published analyses, as many as six significant

figures have been reported. These have been arbitrarily

rounded in the following way: less than 1 ppm, 1 or 2

significant figures; 1 to 99 ppm, 2 significant figures;

and over 100 ppm, 3 significant figures. All values for

equivalents per million are reported to comparably significant figures but are not reported for more than two

decimal places. Some published analyses show precise

chemical balance of anions and cations; presumably one component (generally Na) has been calculated by dif- ference. The equivalents per million reported here as

significant figures generally do not balance exactly.

Rates of discharge of springs are stated in U.S. gallons

per minute (gpm). One gpm equals 0.83311 Imp. gallons per minute, 3.7854 liters per minute, and 0.002228

cubic feet per second.

Stratigraphic nomenclature used is that of the published and unpublished sources and does not necessarily

conform to that of the U.S. Geological Survey.

WATERS OF LOW MINERAL CONTENT ASSOCIATED

WITH COMMON ROCK TYPES

The analyses of tables 1 to 11 were selected from

about 1,200 analyses. Most of the water samples would

be considered potable, with dissolved matter of less than

1,000 ppm. These dilute waters were selected largely

from environments in which the waters were most likely to be atmospheric precipitation that was then influ- enced primarily by reactions with the rocks in which

they are found (including associated soil zones).

Dilute waters are relatively scarce in some rocks,

particularly in fine-grained sedimentary rocks such as

siltstones and shales. (See table 5.) Most sedimentary

rocks were deposited in a saline environment; extensive

flushing or displacement is necessary to remove the

highly soluble matter retained from such an environment. However, most of the rocks that are highly

productive sources of ground water were deposited in

nonmarine environments.

WATERS FROM IGNEOUS TERRANES

GRANITE, BHYOLTTE, AND SIMHAB BOCK TYPES

Silicic igneous rocks generally yield only small supplies of water, except where extensively jointed or brec-
F6 DATA OF GEOCHEMISTRY

ciated. Nevertheless, these rocks are utilized in many

areas where better sources are lacking.

Ground waters from silicic igneous rocks (table 1) generally are relatively low in mineral content. The

dominant ions are generally Na+ and HC03~; Si02 is generally very high for cold dilute waters and fluoride

is relatively high. Calcium, magnesium, and pH are

generally relatively low (table 1)

.

Such characteristics should be expected of meteoric

waters in contact with silicic igneous rocks, which consist dominantly of chemically resistant quartz and

sodium and potassium feldspars. The anomalously low

indicated ratios of potassium to sodium relative to the

ratios in other igneous rocks are surprising, because this

group is normally high in potassium. The rocks of this

group are also relatively high in lithium and boron, but

these two elements have seldom been determined in

dilute waters. In table 1, the sulfate of analysis 14, the chloride of

analyses 11, 13, and 15, and probably the fluoride of

analyses 13 and 14 are all high and require special explanations that are not made here.

GABBEO, BASALT, AND ULTRAMAFIC ROCKS Although most igneous rocks do not yield large quantities of ground water, some favorably situated permeable basalts yield enormous quantities.

The source rocks of the waters of analyses in table 2

consist dominantly of ferromagnesian minerals, with or without calcic plagioclase. All these minerals are less stable and more subject to chemical attack than the

minerals of silicic rocks.

As expected, the waters of the group generally have

high ratios of Ca/Na and Mg/Ca; the magnesium content of peridotite and serpentine is particularly high,

and the magnesium content of waters from gabbro and

basalt is nearly always higher than in waters from silicic igneous rocks. Although mafic rocks contain little or no

quartz and are lower in total silica than felsic rocks, the

chemical instability of the minerals accounts for rela- tively high content of Si02 in associated waters. Most

of the waters are low in fluoride; although no data are

available, further study may show that these waters are generally low in lithium and perhaps in boron relative to waters of silicic igneous rocks.

Table 2 shows that where pH and probably Eh

(oxidation potential) are low, iron and manganese are

relatively high (analyses 1 and 2) . The high sulfate of

analysis 2 suggests oxidation of sulfides or sulfate from some external source; much of the chloride of the waters

of analyses 10, 15, and 16 may be from external sources.

ANDESITE, DIORITE, AND SYENITE The waters given in table 3 are associated with rocks

that are, in general, intermediate between granite and

basalt in composition. Many of the ratios and contents, however, are not between the medians for granite

and basalt, probably because of the small number of

samples and lack of rigid statistical control and perhaps

also because minor analytical errors can influence the

ratios strongly when the waters are very dilute. The high sulfate content of analysis 3 suggests

sulfate from some external source. WATERS FROM SEDIMENTARY TERRANES

SANDSTONE, ARKOSE, AND GRAYWACKE

Sandstone beds are widespread and are important

aquifers throughout the world. Rocks of this group

range in chemical composition from almost pure silica to rocks that are very similar chemically to granite,

andesite, and basalt. The lithologic characters and

chemical compositions of the rocks associated with

waters given in table 4 have not been described suffi- ciently to warrant further subdivision.

The ratios of Ca/Na, K/Na, HC03/C1, and S04/C1

are commonly a little higher than for most waters from

igneous rocks, but the content of Si02 is generally less. Ground waters containing more than 1,000 ppm

dissolved matter are relatively common in sandstone,

especially at depths of more than several hundred feet. Many waters from sandstones contain dissolved matter

clearly not derived from the clastic grains of the

enclosing rocks, for example, the very high fluoride

content (2 to 9 ppm) commonly reported in waters

from the Dakota Sandstone (Cretaceous) of North

Dakota and South Dakota.

A few waters from sandstone contain notable amounts

of iron and are probably low in Eh; some of these

waters also contain appreciable manganese.

SLtTSTONE, ciay, and shaie

Siltstone, clay, and shale are fine grained and, except

for the more brittle jointed varieties, are very low in

permeability. They are poor sources of water, but

most are in areas where more productive sources are not

available.

The bulk of the fine-grained sediments of the world were deposited in saline environments. Soluble components are likely to be retained as adsorbed ions on

clay minerals or in interstitial saline water that was

never completely removed by flushing because of low

permeability of the rocks. One of the outstanding

characteristics of this group (table 5) is the scarcity of

waters with reported sums of less than 1,000 ppm.

The less mineralized waters in table 5 are generally

relatively low in the ratios of Ca/Na, HCO3/CI, and

F/Cl; the ratio of Mg/Ca is relatively high.

Many marine shales and muds are high in boron and

iodine (White, 1957b, p. 1668, 1671; Degens and others,

1957) ; nonmarine shales appear to be low in boron and
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F7

are probably also low in iodine; more attention should

be given to these minor elements in waters of low

mineral content, because these minor elements may

reflect differences in the environments of deposition of

the sedimentary rocks.

Many of the more saline waters given in table 5 are high in chloride, which is probably residual from the

depositional environment. The low sulfate content of

analyses 13 to 15 is probably related to organic content

and reducing environment in the rocks. The relatively

high bicarbonate content of these waters may be due to sulfate-reducing bacteria that have utilized the oxygen

of sulfate to oxidize some of the organic carbon. Experimental studies by Foster (1950) suggest, however,

that the presence of sulfate is not a necessary condition

;

she suggests that the high sodium content may be due

to ion exchange of calcium with sodium from clay

material and that carbonaceous material is the source

of C02 for the waters of very high bicarbonate content. Other waters are relatively high in sulfate, some are

acid and contain moderately high amounts of iron and

aluminum (analyses 2 and 18); these characteristics are probably related to oxidation of pyrite in organic

shales. Other waters are nearly neutral but contain

notable quantities of iron and manganese (analyses 5, 11, and 16), probably because of moderately reducing

environments.

Although commonly ascribed to pollution, the high

nitrate content of some waters from shale (analyses 3,

8, 9, and, especially, 10) may also result from oxidation

of NEU in organic matter and in exchange positions in

clay minerals in sediments rich in organic matter.

LIMESTONE Most limestones are dense, hard rocks that carry

water only in fractures; some limestones, however, contain large solution channels and are highly productive.

Perhaps the most productive limestones, however, are porous reef structures or other accumulations of shells where original porosity has commonly been increased

by solution. In addition to CaC03 , many limestones also contain

silica, clay minerals, dolomite, anhydrite, or gypsum.

All the analyses of table 6 demonstrate the influence of some other minerals in addition to calcite. Dolomite, perhaps as a minor component, has undoubtedly influenced

the composition of the water of analysis 9, and, to a

lesser extent, many of the others. The water of analysis 14 seems to contain dissolved gypsum or anhydrite.

The quantity of alkaline-earth carbonate minerals

that can be dissolved by ground water is controlled

by the abundance of C02 and by carbonate equilibria.

See reports by Hutchinson (1957, p. 653-690) and

Garrels (1960, p. 43-60) for recent discussions that can

be applied to many ground-water problems. The

amounts of calcium and bicarbonate and the pH

values suggest that all waters given in table 6 had

sources of C02 capable of supplying larger amounts

than the atmosphere. The partial pressure of C02 in

the atmosphere is 0.00033 (Hutchinson, 1957, p. 654-655). Other sources of C02 for ground waters

are organic activity in the soil zone and igneous or metamorphic processes at depth (White, 1957a; 1957b).

Many waters from limestone contain more nitrate

than is characteristic of waters from igneous rocks.

Although local pollution is a possible source of some

of the nitrate, the oxidation of minerals or other substances containing ammonia should also be considered.

Another possibility is that NH4 may have been a component of some of the waters when collected, but

became oxidized and was determined as nitrate.

SOLOMITE Dolomite is generally similar to limestone in its water-bearing properties. Some types of dolomite are highly permeable and are economically important

sources of water. The weight ratio of magnesium to calcium in pure

dolomite is 0.61 (ratio of equivalents, 1.0). Meteoric

water that has been in contact only with pure dolomite

should have these ratios if the dolomite dissolved

nonselectively and if no calcite has been precipitated.

, The ratio of Mg/Ca in 3 of the 6 analyses in table 7

is very close to 0.61; the ratio of analysis 2 is low, and

the ratios of analyses 3 and 5 are high. Some other

high-magnesium mineral may be present, or some CaC03 may have been precipitated from the two waters

having high ratios. The water from Fort Recovery, Ohio (analysis 6),

contains very high sulfate and relatively high magnesium. The origin of the sulfate is not clear.

MISCELLANEOUS SEDIMENTARY ROCKS Table 8 contains analyses of waters from some of the

less common types of sedimentary rocks.

In general, the major chemical components of each

rock type have low solubility values and have not

markedly affected the chemical composition of the

associated water. The outstanding exception is the

high content of CaS04 in water from gypsum in analysis

5 (for analyses of other waters from associated Permian

evaporites, see table 27). The very high sulfate content in the water of analysis 4 may be a result of oxidation of pyrite in the associated lignite.

The water of a well 200 feet deep, a short distance

east of the city of Hot Springs, Ark. (analysis 2), is slightly thermal and has with little doubt been in contact with rocks other than chert. This water, as well
F8 DATA OF GEOCHEMISTRY

as some others given in table 8, probably has a rela- tively low Eh, permitting significant iron and manganese to be in solution.

WATERS FROM MBTAMOBPHIC TERRANES

QUABTZITE

Although the permeability and porosity of quartzite are generally very low, this type of rock may be a productive source of water if sufficiently brecciated.

It is chemically similar to silica-rich sandstone (see

tables 4 and 9).

Many waters from quartzite are low in Si02 and total

dissolved matter and have a high ratio of K/Na; pH

is commonly low, probably because of the scarcity of

unstable minerals to react with dissolved C02

. MAEBLE Marble is the coarsely crystalline metamorphic

equivalent of limestone. Two analyses of waters from

marble (table 9) are very similar to those from limestone

(table 6). Both waters are in equilibrium with C02 pressures that are considerably higher than the C02 pressure of the atmosphere (Hutchinson, 1957, p. 654-

671). As in most limestone waters, excess C02 probably

has been supplied from the soil.

SLATE, SCHIST, AND GNEISS In general, metamorphic rocks yield only small

supplies of water, because their permeability is low.

Analyses of waters from several examples of metamorphosed shale and impure sandstone are included in

table 10. In many respects the waters from these metamorphosed rocks are similar to waters from shale and

siltstone (table 5). Water from the metamorphic

rocks, however, is commonly lower in mineral content

and generally the ratio of Ca/Na is more than unity.

The differences are best explained by extensive compaction and decrease of porosity of the rocks before

and during metamorphism; interstitial saline water of

the original environment has largely been forced out,

and clay minerals of high ion-exchange capacity have

been reconstituted to micas and anhydrous minerals of

very low exchange capacity.

The very low content of dissolved matter of water

from a metamorphosed iron-formation in Brazil (table

10, analysis 14) is noteworthy. The water is from a humid region, and the rocks are highly resistant to chemical attack. For comparison, see analysis 1 of

table 8 from unmetamorphosed iron-formation of

Minnesota.

Waters of analyses 12, 13, and 15 of table 10 are

relatively high in chloride, and 13 and 15 are also high

in sulfate; both components probably came from sources other than the enclosing rocks.

WATERS FROM UNCONSOLIDATED SAND AND GRAVEL.

Unconsolidated sand and gravel are the most important sources of ground-water supply. They include

alluvium of normal streams; glaciofluvial deposits,

which, of course, can be considered a type of alluvium;

and extensive marine and littoral strata of the coastal

plains. The water most readily recoverable from unconsolidated deposits generally occurs in beds of gravel

and sand accumulated and sorted through the action

of streams. The mineralogic composition of unconsolidated sand

and gravel can be correlated in some places with the

composition of the source rock. Especially in arid

regions, the particles that make up these deposits are

likely to be relatively unweathered fragments of the

original rock.

The ratios and contents of the analyses given in

table 11 are in general similar to those of other types

as might be expected. The eight waters from alluvium

of dominantly igneous origin (table 11, analyses 1, 2, 3, 6, 7, 10, and 18) are mostly similar to waters from

igneous rocks, having relatively low total dissolved

matter and relatively high silica content. Most of the other analyses are of waters from

alluvium derived from sedimentary rocks of many

types. Total dissolved matter is commonly high,

which is, in part, due to the large surface area per unit

volume that is available for chemical reactions. This

factor is particularly apparent in analyses 8, 12, and

16, which are of waters from relatively unweathered

glacial sands and gravels in the north-central United

States. Ground waters from alluvium are hydrologically and

chemically closely related to surface waters of the same

drainage basin. A high content of dissolved matter can be present in such interrelated systems for any of the

following reasons: (1) salts may be contributed from

connate water or from salt beds in the basin (analyses

11, 19, and 20); (2) return flow from irrigation may in- troduce soluble matter leached from cultivated lands

(analyses 11, 17, 19, and 20), possibly after several

cycles of reuse; (3) in arid climates, evaporation and

transpiration may concentrate soluble matter in the

remaining water (analyses 14 and 15) and the ground

water of alluviated valleys may have undergone several

cycles of exposure to evaporation and of return as underflow into sediments (analysis 14); (4) activities of

man provide salts in industrial wastes and in other

forms. The high nitrate content in the waters of analyses 3, 5, 9, 13, 16, 18, 19, and 20 of table 11 may

indicate pollution or direct aerobic decomposition of

nitrogenous material, but other sources of these components, such as oxidation of NH4 to nitrate, should be

considered.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F9

WATEBS THAT MAY BE, IN PABT, CONNATE

OEG-FEELD WATERS

The existence of connate or "fossil" water has been

questioned by Chebotarev (1955) and others, but most

geologists assume that many saline brines probably

contain some water that is not greatly different in age

from the enclosing rocks (White, 1957b, p. 1661-1678).

Most connate waters probably consist of connate ocean

water associated with marine sediments. Several waters

that may be, in part, connate and are associated with

marine and nonmarine evaporite deposits are included

in table 27 (see in particular analyses 1, 2, and 7). Near-surface marine sedimentary rocks in depositional basins and in coastal plains ordinarily have been

flushed extensively by meteoric water. Most of the

waters that have been collected from considerable depth

in sedimentary basins, however, are saline and are probably connate. Nearly all these saline waters that have

been analyzed for minor and major components were

obtained from oil fields, but analyses 7 and 8 of table 13

are exceptions. These waters have a wide range in the

proportions of individual components of dissolved matter. In most oil-field brines (see tables 12 and 13), the

dominant anion is chloride (Chebotarev, 1955, p. 159)

but in a few, bicarbonate or sulfate (table 14) exceeds

chloride by weight.

In the chloride waters, sodium is, with rare exception,

the dominant cation, but calcium very commonly is present in larger proportions than in sea water. Chloride

waters are here divided into two major subtypes. In

one, sodium is greatly dominant over calcium; in the

other, calcium is relatively abundant. In tables 12 and

13, the dividing line is arbitrarily considered to be

Ca=0.1 Na (by weight).

Some oil-field waters contain so little dissolved matter

(Crawford, 1940; 1942; 1949, p. 210) that they are

clearly almost entirely of meteoric origin. Other oil- field waters are very saline*—commonly 5 to 10 times as

saline as sea water—and their origin is a major problem

that has long been debated (Mills and Wells, 1919;

W. L. Russell, 1933; de Sitter, 1947; Chebotarev, 1955;

White, 1957b). Most of these very saline waters are

relatively high in calcium and several examples are included in table 13. A few high-calcium waters are lower

in salinity than sea water (table 13, analyses 2 and 5)

and probably result from dilution of high-density brines.

In contrast, the brines that are low in calcium generally

are similar in salinity to sea water or are lower in mineral

content, but the waters of analyses 4, 5, 9, and 10 given

in table 12 are exceptions.

Analyses 7 and 8 of table 13 are of Michigan brines

exploited by the Dow Chemical Co. for dissolved salts. These brines are similar to waters associated with

small oil pools in the same formations in other parts

of the Michigan basin. They are not known to be

associated with crystalline-salt deposits, and their

high ratios of Br/CI are indeed very good evidence

against influence of precipitated NaCl; Br is accepted

only to a minor extent in the crystal lattice of NaCl and

is concentrated in residual brines. (See chapter Y.)

Most of the waters given in table 12 are from Tertiary rocks, but some are from rocks as old as Triassic;

the water of analysis 10 may be from Permian rocks.

In contrast, brines high in calcium are likely to be from

Paleozoic and Mesozoic rocks, but the waters of analyses

1, 2, 3, and 12 of table 13 are from lower Tertiary rocks.

The oil-field brines high in sodium and chloride are commonly characterized by moderately high dissolved matter and NH4 , high ratio of I/O, and low

ratios of K/Na, Li/Na, and S04/C1 (tables 12 and 29).

The chloride brines high in calcium are generally

high in total dissolved matter and moderately high

in NH4 (tables 13 and 29). The ratio of Br/CI in

this group is perhaps the highest of all natural waters,

although remarkably slight variations of Br/CI are

indicated for the different types included in table 29. Ratios of Li/Na, HC03/C1, S04/C1, and F/Cl are very

low in the brines high in calcium, and K/Na, I/Cl,

and B/Cl are moderately low. Barium is generally

high where sulfate is low or absent; silica is near the

minimum for all natural ground waters. The characteristics and minor-element contents of

sulfate and bicarbonate waters of table 14 are not sufficiently well known to distinguish them clearly from

other waters that are high in sulfate and bicarbonate.

Their origin, interrelationships, and minor constituents

need further study. Chebotarev (1955, p. 159) has

shown statistically that the average depth of bicarbonate waters in oil pools is about 2,300 feet and of

sulfate waters, 1,700 feet. These waters doubtless

grade upward into ground waters that are only moderately high in sulfate and bicarbonate.

SPRINQ WATERS SIMILAR E* COMPOSITION TO OEL-FEELD

WATERS

A considerable number of cold to moderately thermal

spring waters of relatively high salinity have compositions that are similar to oil-field brines high in

sodium and chloride. The chemical characteristics

of these spring waters, other than high salinity re- lative to that of other spring waters of similar temperature, include, in general, low sulfate and silica,

moderately high combined nitrogen, low ratios of

Li/Na and K/Na, and a high ratio of I/Cl (see tables

12, 15, and 29). The waters of table 15 generally are higher in bicarbonate, boron, and probably, sulfide

than are those of table 12. Oil-field brines, however,

seldom have been analyzed for sulfide and lithium

and not ordinarily for boron and combined nitrogen.
F10 DATA OF GEOCHEMISTRY

Other spring waters are chemically very similar to

oil-field brines high in calcium and chloride. (See

tables 13, 16, and 29.) A major criterion for separating

the waters of analyses given in tables 15 and 16 and in tables 12 and 13 is the weight ratio of Ca/Na; the

separation is here made at 0.1. The high sulfate

content in the waters of some analyses in table 16

suggests direct solution of CaS04 by water that may

have been low in calcium. For several other waters

given in table 16, waters high in sodium, chloride, and

C02 may have come in contact with limestone, dissolving CaC03 and increasing the ratio of Ca/Na.

All the spring waters given in table 15 and many of

those in table 16 are from rocks whose geologic en- vironments seem from available data to be compatible

with a connate origin for the water. The spring water

from London, Oreg. (analysis 1), is, however, from

nonmarine Eocene tuffs and basalts; that from

Wiesbaden, Germany (analysis 6) , is from pre-Tertiary

mica gneiss; that from Thermopotamos, Greece

(analysis 7), is from schist of Devonian age; that from

Trompsberg, Union of South Africa (analysis 8), is from norite of Precambrian age; that from Tiberias,

Israel (analysis 10), appears to be from Tertiary(?)

basalt; that from Neshkin, U.S.S.R. (analysis 13), is from Silurian crystalline schist; and that from Arima,

Japan (analysis 14), is from Tertiary rhyolite near

granite. At least some of these waters are probably

not connate, and others may have migrated from rocks

of earlier association, as suggested by Kent (1951) for

the Trompsberg water; extensive exchange of sodium

for calcium from intermediate and basis igneous rocks

is indicated. The waters of analyses 1 and 14 are moderately low in ratios of Br/CI, and analyses 6, 7,

8, and 9 are notably low, suggesting that these waters

may indeed not be connate. Further study is obviously

needed.

Many spring waters are similar to the bicarbonate and

sulfate waters of table 14 that are associated with

petroleum. More study is needed on the origin of

oil-field waters and more analytical work should be

done on the minor components.

WATERS THAT MAY BE, IN PART, MAGMATIC

It is clear that magmatic waters cannot be sampled

directly at their sources. Waters that are associated

with especially high temperatures and heat flow and

that are in areas of recent or active volcanism are of

great interest, because they may contain at least some

volcanic or magmatic water (White, 1957a). All

students of the problem agree that most of the water

discharged at the surface in thermal areas is probably

meteoric in origin but that a part may be magmatic.

Possible origins of the greatly different types of water

that are found in volcanic environments have been

discussed by Allen and Day (1935), Barth (1950), and

others and have been reviewed recently by White

(1957a) and Ivanov (1958a; 1958b). There is still much

disagreement in regard to the origin of the different

types.

Waters that are dominated by sodium, chloride, and

bicarbonate are shown in tables 17 and 18. All theories

of the origin of geysers require not only high temperatures at the surface but also high geothermai gradients

from the surface to considerable depths: wherever wells

have been drilled in geyser areas, temperatures considerably above the boiling points at the land surface

have been found. The chloride in waters of geyser areas, therefore, is very likely to be of volcanic origin. However, any ground water that is heated sufficiently in a

favorable environment may erupt as a geyser. The "Seawater Geyser" of Reykjanes, Iceland, for example

(table 17, no. 8), has erupted as a true geyser (Barth,

1950, p. 23). Because this water is similar in composition to many of the waters given in tables 13 and 16,

it is probably heated connate water rasher than direct

inflow of ocean water, as suggested by Barth, or

volcanic water. Most geyser waters (tables 17 and 29) are very high

in silica and generally high in pH; the ratio of Li/Na

is very high and B/Cl is moderately high. These waters

are generally very low in combined nitrogen and,

for mineral waters, are low also in total dissolved matter;

the ratios of Ca/Na, Mg/Ca, and I/Cl are commonly

near the minimum for natural waters, and Br/CI may

be significantly lower than in average crustal matter.

Some of the waters of table 18 may be, in part, connate; in areas of lower heat flow than in geyser areas, hot volcanic emanations are not so necessary to explain

the anomaly and, therefore, the possibility of chloride

from nonvolcanic sources may be a little greater.

Water from Kuan-Tsu-Ling spring in northern Taiwan

(table 18, no. 8), for example, has many of the chemical

characteristics of water that may be connate or, possibly, metamorphic in origin (see tables 12, 13, 22,

and 29); bicarbonate, boron, and the ratio of I/Cl are

relatively high, and silica, sulfate, and the ratio of

Li/Na are relatively low.

The median mineral matter and ratios of the analyses

of table 18 (see table 29) are, in part, similar to those

of geyser waters (tables 17 and 29) and, in part, to possible connate waters (tables 12, 15, and 29).

Many of the acid sulfate-chloride waters of table 19

are very closely associated with active or recent volcanism. All gradations exist between acid springs,

large spring pools, and crater lakes; superheated

fumaroles commonly are found in the vicinity. Possible origins of these unusual waters have been reviewed
CHEMICAL COMPOSITION OF SUBSURFACE WATERS Fll

by White (1957a, p. 1647-1649). Their chemical

characteristics (tables 19 and 29) are clearly derived,

in part, from volcanic emanations and, at least in some

places, by vigorous acid attack of associated rocks.

The cation ratios are strongly influenced by associated

rocks except, perhaps, the ratio of Li/Na, which may

reflect a high content of lithium in certain volcanic

emanations. Other outstanding characteristics of most

waters of this group are very high contents of silica and

of total dissolved matter and possibly low ratios of

Br/CI and I/Cl.

Acid sulfate waters (low in chloride) may also originate in several different ways (see Allen and Day,

1935, p. 65, 100-125, 393-448; Barth, 1950, p. 43;

White, 1957a, p. 1651-1652). Most geologists agree, however, that one common origin involves partial con- densation of vapors containing H2S and the reaction

of sulfide, water, and atmospheric oxygen to form sul- furic acid. The cation ratios of these acid waters are influenced greatly by the associated rocks (tables 20

and 29). Ammonium is very high in some waters,

perhaps because of selective concentration of small

amounts of NH3 from the gases, due to low volatility

in acid water. Sulfate is by far the dominant anion;

and fluoride and boron, according to meager data, are somewhat high relative to chloride ; silica and the ratios

of Mg/Ca and K/Na are commonly high.

High-temperature waters high in bicarbonate and

sulfate have been recognized in only a few volcanic

areas, where they appear to be related to condensation

of steam containing C02 and H2S in ground water,

commonly below the surface (White, 1957a, p. 1649).

The ratios of HC03/C1, S04/C1, F/Cl, and B/Cl may be

near the maximum for natural waters, but total dis- solved matter and combined nitrogen may be relatively

low.

WATERS THAT MAY BE, IN PART, METAMORPHIC

Metamorphic water has been defined (White, 1957b,

p. 1662) as water that is or has been associated with

rocks during their metamorphism and is probably

derived largely from hydrous minerals during their

reconstitution to anhydrous minerals.

Many thermal springs and mineral waters have

characteristics that do not clearly indicate any of the

groups previously considered. One type that may

warrant special attention is characterized by high

concentrations of sodium, bicarbonate, and boron and

by relatively low chloride (see tables 22 and 29).

Other similar waters associated with California quicksilver deposits are included in table 23 (analyses 1 to 3).

White (1957b, p. 1678-1679) has suggested that these

waters may be driven off from hydrous minerals of

sedimentary rocks that are being progressively metamorphosed after interstitial connate water high in

chloride has been largely driven off by compaction of

the sediments. The group as a whole has, of course, high ratios of HC03 /C1 and B/Cl, because these ratios were the criteria for selection. Other characteristics are relatively low temperatures; and, in most of the

analyses, high ratios of I/Cl and low ratios of Li/Na

and K/Na. These characteristics suggest a close

relationship to possible connate waters (tables 12 and

15) and are not similar to those of waters most likely to contain a volcanic component (tables 17 and 19).

OTHER SPECIAL GROUPS

THERMAL WATERS ASSOCIATED WITH EPITHBRMAL

MINERAL, DEPOSITS

Most mineral deposits were formed milli ons of years

ago and probably were related to hydrothermal activity

that has long since ceased. In contrast, some epithermal mineral deposits may have formed so recently

that a study of associated waters may throw light on

their origin and on the geochemistry of ore transport

and deposition. The association of thermal springs

with epithermal ore deposits has been reviewed recently

by Schmitt (1950) and White (1955a). The evidence

must always be examined with caution, because significant changes in nature of the discharging water may

have occurred since the ore minerals were deposited;

it is usually difficult to prove conclusively that the ore minerals are still being deposited from existing waters. Table 23 includes six analyses of thermal waters

occurring in or near quicksilver deposits. Other waters

associated with no'table quicksilver deposits are those

from the thermal springs of the Elgin quicksilver mine,

3 miles northwest of Wilbur Springs, Calif, (table 15,

analysis 2), which are very similar in composition to the

waters given in table 23 (White, 1955a, p. 130-131); the

brine from the Cymric oil-field, Calif, (table 12, no. 2; see also Stockman, 1947); water from Skaggs Springs,

Sonoma County, Calif. (Everhart, 1950, p. 385-394;

White, 1955a, p. 125; 1957b, p. 1676-1679); and water

from Steamboat Springs, Nev. (table 17, no. 3).

Waters associated with quicksilver deposits (tables 23

and 29) tend to be relatively high in total combined

nitrogen and in the ratios of Mg/Ca, HC03/C1, B/Cl,

and I/Cl, but the ratios of Ca/Na, K/Na, and Li/Na are

relatively low. The median pH of 7 should be noted

because of the generally held belief that mercury is transported in alkaline waters. The waters appear to be closely related to those given in tables 12, 15, and 22. Of the analyses given in table 23, those of waters from

the Abbott, Sulphur Bank, and Valley mines could have

been included in table 22. The water of Steamboat

Springs, Nev., is the only one associated with a notable

quicksilver deposit that is also convincingly related to volcanism. It should be mentioned that the spring
F12 DATA OF GEOCHEMISTRY

waters at Sulphur Bank, Calif., and Ngawha, NewZealand (table 23, nos. 1 and 6) are closely associated

with Quaternary volcanic rocks, but these thermal waters are not clearly volcanic in origin.

Table 23 also includes an analysis (No. 15) of water

from an epithermal silver-gold deposit; one analysis

(No. 14) is of water from a spring depositing a notable

amount of barite, six (Nos. 7 to 12) are from manganesedepositing springs, and two (Nos. 12 and 13) are from

springs that have deposited fluorite-bearing travertine.

These waters are not convincingly similar to any of the

types included in tables 12 to 22. The water of Steamboat Springs, Nev. (table 17),

mentioned previously, is depositing considerable stibnite and arsenic and some gold and silver (Lindgren,

1906; Jones, 1912; Gianella, 1939; Brannock and others,

1948; p. 222-225; White, 1955a, p. 110-113). The

water of Crabtree Springs, Calif, (table 22, analysis

3) contains appreciable amounts of arsenic and emerges

from serpentine replaced by opal containing veinlets of

realgar and marcasite. The iron phosphate deposits of

Tjiater Springs, Java (table 19, analysis 11), contain

about 2 percent arsenic.

In addition to the Peitou Spring, Taiwan, where

deposition of lead sulfate has been reported (table 23,

analysis 16), hokutolite, a lead-bearing barite, has also been identified at Shibukuro Springs, Honshu, Japan

(Miura, 1938; 1939a; 1939b). A surprisingly high

content of lead (8.3 ppm) has also been reported from

Kuan-Tsu-Ling Spring in northern Taiwan (table 18,

analysis 8). This spring, although associated with

Pleistocene volcanic rocks, has many of the chemical

characteristics of waters included in tables 12, 15, and

22. NONTHERMAL SALINE AND ACID MINE WATERS

The composition of many nonthermal mine waters is of interest. Acid waters in pyritic deposits (table 24,

analyses 4 to 8) are likely to be meteoric waters that

have been acidified by oxidation of pyrite. Such acid

waters commonly contain relatively large quantitites

of heavy metals dissolved from adjacent rocks and ore

deposits.

Other mineral waters from deep mines are not acid

and are otherwise very different in composition from

acid or normal meteoric waters. Some are very saline

and their compositions may have resulted from contact

with the wallrocks. Another distinct possibility is that

the ore-bearing solutions or other postore waters of

high mineral content were trapped and have not yet

been flushed completely by meteoric water. Analyses 2 and 3 of table 24 are similar in nearly all respects to those of the high-calcium brines of many oil fields (table 13). The analysis of water from the Calumet and Hecla copper mine (No. 2) is very similar to

an earlier analysis from the nearby Quincy mine, re- ported to contain about 5 ppm of nickel and 14 ppm of

copper (Lane, 1908, p. 110).

Saline water similarly dominated greatly by calcium

chloride has been identified in the Sturgeon Kiver gold

mines of Canada (Bruce, 1941, p. 25-29; the salinity is 15.5 percent and the ratio of Ca/Na is 4.1). A very

saline sodium chloride water was found in the Morro

Velho mine of Minas Gerais, Brazil (written communication, D. W. J. Grey to Earl Ingerson). The water came

from a vug lined with albite, calcite, ankerite, and

quartz at a depth of 7,126 feet. A partial analysis

showed Ca, 3,900 ppm; Mg, 1,200 ppm; Na, 46,400

ppm; CI, 81,900 ppm; carbonates and sulfates, nil. Wallrocks are believed to be basic lava flows or spilites

metamorphosed to carbonate schist. Analysis 1 of table 24 is of a mine water of low mineral

content that is similar in many aspects to meteoric

water but that is unusually high in bicarbonate.

OTHER NONTHERMAL ACH) MINERAL WATERS

Waters of analyses 9 and 10 included in table 24 are examples of nonthermal acid waters that are probably

associated with oxidation of pyrite or native sulfur. They are similar to those of analyses 4 to 8 but are less closely associated with mines. Other similar nonthermal acid spring waters in Japan have been analyzed

(Morimoto, 1954, p. 38, 93, 361, 367, 595-596, and 627-

628).

SPRINGS WITH LARGE SPRING DEPOSITS

Most springs discharge at the surface without depositing significant amounts of mineral matter. However, some spring waters are unstable at atmospheric

pressure and ordinary air temperatures and may deposit considerable amounts of solid material near their

orifices. Opaline sinter is the characteristic deposit of most of

the geyser waters given in table 17. However, the

quantity is relatively minor at Morgan Springs, Calif,

(analysis 5). Sinter probably is not deposited ordinarily from waters that contain less than 200 ppm of

silica (White, Brannock, and Murata, 1956).

Sinter was deposited rapidly from about 1920 to 1950

at Roosevelt Springs, Utah (table 18, analysis 3), but

in recent years the flow of water from the principal

spring has become very small and deposition of sinter

is negligible. Travertine deposits (CaC03 ) of the

Lysuhdll Springs of Iceland (table 25, analysis 5) lie on

earlier and more extensive deposits of sinter. Calcite or aragonite travertine is considerably more common as a spring deposit than is sinter. The deposits of all the springs given in table 25, except at Lysuh611, Iceland (analysis 5), are very large as they

are measurable in millions of tons. Urbain (1953) has
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F13

estimated that 2 tons of travertine per day is deposited

at Meskoutiae Springs, Algeria (analysis 6).

Analyses of waters from other springs associated with

notable travertine deposits are at Doughty, Colo,

(table 23, analysis 14); Abraham, Utah (table 23,

analysis 8) ; Poncha, Colo, (table 23, analysis 12) ; Ojo

Caliente, N. Mex. (table 23, analysis 13); Tolenas,

Calif, (table 15, analysis 3); Ain Djebel, Tunisia (table

16, analysis 9); and Saratoga, N.Y. (table 16,

analysis 4). A small part of the waters of some of the springs that

deposit travertine may be of volcanic origin but diluted

extensively with meteoric water (probably table 25, no. 3). The composition of such waters suggests

contact with limestone and perhaps with gypsiferous

sedimentary rocks, probably at relatively low temperatures (White, 1957a, p. 1652-1653). Other springs

that deposit travertine may be unrelated to volcanism

and have a source of C02 other than the atmosphere

(see Introduction). All springs that deposit carbonate

contain more C02 in solution at depth than can be re- tained at pressure and temperatures at the surface.

As the pressure decreases, C02 is evolved and the pH

increases, shifting the carbonate equilibria and causing

precipitation of CaC03

. The two analyses of waters

from Keene Wonder Springs in Death Valley, Calif,

(table 25, analyses 1 and 2), illustrate the chemical

changes that occur when carbonated water with appreciable calcium is discharged at the surface.

Tjiater Springs in western Java (table 19, analysis

11) deposited hundreds of thousands of tons of jarosite

(KFe3 (S04) 2 (OH)6 ) and iron phosphate high in arsenic.

Many other spring waters deposit iron oxides at or near

the surface. Ferrous iron is soluble in near-neutral

waters with a moderately low oxidation potential but is oxidized near the surface to ferric iron, which precipi- tates because of the low solubility of ferric hydroxide

(Hem, 1959b).

THERMAL METEORIC WATERS OF DEEP CIRCULATION

Some meteoric waters may circulate to depths of

thousands of feet in areas where the permeability of the

rocks is sufficiently high and differences in hydrodynamic pressure exist. The energy necessary for such deep circulation may be provided by artesian

pressure and by differences in density caused by dif- ferences in temperature and salinity.

Most thermal spring waters have somewhat higher

contents of dissolved matter than do associated meteoric waters. It is especially difficult to determine

the origin of some of the small to moderate quantities

of dissolved salts. They could be leached entirely

from rocks, because of the long flow path and increased

solvent action brought about through increase in temperature; or they could represent the admixture of

small amounts of very saline water from connate or magmatic sources. The waters of table 26 are of moderate to high temperatures, are of relatively low mineral content, and

are especially low in chloride when compared with most

hot-spring waters given in tables 15 to 25. They

probably have circulated to great depths and their

compositions probably have been determined almost

entirely by the original composition of the meteoric

water and by reaction with rocks.

According to Hutchinson (1957, p. 654-670), meteoric

water in equilibrium with the C02 of the atmosphere

could contain about 60 to perhaps 100 ppm of HC03

. Most of the waters given in table 26 are within this range. Some additional C02 probably has been supplied by organisms in the soil; extensive reaction with

silicate minerals and the resultant increase in pH in

the waters of analyses 1, 4, and 6 given in table 26

have probably caused some subsurface precipitation of

CaCO-3.

WATERS OF SALT DEPOSITS

Analyses of waters associated with evaporite deposits

are shown in table 27. Analyses 1 to 5 are of waters

from nonmarine saline deposits, and analyses 6 to 10

are of waters from marine saline deposits. Anhydrite

and gypsum deposits are commonly included with the

saline deposits. An analysis of water from gypsum is included in table 8 (analysis 5). The relatively high concentration of minor elements

in the brines of Searles Lake suggests that the brines

are probably connate nonmarine waters that are

similar in age to the enclosing salts; the highly soluble

minor elements have been greatly concentrated by

evaporation of water and by precipitation of the major

dissolved components. The apparent absence of subsurface drainage from the basin makes unlikely the

possibility of displacement by meteoric water and

selective dissolving of minor components.

The water from the salt deposits of the Salado

Formation (analysis 7) is particularly likely to be

connate, although perhaps it is modified greatly in

composition by diagenetic and metamorphic processes

(see chapter Y). When the ratio of Br/CI is notably

greater than 0.003, the water is likely to be connate;

in contrast, when the ratio of Br/CI is notably less than

0.003 (as analyses 6 and 9), the water is likely to be

meteoric in origin and salts are dissolved from crystalline deposits.

The sodium magnesium sulfate water, or "bitter"

water, of Budapest, Hungary (table 27, analysis 12),

is an example of other saline waters whose origin is highly uncertain. Vendl (1951, p. 188-196) suggests

that pyrite has been oxidized extensively and carbonates

have been dissolved, but other explanations appear

equally or more attractive.
F14 DATA OF GEOCHEMISTRY

Table 1.

Chemical analyses of ground waters from granite, rhyolile, and similar rock types

1 2 3 4 5 Rhyolite, Beatty, Nev.

Feb. 22, 1956

6 7 g Rock type and location Silicic volcanics, Grandview,

Idaho June 20, 1956

Rhyolite, W. of Los Alamos, N. Mex. May 25, 1954

Rhyolite tuff, S. of Mebane,

N.C.

Mar. 23, 1955

Rhyolite, Burns, Oreg.

Nov. 16, 1956

Granite, West Warwick,

R.I. May 26, 1955

Granite, McCormickCo.,

S.C. Date of collection - Nov. 24, 1954

New Bedford, Mass.

Oct. 31, 1955

SiOj _ ppm37

.1.19

.01 .00

.07 3.6

.8 3.9

2.3

epm ppm

55

.1.08

.0

epm ppm

39

2.7

1.1.0

.0

epm ppm

62

.2.00

.0

.0

epm ppm

52

.0.22

.0

epm ppm

20

.0.19

.0

.0.07 6.5

2.6

5.9

.8

38

.9 5.0

.5

1.5

.0

epm

0.32

.21 .26

.02

ppm

35

.1.18

.13

.0.09

134.3

8.4 3.5

72

6.9

3.8

.2

.4

.1

epm

0.65

.35

.36

.09

ppm

17

.0.04

.00

.00

.03

177.3

16

.9

51

22

15

.0 27

.1

epm

Al -- FeMn

Cu

Zn - Ca — 0.18

.07

.17 .06

4.4

1.4

111.2

42

1.9 2.0

.6

.3

0.22

.12

.48

.03

122.2 6.8

.6

80

.1 2.0

.1.8

.1

0.60

.18 .30

.02

145.8 20

5.2

112

7.7 4.0

.3

3.1

.2

0.70 .48

.87

.13

8.0

1.0 62

2.0

131

22

16.5 6.7

.2

0.40

.08 2.70

.05

0.85 Mg .60 Na .70 K._ .02

Total cations - 0.48 0.85 1.10 2.18 3.23 0.81 1.45 2.17

21

2.6

1.4

.1 1.9

.0

HCO3 - - 0.34

.05 .04

.01 .03

0.69

.04

.06

.03

.01

1.31

.00 .06

.01

.01

1.84

.16

.11 .02

.05

2.15

.46

.45

.03

.11

0.62

.02

.14 .03

.02

1.18

.14

.11

.01 .01

0.84 CO3 SO(

. - .46 CI - .42 F .00 NOj .44 PO«

0.47 0.83 1.39 2.18 3.20 0.83 1.45 2.16

Total, as reported 75 120 148 234 302 82 148 173

Specific conductance, micromhos

at 25° C 476.6

9.4 <6

0.2

0.1

0.9

.2.6 15

1.9

.07

807.2

12.8 <10

<0.1

0.2

0.4

.3

.1 21 .9

.3

1306.9

155.4 <0.1

1.3

1.8

.2.09 40

.05

.05

2177.6

14.4 <8

0.1 0.3

0.7

.4

.3 28

1.9.08

319

7.9

15.6

17 <0.1

5.0

0.1

.1.03 8.2

1.4.03

767.6

11.1

150.4

1.4

1.1.4

.1 7.6

.2

.1

1507.0

18.1 7.5 0.2

0.4

1.5

.3

.4 19

1.8

.05

236 pH — 6.3 Beta-gamma activity ...«ic per I.. U fS per I.. Ratios by weight: Ca/Na -

10.0

100.3

1.6

1.1 Mg/Ca .4 K/Na — .06 HCO3/CL 3.4 SO4/CI - 1.5 F/Cl - -

9

Granite,

Ellicott City, Md.

Mar. 21, 1951

10 Quartz Monzonite, W. of Clayton, Idaho

Sept. 8, 1954

11 Granite,

Stellenbosch, Union of South

Africa Mar. 19, 1940

12 Granite, Spokane, Wash.

June 6, 1951

13 Granite, Transvaal, Union of South

Africa

1944

14 Granite, Chester, Va.

Oct. 18, 1939

15 Granite, NE. Transvaal, Union of South

Africa July 1941

SiOj - —

ppm

39

.9 1.6

.0

epm ppm

27

.1.05

.00 .00

epm ppm

10 epm ppm

25 epm ppm

45

.0

.0

epm ppm

17 epm ppm76 epm

Al --- Fe - .22

.0 .03 Mn

Cu

Zn .- Ca — 276.2

9.5

1.4

1.35

.51 .41 .04

34

7.3 8.5

3.3

136

20

1.2

.2

.2

1.70

.60

.37

.08

6.0

11

} 85

43

15 138

0.30

.91 3.70

87

14

f 12

1 3.2

268

33

14

.2 32

4.34

1.15 .52

.08

27

4.7

1525.7

214

35

1386.6

.0

1.35 .39 6.59

.15

675.0

197

14

126

46824

3.4

.1

3.34

.41 8.57

.36

96

18

} 258

710

4.79 Mg - 1.48 Na -- 11.23 K - -

2.31 2.75 4.91 6.09 8.48 12.68 17.50

93

32

5.2

.0 7.5

HCOj — 1.52

.67 .15

.00

.12

2.23

.42

.03

.01

.00

0.70

.31 3.89

.00

4.39

.69

.39

.01 .52

3.50

.73 3.89

.35

.00

2.07 11.64 CO3

SO4 9.74 .68

.18

.00

20

193 .42 CI - - 6.44 F

NO3-. .00 PO)

Total anions - 2.46 2.69 4.90 6.00 8.47 12.67 17.50

223 238 308 489 628 922 1,370

spB^ffl'' oonductnriffi miei omhos at 25° C. 2586.6

6

255

7.5 7.8

70.1 4.6

4.0

.2

.4 113

17.2

569

7.3

10.6 pH 6.8 7.1 30.6

7.7 Temperature Beta-gamma activity Ra

____" C__ w

---;

ic per 1..

ic perl.. U .. ig perl.. Ratios by weight: Ca/Na 2.8

.2

.1 186.2

0.07

1.8

7.2

.2

.3

192.4

.01

0^2

.2

.04

1.6

.3

. 05-

0.3

.07 .07 5.2

20

.1

0.4 Mg/Ca .2 K/Na

HCO3/CI .3

.11 00

3.7 SO«/Cl - .1 F/Cl
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F15

EXPLANATION FOR TABLE 1

1. Spring, southwest of Grandview, sec. 9, T. 10 S., R. 1 W., Owyhee County,

Idaho. Water from pool below spring. Flows 25 gpm (estimated) from Tertiary silicic volcanic rocks. Unpublished data in U.S. Oeol. Survey flies; analyst, B. V. Salotto.

2. Spring, at head of East Fork of Jemez River, Sandoval County, west of Los

Alamos, N. Mex. Flows 250 gpm (estimated) from rhyolite of Tertiary age. Unpublished data in U.S. Geol. Survey flies; analysts, J. D. Honerkamp and

J. D. Weeks.

3. Drilled well, 106 ft deep, 1 mile south of Mebane, Alamance County, N.C. In

rhyolite tuff of Paleozoic(?) age. Unpublished data in U.S. Geol. Survey

flies; analysts, J. E. Whitney and J. A. Shaughnessy.

4. Well, 251 ft deep, sec. 12, T. 23 S., R. 30 E., Harney County, Oreg. In rhyolite

of Danforth Formation of Tertiary (Pliocene) age. Unpublished data in U.S.

Geol. Survey flies; analyst, R. A. Wilson.

5. Spring, about 3 miles north of Beatty, Nye County, Nev. Flows 5 gpm from

rhyolite of Tertiary age. Unpublished data in U.S. Geol. Survey flies; analyst, R. A. Wilson.

6. Drilled well, 140 ft deep, West Warwick, Kent County, R.I. In Cowesett Granite of Mississippian(?) age. Unpublished data in U.S. Geol. Survey files; analysts, J. E. Whitney and J. A. Shaughnessy.

7. Drilled well, 252 ft deep, John de la Howe School, McCormick County, S.C. In granite of Carboniferous(?) age. Unpublished data in U.S. Geol. Survey

flies; analysts, J. E. Whitney and J. A. Shaughnessy.

8. Drilled well, 205 ft deep, New Bedford, Bristol County, Mass. In Dedham

granodiorite of early Paleozoic age. Unpublished data in U.S. Geol. Survey

files; analyst, D. E. Weaver.

9. Drilled well, 28 ft deep, Ellicott City, Howard County, Md. In Ellicott City

Granite of late Paleozoic(?) age (Dingman and Meyer, 1954).

10. Snyders Spring, west of Clayton, near U.S. Highway 93, T. 11 N., R. 16 E., Custer County, Idaho. From quartz monzonite, probably late Mesozoic in age; contains 0.2 ppm boron (B). Unpublished data in U.S. Geol. Survey

files; analysts, J. D. Honerkamp, J. D. Weeks, and J. O. Johnson.

11. Drilled well, at Edenville, 4.5 miles southwest of Stellenbosch, Cape Province, Union of South Africa (Bond, 1946). In Cape Granite of late Precambrian(?)

age; water deposits iron oxide on standing; analyst, G. W. Bond.

12. Dug well, 45 ft deep, sec. 7, T. 26 N., R. 42 E., Spokane County, Wash. In

granodiorite of pre-Tertiary age, surrounded by alluvium of Spokane River; much of detrital material is basaltic (Weigle and Mundorff, 1952).

13. Warm spring, lat 24c34' S., long 27°36' E„ Buffelshoek, Transvaal, Union of South Africa. From Bushveld Granite of Precambrian age (Bond, 1946).

14. Drilled well, 386 ft deep, Chester, Chesterfield County, Va. (Cederstrom, 1945). In granite of Paleozoic age.

15. Drilled well, Malopena Camp, Kruger National Park, District of Letaba, north

eastern Transvaal, Union of South Africa. In Archean granite (Bond, 1946).
F16 DATA OF GEOCHEMISTRY

Table 2.Chemical analyses of ground waters from gabbro, basalt, and ultramafic rock types

1 Gabbro,

Waterloo, Md.

Dec. 23, 1952

2 Gabbro,

Laurel, Md. May 23, 1952

3 4 5

Peridotite, Webster, N.C.

6 7 Serpentine, Nottingham,

Pa.

Sept. 21, 1925

8

Basalt, Wa

May 1

Rock type and location Gabbro,

Harrisburg, N.C.

Feb. 22, 1955

Bushveld ultra- maflcs, Pretoria

district, Union

of South Africa Dec. 17, 1940

Serpentine, Lake Roland, Md.

Mar. 19, 1954

Camas,

sh.

7, 1949

Si02 ppm

39

.0

5.1.19

>.21 '2.7

5.1 2.3 6.2

3.2

epm ppm

21

.3 1.2

.16

epm ppm

56 epm ppm50 epm ppm

16 epm ppm

31

.2

.06

.00 .00

.05 9.5

514.0

2.2

276

2.6

12

.0 6.8

.0

epm ppm

40 epm ppm

49 epm

AlFe .06

.00 .08 .28 .04 Mn

Cu

Zn

0.25

.19

.27

.08

.0

16

10

151.5

20

5925

.1 2.2

.0

Ca 0.80

.82

.65

.04

32

1625

1.1

203

10

13

.2 2.7

1.60

1.32

1.09

.03

9.6

35

} 5.8

168

.5

14

0.48

2.88

.25

2.5 7.7

{ :l

44

.0

.0

.7

.3

0.12

.63

.01 .00

0.47

4.19

.17 .06

2.1 76

4.2

1.0

329

8.5

30

0.10

6.25

.18 .03

139.0

6.6

2.8

88

4.9

6.9

.1 8.4

0.65 Mg - .74 Na .29 K .07

0.79 2.31 4.04 3.61 0.76 4.89 6.56 1.75

37

9.2

1.0

.0.3

.0

HCOj 0.61

.19

.03

.00

.01

0.33

1.23

.70

.01 .04

3.33

.21 .37

.01 .04

2.75

.01 .40

0.72

.00 .02

.02

4.52

.05

.34

.00

.11

5.39

.18

.85

1.44 CO3 S04 - .10 CI .20 F .01 NO3 28 .45 2.7 .04 .14 POi

Total anions 0.84 2.31 3.96 3.61 0.76 5.02 6.46 1.89

Total, as reported 112 172 359 311 71 395 494 189

Specific conductance

776.7 259

5.6 3886.8

16.7

427

8.3

181 pH — 7.6 8.5 7.7

U -. p% per 1. Ratios by weight: Ca/Na 0.8

.4.5 37

9.2

1.1.6

.1.8 2.4

.004

1.3

.5

.4 16

.7.02

1.7 3.612

3.1

.0 63

.0.4

2.4

13

.6 23

.2

0.5

18.2

11 .3

2.0 Mg/Ca .7 K/Na .4 HCO3/CI 12

.04

13 SO</CI..__ .7 F/Cl .01

Analysis S 10 11 12 13 14 15 16 Columbia River

Basalt, Farmington,

Oreg. May 15, 1951

Basalt, Oahu Island, Hawaii

Mar. 6, 1928

Basalt, Moses Lake, Wash. May 1, 1950Basalt, Shoshone, Idaho

Oct. 30, 1956

Olivine Basalt

tuff-breccia, Buell Park,

Ariz. Sept. 29, 1948

Deccan Basalt, Puma,

Hyderabad,

India

Snake River

Basalt, Eden, Idaho Nov. 29, 1956

Stormberg

Date of collection

Basalt, Barberton, Union of South Africa

Sept. 20, 1941

SlOj ppm50 epm ppm63 epm ppm

55 epm ppm

33

.0.00

.00

epm ppm

31 epm ppm

30 epm ppm44

.05 .03

.00

epm ppm

43 epm

AlFe .43 .08 .03 Mn

Cu... Zn

Ca. 24

1512

5.3

1.20

1.23 .52

.14

17

1238

3.1

84

15

63

0.85

.99

1.65 .08

29

19123.5

177

156.9

.4 9.7

1.45

1.56

.52 .09

48

14

163.2

220

198.0

.3 5.2

.15

2.40

1.15 .70

.08

2042 }19

279

22

7

.2 2.5

1.00 3.45

.83

62

28

3.09

2.30

1.04

54

20

517.2

242

6146

.4 6.0

.00

2.69

1.64 2.22

.18

68

64

} 95

616

15

75

.0

16

3.39 Mg 5.26 NaK

4. 14

294

30

37

Total cations 3.09 3.57 3.62 4.33 5.28 6.43 6.73 12.79

156

1.6

15.2

.1

HCO3 2.56

.03

.42

.01 .00

1.38

.31 1.78

2.90

.31 .20

.02

.16

3.61

.40

.23

.02

.08

4.57

.46

.20

.01 .04

4.82

.62 1.04

3.97

1.27

1.30 .02

.10

10.10 COi

SO< .31 CI 2.12 F .00 NO3 .4 .01 .26 PO<

Total anions 3.02 3.48 3.59 4.34 5.28 6.48 6.66 12.79

Total, as reported 280 296 328 367 423 505 532 992

Specific conductance mieromhos at 25° C._ 427

7.7 340

7.9

404

8.0

13.1 <11

<0.1

2.7

3.0

.3

.2 282.4

.04

4588.2

12.2

641 pH 7.7 7.1 Temperature °C__ Beta-gamma activity. -w»c per 1.. <23

<0. 1 2.7

1.1

.4

.1 5.3

1.3nna

Ratios by weight: Ca/Na 2.0

.6

.4 10

.1

.01

0.4

.7.08

1.3.2

2.4

.7

.3

262.2

.06

1.1 2.1 2.6

.5

7 Mg/Ca .9 K/Na

HCOs/Cl 40

3.1

.na

7.9

.8 8.2 SOj/Cl .2 F/Cl

1 Values considered dubious, possibly contaminated.
CHEMICAL COMPOSITION OF SUBSURFACE "WATERS F17

EXPLANATION FOR TABLE 2

1. Drilled well, 75 ft deep, Waterloo, Howard County, Md. In gabbro (Dingman

and Meyer, 1954).

2. Drilled well, 35 ft deep, Laurel, Howard County, Md. In gabbro (Dingman and

Meyer, 1954).

3. Drilled well, 79 ft deep, 1 mile south of Harrisburg, Cabarrus County, N.C. In

gabbro. Unpublished data in U.S. Geol. Survey flies; analyst, S. A. Phillips.

4. Drilled well, 120 ft deep, 5 miles west of Hartebeespoort Dam, on main road to Rustenburg, District of Pretoria, Transvaal, Union'of South Africa. In norite, pyroxenite, and other ultramafic rocks of Bushveld complex of Precambrian

age (Bond, 1946); analyst, Q. W. Bond.

5. Drilled well, 250 ft deep, Webster, Jackson County, N.C. In periodotite (Le- Qrande, 1958).

6. Well Ed 22, 140 ft deep, Lake Roland, Baltimore County, Md. In serpentine (Dingman, Ferguson, and Martin, 1956).

7. Well 211, 100 ft deep, three-fourths of a mile southwest of Nottingham, Chester County, Pa. In serpentine (Hall, 1934).

8. Drilled well, 390 ft deep, near Camas, NWHNEH sec.8,T. 1 N., R. 3 E., Clark County, Wash. In basalt of Tertiary age (Griffin, Watkins, and Swenson,

1956).

9. Well at Farmington, NEHNWH sec. 31, T. 1 S., R. 2 W., Washington County

Oreg. In Columbia River Basalt of Tertiary age (Griffin, Watkins, and Swenson, 1956).

10. Well 153, Oahu Island, Hawaii. In late Tertiary basalt (Stearns and Vaksvik,

1935).

11. Drilled well, 210 ft deep, near Moses Lake, SWH sec. 28, T. 19 N., R. 24 E., Grant County, Wash. In Tertiary basalt (Mundorfl, Reis, and Strand, 1952).

12. Well at Shoshone, sec. 2, T. 6 S., R. 17 E., Lincoln County, Idaho. In Tertiary

basalt. Unpublished data In U.S. Geol. Survey flies; analyst, R. A. Wilson.

13. Spring, 3M miles east of Sawmill, Buell Park, Apache County, Ariz. (10 miles north of Fort Defiance). From olivine basalt tuff-breccia. Unpublished

data in U.S. Geol. Survey flies; analyst, L. S. Hughes.

14. Well at Purna Railway Station, State of Hyderabad, India. In Deccan Basalt of Cretaceous(?) age (Munn, 1934).

15. Well, 380 ft deep, Eden, NEH sec. 35, T. 9 S., R. 19 E., Jerome County, Idaho

In Snake River Basalt of Tertiary age. Unpublished data in U.S. Geol. Survey

flies; analyst, M. Fishman.

16. Drilled well at Komatipoort, District of Barberton, Transvaal, Union of South

Africa. In Stormberg lavas of Late Triassic age (Bond, 1946); analyst, G. W

Bond. EXPLANATION FOR TABLE 3

1. Spring, 16 miles northeast of Bear, sec. 3, T. 21 N., R. 2 W„ Adams County,

Idaho. Discbarges 200 gpm from altered andesite flows and pyroclastics and

younger intrusive dikes in Seven Devils Volcanics of Permian age. Unpublished data in U.S. Geol. Survey flies; analysts, R. A. Wilson, J. D. Weeks, and J. O. Johnson.

2. Drilled well, 160 ft deep. 8 miles west of Asheboro, Randolph County, N.C. In

Paleozoic andesite tuff. Unpublished data in U.S. Geol. Survey flies; analyst,

J. E. Whitney and J. A. Shaughnessy.

3. Drilled well, 683 ft deep, China Grove, Rowan County, N.C. In diorite. Unpublished data in U.S. Geol. Survey flies. 4. Drilled well, 179 ft deep, at Hamilton County Jail, Lake Pleasant Village, Hamilton County, N.Y. In syenite of Precambrian age. Unpublished data in U.S. Geol. Survey files; analysts, J. A. Shaughnessy and J. E. Whitney.

Table 3.Chemical analyses of ground waters from andesite

diorite, and syenite

1 Andesite, NE. of Bear, Idaho Aug. 8, 1954

2 Andesite

tuff, W. of Asheboro, N.C.

Mar. 22, 1955

3

Diorite, China

Grove, N.C.

1 Rock type and loca- tion

Date of collection

Syenite, Lake

Pleasant. N.Y.

Oct. 5, 1954

SiOj ppm8.9

.0.00

.00

epm ppm

31

.2.16

.03

.01

epm ppm

22 epm ppm

19

.0.14

.00

.00

.03 9.5 2.3 2.8

.6

38

2.8

2.1

.1 2.5

.1

epm

AlFe .04 Mn

Cu

ZnCa 12

.5 1.8

2.6

0.60

.04 .08

.07

145.6

9.6

.4

74

.1 8.8

.0 6.8

.0

0.70

.46

.42

.01

72

4.1

102.8

114

1156.5

.1.0

3.59

.34

.44

.07

0.47 Mg .19 Na .12 K .02

Total cations 0.79 1.59 4.44 0.80

38

6.3

.0

.1.2

.0

HCO3 0.62

.13

.00

.01 .00

.00

0.76

1.21

.00 .25

.00

.11

1.87

2.39

.18

.01

.00

0.62 COj

SO* 0.6 CI .06 F .01 NO3 .04 PO«

Total anions 1.57 4.45 0.79

Total, as re- 70 151 ?47 80

Specific conductance micromhos at 25° C PH

78

7.7

163

7.2 15.0 <5

<0.1

0.9

1.5

.4.04 8.4

.01 .0

80

7.7 7.6

10.0 Beta-gamma activity nnc per 1... Ra wc per 1..

<5

<0.1

0.2

6.7

.04 1.4

<5

0.1 0.6 Ratios by weight: Ca/Na 7.2

.06

.3 1818

.02

3.4 Mg/Ca .2 K/Na .2 HCO3/CI 18 SO«/Cl 1.3 F/Cl .05
F18 DATA OF GEOCHEMISTRY

Table 4.Chemical analyses of ground waters from sandstone , arkose, and graywacke

1 Catahoula

Sandstone, Collins, Miss.

Dec. 19, 1955

2 Dawson Arkose, E. of Monument,

Colo.

Sept. 2, 1955

3

Caseyville Sandstone, Dawson

Springs, Ky.

Jan. 3, 1955

4

Triassic Sandstone near Manchester, Conn. Nov. 4, 1954

5

St. Peter Sandstone Near Melbourne, Ark.

Sept. 19, 1954

6 Homewood

Sandstone Near Worthington, Pa. Mar. 3, 1955

7 Cretaceous

sandstone, Monzi, Zululand, Union of South Africa Nov. 5, 1941

i Arik

Sands SW. of

ford,

Sept. 1

Rock type and location

tone, CrawVebr.

9 1954

SiOj ppm

25

.2

.41 .00

epm ppm

35

.3.20

.00

epm ppm

9.4

.1 4.2

.21 .00

.00

166.4

epm

0.80

.53

ppm

14

.1.08

.10 .00 .00 27

10

epm ppm

12

.2.06

.00

epm ppm

8.0

.1.16

.00

.00

.00 447.6

epm ppm

20 epm ppm

61

.1 1.1.15

epm

Al -- FeMn

Cu -

ZnCa . - 2.4

.5 0.12

.04 9.6

1.9 0.48

.16

1.35

.82

50

6.0 2.50 .49

2.20 .621421 0.70

1.73 35

9.1 1.75 Mg .75 SrNa 2.6

2.0

.11 .05 },1

38

7.4

1.8

.1 1.5

.22 f 13

\ 2.2

98

143.0

.1 1.0

.56

.06

2.3

.8

80

315.6

.118

.1

.10 .02 2.4

3.0

184

2.1 1.8

6.5

.10 .08123.9

163

28

6.4

.1 1.2

.52

.10 } 36

122

12

61

1.57 f 7.8

I 6.0

161

5.5

4.0

.3 3.2

.34 K — — .15

Total cations 0.32 0.86 1.95 2.29 3.17 3.44 4.00 2.99

18

1.4 2.5

.1.0

HC03 - 0.30

.03

.07

.01 .00

0.62 "\~15~

.05

.01 .02

1.61

.29

.08

.01

.02

1.31

.64 .16

.01 .29

3.02

.04

.05

.00

.10

2.67

.58

.18

.01 .02

2.00

.25

1.72

2.64 COj so( .12 CI - .11 F .02 NO3 t 2 .00 .05 PO<

Total anions 0.41 0.85 2.01 2.41 3.21 3.46 3.97 2.94

Total, as reported 55 101 168 189 268 274 286 294

Specific conductance mieromhos at 25° C 38

6.2

18.9 <5

0.2

0.1

0.9

.2

.8 7.2.6

.04

916.7 8.9 <5

0.4

0.1

1.9

.2

1947.2 233

7.8

12.8 <10

0.1 0.6

12.4

.3

145.5

.02

299

7.4 16.7 <7

0.1 0.3

21

.1 1.3 1021.2

327

8.0

283 pH 5.6 7.8

12.2

101.3

2.1

1.2

.4.2 334.7

.na

<10

<0.1

0.2

3.7

.2

.3 26

4.4

.02

<)4 Ra /iMcperl.. U - MgperLRatios by weight: Ca/Na

<0.1

3 8

0.4

1.5

4.5 Mg/Ca .3 K/Na g HCO3/CI 214.1.06

2.0

.2 40 scvci 1.4 F/Cl .08

9 10 11 12 13 14 15 16 17 Rock type and location Navajo Sandstone, E. of Mexican

Water, Ariz.

Mar. 11, 1955

Pocono

Sandstone

near Jamestown, Pa.

May 26, 1954

Rensselaer Graywacke

near Sand

Lake, N.Y.

Sept. 20, 1954

St. Peter and

other Sandstone, Waukesha, Wis.

May 2, 1952

Franconia

Sandstone, Mound,

Minn.

May 29, 1939

Cambrian

sandstone, Kaukauna

Wis.

Oct. 27, 1955

Sylvania Sandstone

near Carleton, Mich.

Oct. 23, 1956

Bushveld

Sandstone,

Pretoria, Transvaal, Union of South Africa July 3, 1940

Oakville

Date of collection

Sandstone, Kennedy,

Tex.

Dec. 9, 1955

Si02 -- ppm11.2

.50

.00

.00

epm ppm

14

.0 1.3

.00

.00

.00 44

11

epm ppm

12

.0.62

.02

.00

epm ppm

8.7 epm ppm

20 epm ppm

6.9

.0.72

.07

.00

epm ppm

14.2

.71 .00

.00

.00

15363

epm ppm

56 epm ppm

58

.1.05

.00

epm

AlFe .37

.05

.58 Mn .34 Cu

ZnCa .8

.9 0.04

.07

2.20

.90

74

20 3.69

1.64

60

3152

124.0

285

11112

.5.8

2.99

2.55

1.19

.52

.10

78

51 3.894.19

157

2120

144.6

241

330

8.0

1.9

.3

.0

7.83

1.73 .46

.61 .12

7.63

5.18

7487 3.69

7.15 65

6.8 3.24 Mg .56

Sr. Na 144

.8 6.26.02

60

4.1

327

22

4.4

.2 2.0

2.61

.10 341.2

381

26

2.7

.2 1.0

1.48

.03 263.4

490

60

1.5

.2

2.4

1.13 .09 24

3.8

330

36230

1.1

.1

1.04

.10 }81

774

3.52 /374

\ 20

378

85

442

.8 5.2

.1

16.27 K .51

Total cations 6.39 5.81 6.84 7.35 9.30 10.75 13.95 14.36 20.58

21733

64

16

.3

.5

HCO3 3.56

1.10 1.33

.45

.02

.01

5.36

.46

.12

.01 .03

6.24

.54

.08

.01 .02

4.67

2.31 .34

.03

.01

8.03

1.25 .04

.01 .04

3.95

6.87

.23

.10

.00

5.41 12.68 6.20 CO3 - SO« 7.54 .85

.06

.00

1232

.2 32

.25

.90

.01 .52

1.77 CI 12.46 F .04 NO3 .08 PO<

Total anions 6.47 5.98 6.89 7.36 9.37 11.15 13.86 14.36 20.55

Total, as reported 489 490 553 577 733 806 982 1,150 1,440

Specific conductance mieromhos at 25° C 6309.2

14.4

72 <0.1

6.9

0.006

1.1.006

144.0

.02

533

7.4 10.6 <20

0.6

0.7

0.7

.2

.07

745.0

.OB

609

8.2

10.0 <25

0.1

5.0

2.2

.3.04

1419.6

(17

658

7.6

802

8.0 11.1

963

7.3

11.1 <25

2.7 0.5

11 .1.3 30

41 .2

1,1907.6

11.1 <50

1.2 2.1

6.4

.4

.2

1112.04

2,130 pH 7.6

7.6 26.4 Beta-gamma activity ^icperl.. <68 Ra /i^cperl.. 0.2 U jig per 1-. 15 Ratios by weight: Ca/Na

Mg/Ca

K/Na

5.0

.5

.3 24

9.3

.(U

3.0

.7

.1 327

40

1

0.9

1.2 0.2

.1.05 HCO3/CI 141 .4.006

.0 SOt /Cl .2 F/Cl .002
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F19

EXPLANATION FOR TABLE 4

1. Drilled well, 240 ft deep, Collins, Covington County, Miss. In Catahoula Sand

stone of Miocene(?) age. Unpublished data in U.S. Qeol. Survey files; analyst, E. Zitnik.

2. Drilled well, 180 ft deep, 3 miles east of Monument, SWH sec. 9, T. 11 S., E.

66 W., El Paso County, Colo. In Dawson Arkose of Tertiary age. Unpublished

data in U.S. Oeol. Survey files; analyst, E. Zitnik.

3. Drilled well, 188 ft deep, Dawson Springs, Hopkins County, Ky. In Caseyville Sandstone of Pennsylvanian age. Unpublished data in U.S. Geol. Survey

flies; analysts, J. A. Shaughnessy and J. E. Whitney.

4. Drilled well, 602 ft deep, 1 mile east of Manchester, Hartford County, Conn.

In sandstone of Triassic age. Unpublished data in U.S. Qeol. Survey files; analysts, J. A. Shaughnessy and J. E. Whitney.

5. Spring, 1 mile east of Melbourne, SEM sec. 1, T. 16 N., R. 9 W., Izard County,

Ark. From St. Peter Sandstone of Ordovician age. Unpublished data in U.S. Qeol. Survey files; analysts, R. A. Wilson, J. D. Weeks, and J. 0. Johnson.

6. Drilled well, 300 ft deep, near Worthington, Armstrong County, Pa. In Homewood Sandstone of Pennsylvanian age. Unpublished data in U.S. Geol. Survey

flies; analysts, J. E. Whitney and J. A. Shaughnessy.

7. Well at Monzi, Zululand, Union of South Africa. In Cretaceous sandstone (Bond, 1946) ; analyst, Q. W. Bond.

8. Drilled weU, 180 ft deep, 25 miles southwest of Crawford, NWK sec. 19, T. 29 N., R. 53 E., Sioux County, Nebr. In Arikaree Sandstone of Miocene age. Unpublished data in U.S. Geol. Survey files; analysts, J. D. Honerkamp, J. D. Weeks, and J. O. Johnson.

9. Drilled well, 592 ft deep, 6 miles east of Mexican Water, Apache County, Ariz. In Navajo Sandstone of Jurassic age. Unpublished data in U.S. Qeol. Survey

flies; analysts, J. E. Whitney and J. A. Shaughnessy.

10.

11.

12.

Drilled well, 122 ft deep, 0.3 mile northeast of Jamestown, Crawford County.

Pa. In Pocono Sandstone of Mississippian age. Unpublished data in U.S.

Geol. Survey flies; analysts, J. A. Shaughnessy and W. F. White.

Drilled well, 166 ft deep, 1.2 miles northeast of Sand Lake, Rensselaer County, N.Y. In Rensselaer Graywacke of Cambrian age. Unpublished data in U.S.

Geol. Survey flies; analysts, J. A. Shaughnessy and J. E. Whitney. North Street well, 1,907 ft deep, Waukesha, Waukesha County, Wis. In St. Peter, Mt. Simon, and associated sandstones of Cambrian to Ordovician age (Lohr and Love, 1954a).

13. Well, 509 ft deep, Mound, Hennepin County, Minn. In Franconia Sandstone

of Cambrian age (Prior, Schneider, and Durum, 1953).

14. Drilled well, 557 ft deep, Kaukauna, NWH sec. 25, T. 21 N., R. 18 E., Outagamie

County, Wis. In sandstone of Cambrian age. Unpublished data in U.S.

Geol. Survey files; analysts, B. V. Salotto and D. E. Weaver.

15. Drilled well, 100 ft deep, south-southeast of Oarleton, NWJ4 sec. 21, T. 5 S., R. 9 E., Monroe County, Mich. In Sylvania Sandstone of Devonian age. Unpublished data in U.S. Geol. Survey flies; analyst, D. E. Weaver. See

table 13, analysis 8, for deep saline water of Sylvania sandstone.

16. Drilled well, 140 ft deep, on Kalkheuvel 389, District of Pretoria, Transvaal, Union of South Africa. In Bushveld Sandstone (arkosic) of Triassic age (Bond,

1946, p. 141-142); analyst, G. W. Bond.

17. Drilled well, 416 ft deep, Kennedy, Karnes County, Tex. In Oakville Sandstone

of Miocene age. Unpublished data in U.S. Geol. Survey files; analyst, R. A.

Wilson.
F20 DATA OF GEOCHEMISTRY

Table 5.

Chemical analyses of ground waters from siltstone, clay, and shale

1 5 f 4

1 Sh

vs

M

e 8 9 Rock type and location .. Hattiesburg

Clay,

Prentiss, Miss.

Dec. 19, 1955

Ohio Shale, Park Lake, Ky.

Jan. 5, 1955

Brunswick

Shale, Wyckoff,

N.J. Feb. 27, 1957

Tuffaceous

clay, Dear

Sheaville, Oreg. June 28, 1956

Chicopee

Shale, Chicopee, Mass.

Dec. 8, 1954

ale, Transal, Union

}f South

Africa ay 8, 1941

Clay, George- town, S.C.

Jan. 10, 1947

Brule Silt- stone, Harrisburg, Nebr. Nov. 9, 1955

Ecca Shale,

Date of collection

Cape

Province, Union of South Africa Nov. 7, 1941

SiOj ppm

12

.2

.0( .«

epm ppm

22

1.5

.39

.22

.05

.36

157.5 36

3.5

epm ppm

16

.0.02 .00

.00

.00 2916

12

1.1

epm ppm

43

.0

.00

.00

epm ppm

15

.0 1.0

.08

.00

.03

96

19

18

1.5

epm ppm

40 epm ppm

12- epm ppm

64

.4.00

.00

epm ppm

32 . epm

AlFe > .92 Mn I Cu

ZnCa 1.2

.5 2.1.8

6.06

.04 .09

.02

6.75

.62

1.56

.09

1.45

1.32

.52

.03

29

11

318.0

1.45

.90

1.35

.20

4.79

1.56 .78

.04 }

32

46

34

1.60 3.78

1.48

1.6

.7 210

0.08

.06 9.13J

449.2

129

10

346

76

42

.1 16.2

2.20

.76

5.61 .26

6264

} 92

362

. 106 140

.6 16

3.09 Mg 5.26 Na 4.05 K—

. 0.21 3.02 3.32 3.90 7.17 6.86 9.27. 8.83 12.40

8.0

.5 2.0

.0 2.2

.0

3.2

128

21

.2.5

.0

126

22

12

.2 26

.0

173

733

6.0

.7.0

.0

133

208

25

.4

.4.0

366

428

447

32

1.5 28

.9.0

HCO3 0.13 0.05 2.06 2.84

.23 .69

.17 .04

2.18 6.00 7.33

1.07

.03

.79

.05

.00

5.67

1.58 1.18

.01 .26

5.93 CO3

SO< .01 .06

.00

.04

2.66

.59

.01

.01

.46

.34

.01 .42

4.33

.70

.02

.01

.08

.79

2.21 CI 3.95 F .03 NOs .26 PO«

Total anions 0.24 3.32 3.29 3.97 7.24 6.87 9.27 8.70 12.38

30 239 260 342 517 550 735 737 875 .

Specific conductance micromhos at 25° C... 26

6.1 19.4 <5

0.1 <0.1

0.6

.4

.4 4.0

.2.0

373

4.9

10.0

16

2.1 18

0.4

.5

.1.2 6.1

.01

340

7.9 10.6 <10

<0.1

1.4

2.4

.6:09

101.8

.02

365

8.5 16.7

16 <0.1

0.1

0.9

.4

.3 295.5

.1

690

7.8 12.5 <25

0.7

1.5

5.3

.2.08

5.3

8.3

.02

839

7.7

11.1 <23

0.1

16

0.3

.2.08 8.2

1.8

.002

pH 7.8 8.6

20

7.6 Temperature °C.. Beta-gamma activity.. -mmc per 1.. Ra we per 1.. U. Mg per 1.. Ratios by weight: Ca/Na 0.9

1.4 0.008.4 0.7 Mg/Ca 1.0 K/Na

HCO3/CI- 13

.1.0

16

.05

.03

2.6 SO4/CI .8 F/Cl .004

10 Wlllard

Shale, Lyon

County,

Kans.

Sept. 11, 1951

11 Camillus and

Vernon

Shales, Syracuse, N.Y.

May 3, 1956

12 Shale, Cuyahoga

County,

Ohio

Jan. 15, 1952

13 Benton

Shale, La

Prele, Wyo.

Aug. 16, 1950

14 Shale, Pekin, N.C.

Feb. 28, 1955

15 Eutaw Clay, Linden, Ala.

Mar. 17, 1952

16 Pierre Shale Langdon, N. Dak.

Oct. 27, 195'

17 Precambrian shale, Cape

Province, Union of South

Africa

[ Mar. 19, 1940

18 Rock type and location . Jackson

Date of collection

Shale, Monticello, Ark.

Dec. 13, 1955

SiOj ppm

11 epm ppm

6.5

.0 3.5

.13

.02

.00 22729

r 12

\ 2.7

epm ppm

19 epm ppm13 epm ppm

17

.1 8.2

.07

.12

.05 48

29

4478.4

epm ppm

133.6

.16

epm ppm

262.2

3.5

21

epm ppm

5 epm) ppm

9828

.88 9.6

epm

Al _ 2.33 Fe .21 1.3

.00

4.1 Mn .34 Cu

Zn

Ca 95

43 }l09

4.74 3.54

4.74

11.33 2.38 .52

.07

12370

612.2

6.13 5.76

2.65

.06

8.5

.4 310

5.0

0.42

.03 13.48

.13

2.40 2.38

19.44

.21

6.1 2.1 624

5.7

0.30

.17 27.13

.15

416

143 362

14

20.7

11.7 15.7

.3

6 33

6 23 1} 69

2

1 16.52

7 19.49

i 30.36

424

194

2,420 380

1.8

3.1.0

21.16 Mg 15.95 Na 18.10 K - .28

13.02

2

14.30 14.60 14.06 24.43 27.75 48. e . 66.37 58.16 HCOi 344

12036

.2 239

5.64 RR 4.72 539

2833.5

.4

.1

8.83 58012

2.0

142

1.0

2.6

9.61 .40

.04

4.00

.05 .04

679

1.5 636

1.2

.2

9.49 642

1.6 692

2.8

1.5

10.52 104

2,17038

.2

.1

1.7

45.1

1.0

.0.€

91

8 15

7 1,71

1

i 14.98

)

2 3.16

5 48.22

)

3

COa

43924

.0

.9

.0

SO« 2.50

1.02

.01 3.86

9.14

.68 .00

.01

5.89 .10

.02

.00

.03 15.12

.06

.00

.03 16.70 .15

.02

50.38 CI ___ 10.72 NO»ir"""TM~~~~""""~

.09

.05 PO«

Total anions 13.03 14.55 14.84 14.04 24.70 27.42 47. S« 66.36

3

61.24

Total, as reported 997 1,030 1,100 1,080 1,680 1,890 3,300 4,0a 3,990

Specific conductancemicromhos at 2 5°C._ 1,2107.6

11.1 <50

<0.1

2.1

19

.1.2 12

if)

1,1807.3

11.1

1,3408.2

10.6

2,410

8.1

17.8 <100

0.6

24

0.1.6

.02

1.1

2,710

7.7 26.7

3,560

6.3

6.1 <110

<0.1

0.3

1.1.3

.04 2.7

K7

4,570 pH 7.5 4.0 Temperature -°C_. Beta-gamma activity ji/ic aer 1 <140

1.7

17 Ratios by weight: Ca/Na 0.9

.5

2.0.6

.6

154

lit

0.03

.05

.02

4.1M

0.01

.3

.3

1.1

0.5

.7 1.0 Mg/Ca_

K/Na

.5.03 HCOj/Cl 9.6 3 3

.5 SOj/Cl na 6.4 F/Cl .006 .0 .1 007 002 005 .005 .0 .005
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F21

EXPLANATION FOR TABLE 5

1. Drilled well, 148 ft deep, Prenliss, Jefferson Davis County. Miss. In clay of Hattiesburg Formation of Miocene age. Unpublished data in U.S. Geol. Survey files; analyst, E. Zitnik.

2. Spring, Park Lake, Fleming County, Ky. From Ohio Shale of Devonian age. Unpublished data in U.S. Geol. Survey files; analysts, J. A. Shaughnessy and

J. E. Whitney.

3. Drilled well, 300 ft deep, Wyckoff, Bergen County, N.J. In Brunswick Shale of

Triassic age. Unpublished data in U.S. Geol. Survey files; analyst, D. E.

Weaver.

4. Spring, one-quarter mile southeast of Sheaville, sec. 24, T. 28 S., R. 46 E., Malheur

County, Oreg. From tuffaceous clay of Miocene age. Unpublished data in U.S. Geol. Survey files; analyst, R. A. Wilson.

f>. Well, 110 ft deep, Chicopee, Hampden County, Mass. In Chicopee Shale of Late Triassic age. Unpublished data in U.S. Geol. Survey files; analysts,

J. E. Whitney and J. A. Shaughnessy.

6. Borehole Donkerhoek 178, Transvaal, Union of South Africa. In slightly met- amorphosed shale of Transvaal System of Precambrian age (Bond, 1946); analyst, G. W. Bond.

7. Drilled well, 720 ft deep, Georgetown, Georgetown County, S.C. In clay of Black Creek Formation of Cretaceous age. Unpublished data in U.S. Geol. Survey files; analyst, F. H. Pauszek.

8. Drilled well, 80 ft deep, Harrisburg, SEK sec. 2, T. 18 N., R. 56 W Banner

County, Nebr. In Brule Siltstone ol Oligocene age. Unpublished data in U.S. Geol. Survey files; analyst, E. Zitnik.

9. Drilled well at Brittstown, Cape Province, Union of South Africa. In shale of Ecca Series of Permian age (Bond, 1946); analyst, G. W. Bond.

10

11

Dug well, 38 ft deep, SEHSEH sec. 28, T. 21 S., R. 11 E., Lyon County, Kans.

In Willard and Dry Shales of Pennsylvanian age (O'Connor, 1953). Drilled well, 300 ft deep, Syracuse, Onondaga County, N.Y. In Camillus and

Vernon Shales of Silurian age. Unpublished data in U.S. Geol. Survey files; analyst, B. V. Salotto.

12. Drilled well, 72 ft deep, Strongsville Township, Cuyahoga County, Ohio. In

shale of Mississippian age. Unpublished data in U.S. Geol. Survey files. 13. Drilled well 32-73-8 DAB, 725 ft deep. La Prele area. Converse County, Wyo.

In Benton Shale of Cretaceous age (Rapp, 1953). Also reported; B, 1.6 ppm.

14. Drilled well, 130 it deep, one-half mile east oj Pekin, Montgomery County, NC.

In shale of Triassic age. Unpublished data in U.S. Geol. Survey files; analysts.

J. E. Whitney and J. A. Shaughnessy.

15. Drilled well, 1107 ft deep, Linden, NEHNWK sec. 6, T. 15 N., R. 2 E., Marengo

County, Ala. In clay of Eutaw Formation of Cretaceous age. Unpublished

data in U.S. Geol. Survey files; analyst, J. H. Hubble.

16. Dug well, 35 ft deep, Langdon, SEK sec. 14, T. 161 N., R. 60 W., Cavalier County, N. Dak. In Pierre Shale ot Cretaceous age. Unpublished data in U.S. Geol. Survey files; analysts, J. D. Honerkamp, J. D. Weeks, and J. O. Johnson.

17. Drilled well, 80 ft deep, Ridgemore Farm, near Faure, Cape Province, Union of South Africa. In shale of Malmesbury Series of Precambrian age (Bond,

1946); analyst, G. W. Bond.

Well, 22 ft deep, 7 miles northeast of Montlcello, NEK sec. 30, T. 11 S., R. 6 W., Drew County, Ark. In Jackson Clay of Eocene age. Unpublished data in U.S. Geol. Survey files; analyst, E. Zitnik.18
F22 DATA OF GEOCHEMISTRY

Table 6.—Chemical analyses of ground waters from limestone

1 Miocene

limestone,

Gainesville, Fla. Apr. 16, 1946

2 Warsaw

Limestone, Tuscumbia,

Ala. Apr. 10,' 1956

3 Miocene

limestone,

Brooksville,

Fla. July 5, 1946

4 Bangor

Limestone,

Irondale, Ala.

Sept. 3, 1952

5 Ocala Limestone, Lake City,

Fla. Mar. 16, 1957

6 Meagher

Limestone,

Ennis, Mont.

Sept. 10, 1956

7 Source (formation or age) and location Castle Hayne

Date of collection

Limestone, New Bern, N.C.

Feb. 21, 1956

SiOj ppm10 epm ppm

7.7

.0.23

.08

.00 .00

431.2

1.5

.7

133

3.2

2.2

.1 5.9

.0

epm ppm

8.9 epm ppm

10 epm ppm

25

.1.17

.00 .00

.02 39

157.5

1.3

196

1.8 9.8

.5

.8

.1

epm ppm

11.2.00

.00

epm ppm

21.0 3.5

.02

epm

AlFe .04 .05 .14 Mn. . Cu

ZnCa 156.7 3.2

.6

0.75

.55

.14 .02

2.15

.10 .06

.02

48

5.8 4.0

.7

168

6.4

4.8

.1.0

2.40

.48

.17

.02

583.2

3.4

.6

164

7.0

7.5

.1 8.9

2.89

.26

.15 .02

1.95

1.23 .33

.03

53

192.8

1.6

187

612.2

.3

1.4.05

2.64

1.56 .12

.04

76

1.3 5.0

.7

240

.2 8.0.2

.2

.0

3.79 Mg .11 Na - .22 K .02

Total cations 1.46 2.33 3.07 3.32 3.54 4.36 4.14

74

2.6

3.4

.4

1.8

HCO3 1.21

.05

.10 .02

.03

2.18

.07 .06

.01 .10

2.75

.13 .14

.01 .00

2.69

.15

.21

.01 .14

3.21

.04

.28

.03

.01

3.06

1.27 .06

.02

.02

3.93 COs

SO4 _ .00 CI .23 F .01 NO3 Voo

PO<

Total anions 1.41 2.42 3.03 3.20 3.57 4.43 4.17

Total, as reported... 118 199 247 263 297 340 356

Specific conductance micromho sat 25° C- 1437.0 22.2

224

7.3

16.1 <10

0.2

0.3

29.03

.5 60

1.5

.05

287

7.7 23.9

301

7.5

17.8

327

8.0 22.2

140.6

0.2

5.2

.4.2 20

.2.05

409

7.8

12.2

393 pH 7.1 Temperature Beta-gamma activity. °C- 16.7 RaU _ Ratios by weight: Ca/Na 4.7

.4.2 22

.8

.1

12

.1.2 35

1.3.02

17.06

.2 22

.9.01

19

.4.6 85

28

.1

15 Mg/Ca .02 K/Na .1 HCOs/Cl 30 SO4/CI .03 F/Cl .03

Analysis . 8 Edwards

Limestone,

Uvalde, Tex. Nov. 2, 1945

9 Laurel

Limestone, Bardstown, Ky.

Jan. 4, 1955

10 Bayport dolo- mitic Limestone, Grand Rapids, Mich.

Jan. 21, 1953

11 Pahasapa

Limestone, Rapid City,

S. Dak.

Aug. 20, 1954

12 Lebanon

Limestone, Mt. Juliet, Tenn. Nov. 17, 1954

13 Conasauga

limestone, Birmingham,

Ala

Oct. 3, 1952

14 Source (formation or age) and location

Date of collection ..

Limestone,

Roswell, N. Mex. May 14, 1954

Si02 ppm

11 epm ppm11

.1.02

.00

.00

.00

6134

9.0

1.1

291

20

11

.1 44

epm ppm

8.4 epm ppm

23

.1.00

.00

epm ppm

9.2

.0.22

.33

.00

epm ppm

11 epm ppm12.2

.01

.01

epm

AlFe .08 .07 1.4 Mn.... Cu

ZnCa 749.5 24

7.0

3.69

.78

1.04

.18

3.04

2.80

.39

.03

79

288.1

5.7

267

5129

.0 28

3.94 2.30

.35

.15

92

375.9

4.9

207

214

1.8

.5

.3

.0

4.59

3.04

.26

.13

12428

143.0

460

57

18

.1 5.0

.0

6.19

2.30

.61 .08

96

37

611.2

291

91 112

.1 20

4.79 3.04

2.65

.03

140

41

311.3

236

31542

.9 3.8

6.99 Mg _ 3.37 Na 1.35 K .03 Total cations.. 5.69 6.26 6.74 8.02 9.18 10.51 11.74

277

1924

.4 4.1

HCO3 4.54

.40

.68 .02

.07

4.77

.42

.31

.01 .71

4.38

1.06 .82

.00 .45

3.39

4.46

.05

.03

.00

7.54

1.19

.51

.01 .08

4.77

1.89 3.16

.01 .32

3.87 COs

SO4 6.56 CI 1.18 F .05 NO3 _ .06 PO( Total anions 5.71 6.22 6.71 7.93 9.33 10.15 11.72

Total, as reported 450 482 504 587 720 722 823

Specific conductance micromhos at 25° C. pH

570

7.0 587

8.2

14.4 <25

0.1 0.7

6.8

.6

.1 26

1.8

(TOO

649

7.3 7057.4

48.9

17 2.0

6.4

16.4

.8 115

119 3

808

7.8

13.9 <25

0.1

1.2

8.9

.2

.2

263.2

nnfi

963

7.3

16.7

1,0407.6 Temperature °C. 20.6 Beta-gamma activity ..mac perl.. <10 Ra .-mmc per l._ 0.1 U ..-Mg perl.. 1.0 Ratios by weight: Ca/Na 3.1

.1.3 12

.8

.02

9.8

.4

.7 9.2

1.8n

1.6

.4.02 2.6

.8mi

4.5 Mg/Ca .3 K/Na .04 HCOj/Cl 5.6 SO,/Cl _ 7 5 F/Cl... _ _._ .02
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F23

EXPLANATION FOR TABLE 6

1. Glen Springs, 2 miles northwest of Gainesville, Alachua County, Fla. Flows

150 gpm from limestone of Miocene age (Ferguson, Lingham, Love, and Vernon,

1947).

2. Artesian spring, Tuscumbia, NWM sec. 9, T. 4 S., R. 11 W., Colbert County,

Ala. From Warsaw Limestone of Mississippian age. Unpublished data in U.S. Geol. Survey flies; analyst, D. E. Weaver.

3. Weekiwachee spring, 12 miles southwest of Brooksville, Hernando County, Fla. Flows 71,000 gpm from limestone of Miocene age (Ferguson, Lingham, Love, and

Vernon, 1947).

4. Drilled well, 210 ft deep.Irondale, Jefferson County, Ala. In Bangor Limestone

of Mississippian age (Robinson, Ivey, and Billingsley, 1953).

5. Drilled well, 275 ft deep, 1792 Putnam St., Lake City, Columbia County, Fla. In Ocala Limestone of Eocene age. Unpublished data in U.S. Geol. Survey

files; analyst, D. E. Weaver.

6. Spring, 9 miles south of Ennis, SWH sec. 13, T. 7 S., R. 2 W., Madison County, Mont. Flows 15,000 gpm irom Meagher Limestone of Cambrian age. Unpublished data in U.S. Geol. Survey files; analyst, R. A. Wilson.

7. Drilled well, 126 ft deep. New Bern, Craven County, N.C. In Castle Hayne

Limestone of Eocene age. Unpublished data in U.S. Geol. Survey files; analyst, S. H. Phillips.

8. Well, 350 ft deep. Uvalde. Uvalde County, Tex. In Edwards Limestone of Cretaceous age (Petit and George, 1956)

.

9. Spring, southwest border of Bardstown, Nelson County, Ky. Flows 15 gpm

from Laurel Limestone oi Silurian age (dolomitic in some areas). Unpublished

data in U.S. Geo). Survey flies; analysts, J. A. Shaughnessy and J. E. Whitney.

Drilled well, 57 ft deep, northeast of Grand Rapids, SEHSEM sec. 1, T. 8 N., R. 12 W., Kent County, Mich. In Bayport Dolomitic Limestone of Mississip- pian age; water may be from sandstone lenses in this formation (Stramel, Wisler, and Laird, 1954).

11. Well, 4,645 ft deep, Rapid City, NW H sec. 18, T. 2 N., R. 9 E., Pennington County, S. Dak. In Pahasapa Limestone of Mississippian age. Unpublished

data in U.S. Geol. Survey files; analysts, J. D. Honerkamp, J. D. Weeks, and

J. O. Johnson; also reported: B, 0.41 ppm.

12. Drilled well, 6y ft deep, Mount Juliet, Wilson County, Tenn. In Lebanon

Limestone oi Ordovician age. Unpublished data in U.S. Geol. Survey files; analysts, J. E. Whitney and J. A. Shaughnessy.

13. Drilled well, 310 ft deep, Birmingham, Jefferson County, Ala. In Conasauga

Limestone of Cambrian age (Robinson, Ivey, and Billingsley, 1953).

14. Flowing well, 843 ft deep, 10 miles southeast of Roswell, SWH sec. 15, T. US., R. 25 E., Chaves County, N. Mex. Flows 2,000 gpm from San Andres Limestone of Permian age. Unpublished data in U.S. Geol. Survey files; analysts, R. A. Wilson, J. D. Weeks, and J. O. Johnson.

10.

Table 7.

Chemical analyses of ground waters from dolomite

1 Gasconade

Dolomite, Alley, Mo.

June 19, 1925

2 Copper Ridge

Dolomite, Center

Point, Ala.

Oct. 1, 1952

3 Niagara Dolomite, West Allis, Wis.

Oct. 29, 1954

4 PreCambrian

5 6 dolomite near

Irene, Pretoria, Transvaal, Union

of South Africa

Oct. 2, 1939

Peebles Dolomite,

Bainbridge, Ohio

May 13, 1955

Guelph Dolomite, Fort Recovery, Ohio Mar. 20, 1955

SiOj ppm

5.4 epm ppm

9.2 epm ppm18

.2.39

.03 .00

.00 35

33

28

1.3

spm ppm

24 epm ppm11.0.48

.13

.00

epm ppm

14

.2 4.2

.05

.00

.00 17886

763.5

epm

AlFe - .17 .34 Mn

Cu

Zn --- Ca - 30

18

} 4.6

1.50 1.48

.20

34

14

/ 2.0

I .6

1.70

1.15

.09

.02

1.75

2.71 1.22

.03

5.71

67

39

} 8.0

3.34

3.21

.35

28

72

/ 3.5

I 1.7

1.40

5.92

.15

.04

8.88 Mg —

7.07 Na - - 3.30 K. . .09

3.18 2.96 6.90 7.51 19.34

160

41.4 5.0

160

3.7

2.5

.1 3.2

241

88

1.0

.9 12

390

1.0

17

.0

.4

398

28

5.0

.1 31.0

285

707

111.7

1.1

HC03 2.62

.13 .03

.14

2.62 3.95 6.39 6.52 4.67 COj - so« .08

.07

.01 .05

1.83 .03

.05

.02

.02 .48

.00

.01

.58

.14

.01 .50

14.72 CI .31 F — - - .09 NO3 - .9 .02 .02 PO«

2.94 2.83 5.88 6.90 7.75 19.81

229 230 448 546 579 1,370

259

7.5

16.7

5118.2

10.3 <25

0.1 <0.1

1.2.9

.04

24188

.9

663

7.6

13.3 <25

0.2 0.8

8.0 2.6

.5 80

5.6

.02

1,510 pH 7.9 7.4 Temoerature °C 15.0 <50 Ra - niic per 1.. 0.6 U /ig per 1„ 2.0 Ratios by weight: Ca/Na 6.5

.6 17

.4

.3 64

1.5

.04

8.4

.6 2.3 Mg/Ca - .5 K/Na .05 HCOj/Cl 32

.3 23

.06

.0

26 S0</C1 „ 64 F/Cl .15

EXPLANATION FOR TABLE 7

1. Alley Spring, Alley Spring State Park, sec. 25, T. 29, N., R. 5 W., Shannon County, Mo. Flows 16,600 gpm trom Gasconade Dolomite of Ordovician age (Beckman

and Hinchey, 1944).

2. Harvey Spring, i W miles southeast of Center Point, Jefferson County, Ala. From

Cooper Ridge Dolomite of Cambrian age (Robinson, Ivey, and Billingsley,

195Sj.

3. Drilled well, 500 ft deep, 2 miles west of West Allis, sec. 6, T. 6 N., R. 21 E., Mil- waukee County, W13. In Niagara Dolomite of Silurian age. Unpublished

data in U.S. Geol. Survey files; analysts, J. E. Whitney and J. A. Shaughnessy.

4. Drilled well, 100 ft deep, 1 mile south of Irene, on main road to Johannesburg,

District of Pretoria, Transvaai, Union of South Africa. In dolomite of Pre- cambrain age (Bond, 1946); analyst, G. W. Bond.

5. Drilled well, 95 tt deep, 3.3 miles west of Bainbridge, Ross County, Ohio (on U.S. Highway 50). In Peebles Dolomite of Silurian age. Unpublished data in U.S. Geol. Survey files; analysts, J. E. Whitney and J. A. Shaughnessy.

6. Drilled well, 208 ft deep, Fort Recovery, Mercer County, Ohio. In Guelph Dolomite of Silurian age. Unpublished data in U.S. Geol. Survey files; analysts

J. E. Whitney and J. A. Shaughnessy.
F24 DATA OF GEOCHEMISTRY

Table 8.— Chemical analyses c/ ground waters from miscellaneous sedimentary rocks

Analysis.. 1 Biwabik Iron Formation, Grand Rapids, Minn.

Sept. 22, 1954

2 Big Fork Chert, Hot

Springs, Ark. May 28, 1956

3 Phosphoria Phosphate,

Garrison, Mont.

Apr. 2, 1957

4 Lignite, Fort Union

Formation Belfleld, N. Dak. Mar. 9, 1957

5 Gypsum

Formation,

Bluff, > Date of collection Nov. 2

W. of Red

f. Mex.

5, 1949

SiOj ppm14

.0.65

.00

54

197.5

5.8

epm ppm

26

.9.95

.18 26

1.9 7.4 2.8

epm ppm

8.6

.1 1.3

.00 36

142.3

1.8

epm ppm

11

.1.90

.09

74

53 624

5.4

epm ppm

29 epm

Al — — — Fe — Mn

Ca 2.70

1.56 .33

.15

1.30 .16 32

.07

1.80

1.15

.10 .05

3.69

4.36 27.14

.14

636

43

} »

31.74 Mg 3.54 NaK

.74

4.74 1.85 3.10 35.33 36.02

271

6.1.5

.1 1.2

.0

68

34

2.2

.1

.1.0

131

402.0.9

.8.45

702

1,08025

.3

.0.15

143

1,57024

HCO3-— 4.44 1.11 2.15 11.51 2.34 CO3

SO, .13

.01 .01 .02

.71 .06

.01 .00

.83 .06

.05

.01

22.49

.70 .02

32.69 CI .68 F . —

NO3 18 .29 P0(

4.61 1.89 3.10 34.72 36.00

380 171 239 2,580 2,480

Specific conductance— .micromhos at 25° 0—

pH -- 413

7.8

7.8 <14

2.6 0.2

7.2 3.5

.8 500

12

.2

199

6.5 28.9 <7

0.8

294

7.4 12.8 <8

2.1 2.7

16

.4

.8 66

20

.4

3,060

7.1 5.0 <85

0.2

1.0

0.1

.7.009 2843

.01

2,510

Ra

°c.

Tj /xg per L.

Ratios by weight: Ca/Na 3.5

.07 .4

31

15.05

37 Mg/Ca - .07 K/Na -- HCO3/CI 6.0 pcvci 65 F/Cl

EXPLANATION FOR TABLE 8

1. Drilled well, 573 ft deep, Grand Rapids, Itasca County, Minn. In Biwabik

Iron Formation of Precambrian age, consisting of ferruginous sediments, largely unmetamorphosed in this area. Unpublished data in U.S. Geol. Survey files; analysts, R. A. Wilson, J. D. Weeks, and J. O. Johnson.

2. Drilled well, 200 ft deep, east of city of Hot Springs, SWk sec. 33, T. 2 S., R. 19 W.,

Garland County, Ark. In Big Fork Chert of Ordovician age. Unpublished

data in U.S. Geol. Survey files; analyst, B. P. Robinson.

3. Drainage water from 1,000-ft level, Anderson phosphate mine, Garrison, sec. 10, T. 10 N. R. in W.. Powell County, Mont. From Phosphoria Formation of

Permian age. Unpublished data in U.S. Geol. Survey files; analyst, J. O.

Johnson.

4. Drilled well, 85 ft deep, Belfleld, sec. 4, T. 139 N., R. 99 W., Stark County, N. Dak.

In lignitic coal of Fort Union Formation of Teriary age. Unpublished data in U.S. Geol. Survey files; analyst, Darwin Golden.

5. Jumping Springs, sec. 17, T. 26 S., R. 26 E., 15 miles west of Red Bluff, Eddy

County, N. Mex. Flows 5 gpm from gypsum of Castile Formation of Permian

age (Hendrickson and Jones, 1952). See table 27 for analyses of saline waters from associated evaporite deposits.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F25

Table 9. —Chemical analyses of ground waters from quartzile and marble

1 Mutual Quartzite, Kamas,

Utah

Oct. 20, 1954

2 Pretoria Quartzite, Transvaal, Union of South

Africa Nov. 27, 1940

3 Quartz!te, Bucks County,

Pa.

Sept. 7, 1953

4 Quartzite, Cliffs Shaft Mine, Mich.

Jan. 28, 1952

5 Sioux Quartzite, Sioux Falls,

S. Dak.

Aug. 28, 1954

6 Sylacauga Marble, Sylacauga,

Ala.

Apr. 27, 1955

7 Cockeysville

Date of collection

Marble, Balti- more County, Md. May 5, 1953

SiOj ppm

3.6

.0.00

.00

epm ppm

8.0 epm ppm17 epm ppm7.6

.0

.21 .20

epm ppm

15.2

.91 1.6

epm ppm

9.9

.0

.03 .04

.00 39

10

epm

1.95

.82

ppm

17

.3

.16

.01 .05 649.4

epm

AlFe 1.6 Mn

Cu

Ca 2.6

.4 0.13 .03

1.6 5.80.08

.48 255.1 1.25 .42 32

16 1.601.32

102

35 5.09

2.88

3.19 Mg. . .77 SrNa 1.0

1.8 .04

.05 } 2.8

18

2.0

9.9

.0 4.0

.12 J 4.5

\ 3.8

80

138.0

.4.3

.20

.10 8.5

3.1

144

39

8.0

.2 2.7

.0

.2

.37

.08

124.6

346

130

3.0

.5.4

.0

.4

.52

.12

2.7

.3

162

2.4

3.8

.0 5.8

.0

.12

.01 3.4

2.0

223

195.6

.1.6

.0

.15 K .05

0.25 0.68 1.97 3.37 8.61 2.90 4.16

8

3.4

.8

.1 1.2

.1

HCOs 0.13

.07

.02

.01 .02

0.30

.04 .28

.06

1.31

.27

.23

.02

.01

2.36

.81 .23

.01 .04

5.67

2.71 .08

.03

.01

2.66

.05

.11 .00

.09

3.66 C03 SO4 - .40 CI.. .16 F .01 NOi.. .01 PO4 - B

0.25 0.68 1.84 3.45 8.50 2.91 4.24

23 52 159 262 652 236 345

..micromhos at 25° C__ 36

6.5

7.2 <5

0.1 <0.1

2.6

.2 1.8

104.3

.1

206

7.1 11.7

323

7.9

7.2

742

7.4

11.7 <17

2.2

8.1

8.5

.3

.4 11543

.2

260

7.9

19.4 <10

<0.1

<0.1

14.3

.1 43

.7.0

394 pH... 6.5 7.6 °C.

imc per 1.. Ra mmc per 1.. u

Ratios by weight: Ca/Na 0.6

3.6

5.6

.2

.8

101.6

.05

3.8

.5

.4

184.9

(12

19 Mg/Ca .1 K/Na .6 HCOs/Ci... —

1.8.2

.0

40 scvci 3.4 F/Cl .02

EXPLANATION FOR TABLE 9

1. Spring, Mirror Lake, SW>$ sec. 26, T. 1 S., R. 9 E., Duchesne County, near Kamas,

Utah. Flows 20 gpm from Mutual Quartzite of Precambrian age. Unpublished

data in U.S. Geol. Survey files; analysts, R. A. Wilson and J. D. Weeks.

2. Drilled well, 50 ft deep, on Onbekend 226, northeast of Benoni, Transvaal, Union

of South Africa. In quartzite in Pretoria Series of Precambrian age (Bond, 1946); analyst, O. W. Bona.

3. Drilled well, 504 ft deep, Bucks County, Pa. In quartzite of Cambrian age (Green- man, 1955.)

4. Drip from roof of 6th-level raise, Cliffs Shaft iron mine, Marquette mining district, Mich. In quartzite of Precambrian age (Stuart, Brown, and Rhodehamel,

1954). See table 24, analyses 2 and 3 for analyses of saline waters found at depth

In Michigan copperland iron mines.

5. Well, 172 ft deep, Sioux Falls, SWH sec. 13, T. 101 N., R. 50 W Minnehaha

County, S. Dak. In Sioux Quartzite of Precambrian age. Unpublished data in U.S. Geol. Survey files; analysts, J. D. Honerkamp, J. D. Weeks, and J. O.

Johnson.

6. Drilled well, 179 ft deep, Sylacauga, NEM sec. 32, T. 21 S., R. 4 E., TaUedega

County, Ala. In Sylacauga Marble of Paleozoic or Precambrian age. Unpublished data in U.S. Geol. Survey files; analysts, J. E. Whitney and J. A.

Shaughnessy.

7. Drilled well, 95 ft deep, Baltimore County, Md. In Cockeysville Marble of Pre- cambrian age (Dingman, Ferguson, and Martin, 1956).
F26 DATA OF GEOCHEMISTRY

Table 10.Chemical analyses of ground waters from slate, schist, gneiss, and miscellaneous metamorphic rocks

1 Siamo Slate, Morris Mine, Mich. Mar. 25, 1952

2 Wissahickon

Schist, Arcadia, Md. May 12, 1954

3 Mica Schist, Wilkesboro, N.C.

Mar. 17, 1955

4 Wissahickon

Schist, Bucks

County, Pa. Apr. 28, 1953

5 Brevard Schist, Suwanee, Ga.

Jan. 8, 1957

6

Quartzitic

Schist, Vassalboro, Maine

Mar. 27, 1957

7 Schist and

Slate, Tonasket, Wash.

Oct. 25, 1954

8

Baltii Gneiss, Count

Apr. 3(

Rock type and location

Date of collection

Bucks

t, Pa.

, 1953

SiOj ppm

8.2

.0

.12

.50

epm ppm

14.0.16 .02

.00 1.18

3.1

1.2 3.3

.8

epm ppm

26 epm ppm12 epm ppm

21

.0

.11 .02 .00

.02

275.7 16

.7

138

9.6

2.5.5

.0

.0

epm ppm

13.0.09

.00

.00

epm ppm

18

.1.00

.00

epm ppm

17 epm

Al -.- Fe 2.6

.00 .04 .10 Mn

Cu - ZnCa - 1015.6

1310

5.04 .46

.57

.26

0.16 .10

.14 .02

10

1.6 6.5

1.0

45

3.0

2.5

.1 1.4

0.50 .13

.24 .03

22

9.1

214.4

26

48

34

.1 30

1.10

.75

.91 .11

1.35 .47

.70

.02

29

9.7 353.6

183

28

7.9

1.1.0.0

1.45 .80

1.52 .09

82

9.0

9.1 2.8

234

63

1.5

.1 1.2

4.09

.74

.40

.07

5.30

7.4 6.0

4.7 2.0

23

11

11.1

7.4

0.37 Mg - .41 Na - - .20 K .05

0.42 0.90 2.87 2.54 3.86 1 03

212

1285.2

.5.0

.0

21

1.2 2.4

.0

.4

.1

HCOs — 3.47

2.66

.15

.03

0.34

"""."62" .07 .00

.01

0.74

.06

.07

.01 .02

0.42

1.00 .96

.01

.48

2.26

.20

.07

.03

.00

3.00

.58 .22

.06

3.83

1.31 .04

.01

.02

0.38 COj—

SO4 .23 CI - — .31 F — .01 NOj - .12 PO4

Total anions 6.31 0.44 0.90 2.87 2.56 3.86 5.21 1.05

Total, as reported >489 48 99 207 221 310 421 89

Specific conductance micromhos at 25° C.

pH

674

7.4 7.2

416.3 92

6.9

3845.2

12.2

237

8.0

18.3 <10

0.2

0.3

1.7

.4.04 553.8

.2

344

8.0

10.6 <5

0.1 <0.1

0.8

.3

.1 233.5

.1

481

7.7 11.7 <14

0.1

1.4

9.0

.1.3

15642

.07

1207.2 Temperature "C. 12 2

Ratios by weight: Ca/Na 7.8.06

.8

4125

.1

0.9

.4

.2 8.8.5

.0

1.8

.3.2

181.2

.04

1.0

.4.2

.8

1.4.002

1.6 Mg/Ca 1.1 K/Na - - HCO3/CI 2.

1

SCVC1 1 F/Cl .009

Willii Gneiss mantic

Oct. 2

)nantic

, Willi-

, Conn.

5, 1954

10 Grenville

Gneiss, Bloom - ingdale, N.Y.

June 7, 1954

11 Port Deposit

Gneiss, Balti- more County, Md.

Mar. 25, 1953

12 Hornblende

gneiss, Paddysland, Transvaal, Union of South

Africa

1941

13 Gneiss complex, SE. ofNipton,

Calif.

Dec. 22, 1955

14 Quartz-hematite, Itablra

District, Minas

Gerais, Brazil

1 Green Yance

N.

5 Rock type and location ...

yville, C.

Si02 ppm

13

.1.09 .00

.00

.06

195.1 4.4 3.2

epm ppm

23 epm ppm

31

.2 2.7

.22

.01 .00 28

1.9

f 6.8

\ 4.2

121

1.4

1.0

.1.2

.0

epm ppm

86

.0

epm ppm

30

.4.00

.00

epm ppm

2.8

.2

.4.0

epm ppm

31 epm

AlFe .40 1.3 Mn

Cu

Zn. Ca 0.95

.42

.19

.08

337.2 }l.l

108

157.0

.2

1.65 .69

.05

1.40 .16

.30

.11

59

5799

5.8

506

17 1064.0

2.93

4.66 4.29

.15

90

69

722.0

616

132

76

.6

.6

.0

4.49

5.67 3.13

.05

.7

.7 1.3

.4

7.4

.4

0.03

.06 .06

.01

9540 }21

304

76

85

.0.3

4.74 Mg — 3.29 Na - K - .91

Total cations 1.64 2.29 1.97 12.03 13.34 .16 8.94

39

30

5.8

.7 15

.0

HCO3 0.64

.62 .16

.04

.24

1.77

.31 .20

.01

1.98

.03 .03

.01 .00

8.30

.35 2.99

.21

8.46

2.75

2.14

.03

.01

0.12

.01

4.98 CO3 —

SOt - - 1.68 CI 2.40 F .00 NO3 .6

.0

15

.01 .00 PO« — .0 Total anions 1.70 2.29 2 05 11.85 13.39 0.14 8.96

Total, as reported .. 135 195 199 940 989 654

Rppoifio ponrtiictaneA. . ., miCT omhosat 25° C-. 1786.9

13.3 <10

<0.1

0.6

4.3

1.2

.7 6.7 6.2

.1

2617.4

9.4 <10

<0.1

1.0

30

6.5

1926.911808.1

10.5 <34

<0. 1 37

1.2.8

.03

6.8

1.7.008

11 pH 7.4 5.8 °C_. Beta-gamma activity ic per I.. Ra ic Der 1 U . ue ner

1

Ratios by weight: Ca/Na. 4.1

.3.6

1211.4

.1

0.6

.6.06

4.8

.2.04

0.5

1 .3

18

4.5 Mg/Ca .4 K/Na

HCO3/CI 15

2.1.03

3.6 SCWC1 .9 F/Cl -. .0

1 Value considered dubious, possible contamination.

' Includes components mentioned in explanation.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F27

EXPLANATION FOR TABDE 10

1. Drip from roof of drift on 8th level, Morris Mine, Marquette Iron mining district, Mich. In Siamo slate of Precambrian age. Contains 2 ppm and 0.05 epm Sr and 2.9 ppm B, which are Included in totals (Stuart, Brown, and Rhodehamel,

1954).

2. Drilled well, 223 ft deep, Arcadia, Baltimore County, Md. In Wissahickon

Schist (albite fades) of Precambrian age (Dlngman, Ferguson, and Martin,

1956).

3. Drilled well, 700 ft deep, Wilkesboro, Wilkes County, N.C. In mica schist. Unpublished data in U.S. Oeol. Survey flies; analyst, 8. A. Phillips.

4. Well, 450 ft deep, Bucks County, Pa. In Wissahickon Schist of Precambrian

age (Greenman, 1955).

fi. Drilled well, 600 ft deep, Suwanee, Gwinnett County, Ga. In Brevard Schist of Cambrian age. Unpublished data in U.S. Geol. Survey files; analyst, D. E. Weaver.

6. Drilled well, 250 ft deep, Vassalboro, Kennebec County, Maine. In fine-grained quartzitic schist ol Precambrian(?) age. Unpublished data in U.S. Geol. Survey files; analyst, D. E. Weaver.

7. Spring, Tonasket, NWH sec. 20, T. 38 N., R. 26 E., Okanogan County, Wash.

Flows 4.5 gpm from schist and slate of Paleozoic age. Unpublished data in U.S.

Geol. Survey flies; analyst, J. D. Honerkamp.

8. Drilled well, 80 it deep, Bucks County, Pa. In Baltimore Gneiss of Precambrian

age (Greenman, 1955).

9. Drilled well, 180 ft deep, Willimantic, Windham County, Conn. In Willimantic

Gneiss of Gregory, probably of Carboniferous age or younger. Unpublished

data in U.S Geol. Survey files; analysts, J. E. Whitney and J. A. Shaughnessy

.

10. Drilled well, 304 ft deep, Bloomingdale. Essex County, N.Y. In Grcnville Oneiss of Precambrian age. Unpublished data In U.S. Geol. Survey files; analysts, J. A. Shaughnessy and W. F. White.

11. Drilled well, 167 ft deep, Baltimore County, Md. In Port Deposit granitic gneiss

of Precambrian age (Dingman, Ferguson, and Martin, 1956).

12. Warm spring, Paddysland, Transvaal, Union of South Africa. From hornblende

gneiss of Precambrian age (Kent, 1949).

13. Wheaton Springs, 12 miles southeast of Nipton, San Bernardino County, Calif. Flows 5 gpm from sillimanite-biotite-garnet gneiss complex (Olson and others,

1954). Unpublished data In U.S. Geol. Survey files; analyst, E. Zltnik.

14. Spring, in Sant' Anna area, Itabira district, Minas Gerais, Brazil. From ttabirite, a quartz hematite-mica rock, of Precambrian age; analyst, V. M. Campos

Paiva of Brazil Dept. Nacl. Producao Mineral, (written communication,

J. V. N. Dorr, 2d, and A. L. Miranda Barbosa).

15. Drilled well, 485 ft deep, Yanceyville, Caswell County, N.C. In greenstone of Paleozoic age (LeGrand, 1958).
F28 DATA OF GEOCHEMISTRY

Table 11.Chemical analyses of waters from unconsolidated sand and gravel

L 2 3 4 5 6 7 Alluvium, Plymouth, N.H.

Oct. 19, 1955

Alluvium, Cave Junction,

Oreg. Dec. 19, 1956

Alluvium,

Vancouver, Wash. May 17, 1949

Alluvium,

Clear Spring, Md.

Feb. 21, 1957

Alluvium,

Clinton, Iowa

June 8, 1954

Alluvium,

Pigeon Spring, W. of Lida, Nev.

Feb. 23, 1956

Alluvium, lake

beds, Bruneau,

Idaho Nov. 23, 1953

Si02 -. ppm

23

.0

.01 .03 6.8

1.2 2.6

.9

epm

0.40

.10

.11 .02

ppm

25

.0

.03 .00

6.4

7.8

5.8

.2

64

.8 5.5

.0

.7

.0

epm ppm

50 epm ppm

5.2

.0.10

.00 36

2.4

1.7

1.1

120

1.0 1.3

.1.8

.0

epm

1.80 .20

.07 .03

ppm ' 18

.1.04

.00

44

186.0

2.5

144

53

5.0

.1 28

epm

2.20

1.48 .26

.06

ppm

25

.0.05

.00

4520

162.6

207

35

17

.1 3.6

.0

epm ppm

77 epm

AlFe .02 .0 Ca 0.32

.64 .25

.01

155.2

4.2

5.6

64

112.9

.2 7.2

0.75

.43

.18

.14

2.25

1.65 .70

.07

3.6

.5 100

3.1

141

38

1224

2.9

0.18 Mg - .04 Na 4. 35 K .08

0.63 1.22 1.50 2.10 4.00 4.67 4.65

17

9.0

5.0

.1 1.2

.0

HC03 .. 0.28

.19

.14

.01 .02

1.05

.02

.16

.00

.01

1.05

.23

.08

.01 .12

1.97

.02

.04

.01

.01

2.36

1.10

.14

.01 .45

3.39

.73

.48

.01 .06

2.31 C03 SO4 .79 CI .34 F 1.26 NO3 .05 PO( B - - .3 Total anions 0.64 1.24 1.49 2.05 4.06 4.67 4.75

Total, as reported... 67 116 165 170 319 371 402

...micromhos at 25° C._ 72

6.1 9.4 <5

<0.1

0.1

2.6

.2

.3 3.4

1.8

.02

1136.5 140

7.6 10.0

208

7.8

10.0 <5

0.1 <0.1

21.06

.6 92

.8

.08

3978.0

12.2

6 <0.1

0.3

7.3

.4

.4 29

11 .02

446

7.8

13.9

455 pH 7.9 Beta-gamma activity _°C._

/i/ic per L.

33.9 <7

<0.1

<0.1

1.1 1.2

.03

12

.1.0

Ra nnc per 1.. TJ j»g perl.. Ratios by weight: Ca/Na . . 3.6

.3 1.3

223.8

.07

2.8

.4.2

12

2.1.006

0.04 Mg/Ca .1 K/Na .03 HCO3/CI 12 SO4/CI 3.2 F/Cl 2.0

8 Glacial outwash, Eden Valley, Minn

Nov. 2, 1955

9 Alluvium,

Enid, Okla. May 28, 1952

10 Alluvium, Te Aroha, New

Zealand

11 Alluvium, Mesa, Ariz.

Sept. 19, 1951

12 Glacial outwash, Columbus,

Ohio May 28, 1952

13 Alluvium,

Gaylord, Kans. May 3, 1950

14 Alluvium,

Date of collection

Douglas, Ariz. Dec. 13, 1955

Si02 ppm

24

.1.00

.08 86

27

5.1 3.0

epm ppm

21 epm ppm63

1.6

1.0

epm ppm

26 epm ppm20 epm ppm

28 epm ppm

27

.0.02

.00 3.2

1.0

262

2.4

149

16

125 210

2.0

2.5

.05

epm

Al

Fe.... .00 .08 2.3

.00

12643

13

2.1

440

1398.0

.7

.2

.42 Mn

Ca 4.29

2.22 .22

.08

49

13 105

3.0

384

2734

.3 7.8

2.45

1.07

4.57 .08

96

37

} 20

477

5.0 20

4.79 3.04

.87

58

22

1146

I 4.0

184

39

255

.0 2.9

2.89

1.81 6.35

.10

6.29 3.54

.56

.05

13216

53

7.6

302

18

18732

.3 18

6.59

1.32

2.31 .19

0.16 Mg .08 Na 11.40 K .06

Total cations 6.81 8.17 8.70 11.15 10.44 10.41 11.70

337

606.0

.0

.0.2

HCOj 5.52

1.25 .17

.00

.00

6.29

.56

.96 .02

.13

7.82

.10

.56

3.02

.81 7.19 .00

.05

7.21

2.89

.23 .04

.00

4.95

.60 3.89 .90

.02

.29

2.44 COs— .53 so< 2.60 CI 5.92 F .10 NO3 .04 PO< B .2 Total anions 6.94 7.96 8.48 11.07 10.37 10.65 11.63

Total, as reported— 548 644 721 737 794 795 800

micromhos at 25° 0.. 623

7.5

7.8 <17

0.3

0.7

17.3

.6 56

10.0

739

7.4

11807.7

18.3

885

7.6 13.3

943

8.4

13.3

1260 pH 9.0 Temperature ....°C. 20.0 <34 Ra

Mg per I.. <0.1 U 3.8 Ratios by weight: Ca/Na 0.5

.3.03

11.8.009

4.8

.4 0.4

.4.03

.7

.2

.0

9.7

.3

.2 55

17.09

2.5

.1

.1 9.4 5.8.009

0.01 Mg/Ca .3 K/Na... .009 HCO3/CI 24

.2

.7 SO( /Cl .6 F/Cl.. .01
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F29

Table 11.—Chemical analyses of waters from unconsolidated sand and gravel—Continued

15 Alluvium, Fresno County, Calif.

Sept. 18, 1951

16 17 Alluvium, Fort Morgan, Colo. July 28, 1948

18 19 Alluvium, Gila Bend, Ariz. Mar. 1948

20 Glacial deposits, N. of Malcolm, Iowa

Nov. 17, 1955

Alluvium, St. Croix Island, Virgin Islands April 15, 1940

Alluvium, NW.

of Pecos, Tex. Mar. 28, 1950

SIOi ppm

30 epm ppm14

.8.26

.05

12049

1226.2

epm ppm

26 epm ppm

35 epm ppm37 epm ppm

43 epm

Al

Fe - .93 Mn

Ca 63

54 1602.6

3.14

4.44 6.96

.07

5.99 4.03

5.31 .16

210

74 163

12

10.48 6.09

7.09

.31

3024

814

10

1.50 1.97

35.41 .26

307

82

} 1100

15.32 6.74 47.85

856

190 738

42.71 Mg 15.63 NaK

32. 10

14.61 15.49 23.97 39.14 69.91 90.44

160 339

439

6.0

.1 26

.0

348 828

351 625

1.6

17

327 152

1910

1510

HCOs 2.62 5.56 5.70 13.57 5.36 2.49 COa

SO< - 505

57

10.51

1.61 9.14.17

.01 .42

784

62

.7

2.1

16.32 1.75

.04

.03

7.31 17.63 .08

.27

575

18202.5

82

11.97

51.32

.13

1.32

39.77 CI 42.58 F - NOj - 1.3

1.1 .02 468 7.65 PO< - B .4 3.2 1.6

14.76 15.30 23.84 38.86 70.10 92.39

1030 1120 1680 2740 4340 5870

Specific conductance, -micromhos at 25° 0.. PH r- 13408.5 27.8

13307.4

11.9 <45

0.2

0.1

1.0

.4

.05

57

73.02

19807.8

12.8

6860 7560

7.1 Temperature Ra

-__°C__ 25.6 20.8 u

Ratios by weight: Ca/Na 0.4

.9

.02 2.8 8.9

1.3

.4.07 5.6

13

.01

0.04

.8

.01 1.3

.6.003

0.3

.3 1.2 Mg/Ca .2 K/Na .1 HCO3/CI .2

.3.001

.1 S0</C1 - - 1.3 F/Cl

EXPLANATION FOR TABLE 11

1. Well, 48 ft deep, Plymouth, Grafton County, N.H. In Quaternary alluvium

derived from igneous and metamorphic rocks. Unpublished data in U.S.

Geol. Survey files; analyst, B. V. Salotto. Also reported are Cu, 0.00 ppm; Zn,

0.00 ppm.

2. Drilled well, 40 ft deep, southeast of Cave Junction, SEH sec. 28, T. 39 S., R. 8 W.

Josephine County, Oreg. In Quaternary alluvium derived from igneous and

metamorphic rocks. Unpublished data in U.S. Geol. Survey files; analyst, R.

A. Wilson.

3. Spring, near Vancouver, NWHSWH sec. 33, T. 2 N., R. 2 E., Clark County, Wash. From Quaternary allvium derived from igenous rocks (Griffin, Watkins, and Swenson, 1956).

4. Spring, Clear Spring, Washington County, Md. Flows 100 gpm from Quater- nary alluvium derived from sedimentary rocks. Unpublished data in U.S.

Geol. Survey files; analyst, D. E. Weaver. Also reported are Cu, 0.00 ppm; Zn,

0.00 ppm.

5. Drilled well, 160 ft deep, Clinton, SEM sec. 22, T. 81 N„ R. 6 E., Clinton County,

Iowa. In Quaternary alluvium of the Mississippi River. Unpublished data in U.S. Geol. Survey files; analysts, R. A. Wilson, J. D. Weeks, and J. O. Johnson.

<5. Pigeon Spring, about 15 miles west of Lida, T. 6 S., R. 39 E., Esmeralda County, Nev. Flows 5 gpm from Quaternary alluvium derived from igneous and meta- morphic rocks. Unpublished data in U.S. Geol. Survey files; analyst, R. A.

Wilson.

7. Flowing well, 976 ft deep, in SEHSEVi sec. 24, T. 6 S., R. 5 E., near Bruneau

Village, Owyhee County, Idaho. In tuffaceous sand of Idaho Formation of f)robable Pliocene age, consisting of lake beds and terrestrial deposits underying basaltic volcanic rocks. Flows 25 gpm. Unpublished data in U.S. Geol. Survey files; analyst, J. F. Santos.

8. Well, 80 ft deep, Eden Valley, NEHSEHSEH sec. 1, T. 121 N., R. 31 W., Meeker

County, Minn. In Pleistocene glacial outwash. Unpublished data in U.S.

Geol. Survey files; analyst, E. Zitnik.

9. WeU 71 ft deep, Enid, NWH sec. 7, T. 23 N., R. 7 W., Garfield County, Okla

In Quaternary alluvium from sedimentary rocks. Unpublished data in U.S.

Geol. Survey files; analyst, J. M. Myers.

10. Cold Spring C, Te Aroha, Aroha subdivision, Hauraki, North Island, New Zealand. From Quaternary alluvium derived from late Tertiary lavas and tuffs (Henderson and Bartrum, 1913). See table 22, analysis 10, for Te Aroha ther- mal water high in Na, HCO3, and B.

11. Drilled well, 600 ft deep, Mesa, Maricopa County, Ariz. In alluvial valley fill of Quaternary age (Lohr and Love, 1954b).

12. Well, 117 ft deep, Nelson Road Waterworks, Columbus, Franklin County, Ohio. In Pleistocene glacial outwash gravel. Unpublished data in U.S. Geol. Survey

files; analyst, R. W. Leonard.

13. WeU, 50 ft deep, Gaylord, sec. 11, T. 5 S., R. 14 W., Smith County, Kans. In Quaternary alluvium derived from sedimentary rocks (Leonard, 1952).

14. Drilled well, 340 ft deep, Douglas, NWHNWHSEH sec. 10, T. 24 S., R. 27 E., Cochise County, Ariz. In Quaternary alluvial valley fill. Unpublished data

in U.S. Geol. Survey files; analyst, R. A. Wilson.

15. Drilled well, 1,529 ft deep, sec. 36, T. 19 S., R. 17 E„ Fresno County, Calif. In Quaternary alluvium (Krieger, Hatchett, and Poole, 1957).

16. Drilled well, 407 ft deep, 10 miles north of Malcom, NWMNEH sec. 11, T. 81 N.

R. 15 W., Poweshiek County, Iowa. In Pleistocene subglacial sand and

gravel. Unpublished data in U.S. Geol. Survey files; analyst, R. A. Wilson.

17. Well, 90 ft deep, Fort Morgan, sec. 26, T. 4 N., R. 66 W., Morgan County, Colo. In Quaternary alluvium (Krieger, Hatchett, and Poole, 1957).

18. Dug well, 11 ft deep, Annas Hope, St. Croix Island, Virgin Islands. In alluvium

derived from the Mt. Eagle Volcanics and perhaps, in part, from the Kingshill Marl (Cederstrom, 1950).

19. Well, 135 ft deep, near Gila Bend, sec. 8, T. 5 S., R. 4 W., Maricopa County, Ariz. In Quaternary alluvium (Krieger, Hatchett, and Poole, 1957).

20. Well 225 ft deep, 2 miles northwest of Pecos, Reeves County, Tex. In Quaternary

alluvium (Winslowand Kister, 1956).
F30 DATA OF GEOCHEMISTRY

Table 12.—-Chemical analyses of oil-field and gas-field waters dominated by sodium chloride

Analysis 1 Seaboard, Fresno County, Calif.

April 20, 1954

2 Cymric, Kern

County, Calif. June 14, 1955

3 Maine Prairie, Solano County,

Calif. May 11, 1955

4 Timbalier Bay,

Lafourche Parish, La.

1958

5 Katarzyna near Pomiarkach, Poland

6 Nflm« Of flflld nnrt lnnaHnn Przedgorza

Date of collection

Karpat, Galicia, Poland

Si02 ppm31 epm ppm

47

.4 1.2

.08

373

115 5,820

132

4.3

61

epm ppm

32 epm ppm255.0

8.6 il.l

.00 2,600

1,060 51,400

1935.5

147

epm ppm

2 epm ppm14 epm

Al. Fe

} "

14 Mn..

As... . Ca 543

126

6,75099

27.1 10.4 293.5 2.53

18.6 9.45 253.2 3.38

.62

2.8

21166 5,880

168

2.0 24

10.53

5.4 255.7 4.30

0.29

1.4

129.7 87.2

2,236

4.94 .79 8.15

908

935

89,900 3,090

45.3

76.9

3,91178.9

1,080

441 }>11,800

54.0 Mg_- 36.3 Na f 512 K

LiNH< 62 2.9 Total cations '337 288 278 2,470 . 4,110 . 602 HCOs 191

11,6000.4

58

23

70

3.13 635

1.6 9,8403.4 30

23

3

8.77

.00 .03 277.5

.18

.38

.18

565

12 9,230

1.2 32

23

9.26 147

2.6 89,700

1.1 86

19.00 7.9

.00 20

2.41 .00

.05 2,530

.06

1.08

.15

258 4.24 115 1.89 C03 SO< 0.25

260.3

0.06 .40

.18

9,230

139,000

192.2 3,920

104 21,000

2.17 CI.. 3270.02

.73

.18

596 F

Br 105 199

1.32

1.57

91 122

1.14

I .96 NO2-- NOj. 1.13 .05 0.7 0.01 .13 PO<

B.. 57 140 25

Total anions 332 287 270 2,530 4,120 . 602

Total, as reported '19,600 17, 100 16,300 145,000 244,000 34,800

Specific conductance micromhos at 25° C__ 31,500

6.9

25,800

7.5 49H

1.009

0.064

.31 .023 .00074

.054 .0002

.0003

.0030

.0023

.014

25,500

7.1 138,0006.6 70

1.104

0.051

.41 .0038

.00011 .0016 .000029 .000012 .00096

.00021 .00012

pH 6.8 Temperature °C._ Density at 20° C 1.0133

0.080

.23

.015

1. 0106

0.036

.31 .029 .0003

.061 .0013

.0001 .0035

.0025 .0027

1.185

0.010

1.03 .034

1.025 Ratios by weight: Ca/Na 0.090 Mg/Ca .41 K/Na

Li/Na HCO3/CI > .016 .0000 .00003

.0050 .0020

.0049

.0019

.066 .0055 SCWC1 .0050 F/Cl

Br/CI .0008

.0014 .0043 I/Cl .0058 B/Cl

Analysis 7 Hajduszoboszlo, SW. of Debrecen, Hungary

8

Tiszakiirt, SE. of Budapest, Hungary

1943(?)

9 Moinesti near

Moinesti, Rumania

10 North Makat, Kazakh district, USSR11 Mamft of flpld find ln<^t'nTM South Kwanto,

Date of collection

Chiba Prefecture, Japan

SiOj ppm

23 '4.2

/ 0.5

I 'Tr

epm ppm

95 Tr

29 Tr

' 5.8

17422 4,930

89 •84

40

epm ppm

5.2 epm ppm epm ppm epm

Al... Fe 24 '5.4 . Mn...

As

Ca.. 14

2.1 1,76024 0.4

0.70

.17

76.4.62 .06

8.68

1.8 214.5

2.28

12.1 2.2

1,990 836

47,200

169

99.3

68.8 2,053

4.32

3,210

1,690 70,900 279

160.2

139 3,083

7.14

170 325

'10,000

8.48 Mg 26.7 Na 435 K

LiNH. '23 1.3 22 1.22 47 2.60

78.0 242 2,230 3,390 473 HCO3- '1,360 22.3 1,120 Tr

24

7,4909.4 22

2.1

18.4 42 0.69 75 1.23 832 13.63 C03 SOi 1.6

1,950

.03

55.1

.50 211.2

.60

.28

.02

24

78,800

.50 2,222 <2 - CI 120,000 3,380 16,200 457 F

Br 248.4

.29

.07 127 ill

1.59

.09 1271.4

1. 58

.01 81 132

1.02

I 1.04 NOj

NOj... PO» Tr

B... 5.4 89 35 . 14 - 77.8 231 2,220 3,380 473 Total, as reported 5,180 14,200 129,000 196,000 27,800

Specific conductance mi :romhos at 25° C.

pH— 7.8 °C- 73 20 Density at 20° C 1.160

0.045

.53 .0039

' 1.02 Ratios by weight: Ca/Na 0.0080

.15 .014 .0002

.70 .0008

0.035

.13

.018 .017

.15 .0032

.0012

.0029 .00028 ni2

0.042

.42

.0036

017 Mg/Ca 1 9 K/Na

Li/Na HCOj/Cl» .00053

.00030 .00062 051 S04/C1-. .000 F/Cl...

Br/CI .012 .0043

.0028

.0016

.00014

.0010

.00001 0050

I/Cl 0081 B/Cl.. nnns7

' Components mentioned in explanation of table.

» Includes COi as HCOj.
CHEMICAL COMPOSITION OP SUBSURFACE WATERS F31

EXPLANATION FOR TABLE 12

1. Seaboard Oil Co. well S.T.U. 35-13, 6,300 ft deep, sec. 13, T. 15 S., R. 17 E., Fresno County, Calif. Producing from Eocene sandstone. Collected by R. E. Thronson and W. B. Mitchell, Jr., California Division of Water Resources; analyzed by D. D. Watson, U.S. Qeol. Survey. Included in totals is Ba, 12 ppm (0.17 epm). Analysis not previously published.

2. Honolulu Oil Co. weU 22-166, 4,952 ft deep, Cymric oil field, NWKSEM sec. 22, T. 29 S., R. 21 E., Kern County, Calif. Some mercury has been recovered from

this well (Stockman, 1947). Producing from Oceanic Sandstone of Oligocene

age; bottom-hole temperature 81°C, discharge temperature 49H°C. Analyzed

by C. E. Roberson, U.S. Geol. Survey; H2S not found; spectrograph^ analysis

of evaporated residue, by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 18,000; Al, 0.2; Fe, 0.2; Mn, 0.2; Cu, 0.04; Li, 2.6; Rb, 0.2; Sr 80; Ba, 7.1. Analysis not previously published. See table 28, analysis 1, for gas analysis by U.S. Bureau of Mines.

3. Amerada Petroleum Corp. Peters gas well 1, Maine Prairie gas field, sec. 10, T. 5 N., R. 2 E., Solano County, Calif. Producing from depths of 5,590 to 5,630 ft in the Meganos Formation of Eocene age (C. R. McClure, written communication). Collected by C. R. McClure, California Division of Water

Resources; analyzed by R. O. Hansen, U.S. Geol. Survey. Analysis not

previously published.

4. Gulf Oil Corp. well PP 19, 7,790 ft deep, Timbalier Bay oil field, T. 23 S., R. 21 E., Lafourche Parish, La\ Producing from depths of 5,904 to 5,910 ft where temperature was 70° C in Pliocene shallow-shelf and shoreline sands with shale

streaks on north flank of Timbalier Bay salt dome, with salt at depth of 7,782

ft. Collected with cooperation of Dr. Marcus Hanna, who believes that brine

is not directly influenced by contact with the salt of the dome (written communication). Analysis by H. C. Whitehead of U.S. Geological Survey; also determined Cu, 0.02 ppm; Zn and Pb, 0.00 ppm; spectrographs analysis of evaporated residue by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180° C, 152,900; Al, 1.5; Fe, 0.8; Mn, 1.1; Cu, 0.3; Ni, 1.5; Cr, 0.6; Li, 2.3; Sr, 11; Ba, 150. Analysis not previously published.

5. Katarzyna oil field near Pomiarkach, Poland, from a depth of 300 ft in the Argiles

Saliferes Formation of Miocene age (Katz, 1928, p. 13-15, 49-52). Analysis converted from mg per 1; this water has the highest iodine content reported by

Schoeller (1956, p. 100-113) in oil-field brines.

6. Well 29, 1,550 ft deep, Przedgorza, Galicia, Poland, probably in lower Tertiary

rocks (Chajec, 1949, p. 367; Emmons, 1931, p. 631). Analysis converted from mg per 1. Alkalies determined by difference of anions and cations.

7. Artesian test well for gas, 3,600 ft deep, Hajduszoboslo gas field 6 miles southwest

of Debrecen, Hungary. Discharges 450 gpm water (Emszt, 1928, p. 146) prob- ably from Cretaceous limestone (Szalai, 1951, p. 181). HCO3 converted from

reported equivalent CO3; Al, Mn, and Li from analysis of very similar water from well 2, 6,665 ft deep, probably from Triassic strata (Papp, 1951, p. 155; Szalai, 1951, p. 181). Abundant gas (table 28, analysis 2) accompanies water.

8. Tiszakiart, about 60 miles southeast of Budapest, Hungary. Production from

about 7,500 ft from Triassic limestone (Telegdi-Roth, 1950, p. 81; Vajk, 1953,

p. 40-42). Li and As are surprisingly high and should be checked; trace of Cu

and Sr reported. Analyzed by J. Bodnar, Dec. 1943.

9. Well 24, 2,050 ft deep, of Soc. Steaua Romana in the Moinesti field of northeast Rumania. Produces from Oligocene rocks. Naphthenic acids and trace of Sr reported present (Petrescu, 1938, p. 26-28). In 15 other analyses, I is as much

as 167 ppm and NH« as much as 372 ppm.

10. Well 43, 1,750 ft deep, North Makat, Kazakh district, U.S.S.R., near northeast

shore of Caspian Sea. In Permo-Triassic rocks (Sulin, 1948, p. 410-411). Analysis expressed in mg per liter and equivalents per liter converted to ppm.

11. Well A-226, 1,800 ft deep, South Kwanto gas fields, Boso Peninsula, Chiba Prefecture, Japan, 2.5 km northeast of Otaki. Brine produced for iodine and dis- solved gases (30.7 cc per 1; see table 28, analysis 3) from sandstone and shale of Upper Pliocene Otadai and Kiwada Formations. Temperature 20° C; anal- yses reported in g per 1, converted to ppm by assuming a density of 1.02; 4.3 ppm

of total Fe reported as ferrous iron; Na and K not reported, here calculated by

difference.
F32 DATA OF GEOCHEMISTRY

Table 13.

Chemical analyses of oil-field waters and other deep-well brines high in sodium and calcium chlorides

Analysis 1 [ 3 4 5 6 7 Raisin City, Fresno County,

Calif. Apr. 20, 1954

South Mountain, Ventura

County, Calif.

West Bay, Plaque- mines Parish, La. June 17, 1958

Barnhill, Wayne

County, 111. Paintsville, Johnson County, Ky.

Lee, Calhoun

County, W. Va.

1937

Michigan Basin (Dundee Limestone) Mich.

S1O2 —

ppm

36 epm ppm epm ppm

16

3.1

110 '30

9,210

1,070 '180 117

63, 900 869

19 188

epm ppm

16

7 10

7,130 2,400

epm ppm

5.9 8.6

4.4

epm ppm epm ppm

<50 epm

AlFe 7 18

6.0

32, 800 6,440 940

12

51, 500 2,46023

202

Mn

Ca..._ 2,190 832

109.3 68.4

5,890

69 293.9 5.7

459.6

88.0 355.8197 1,340 368

4166

/8.010

\ 96

66.9 30.3.94

.96

348.4 2.46

8,450

2,040

1 2, 610 1,550 28,900 298

421.7

16859.6 20.6

1,2577.62

1,637 Mg 530 Sr 21.45 Ba 42

14,800 251

0.61 643

6.42

.17 Na.. - 4,140

117

180.1 2.99 2,780

22.23 2.7

10.4

} 149, 000 2,133

2,240 K 62.9 Li 3.3 NHi 31 1.7 167 9.26 11.2

51

829 483 3,360 2,700 450 1,930 4,510

193

0.0

29, 0000.6

10821

44

17

18 17,000

HCO3 3.16 115 136 120

8180.03

1.35

.17

0.28

.00

.37 479

1.88 2.23 1.97 0.84 CO3

SO4 153 124,0001.4

393

18.00

9.4

3.18

3,500

.07

4.91 .14

82

1 95, 400

1.71 2,690 15, 500 68,400

.00 1,929

140 160,000 <4

1,310

8

2.91 CI 437 4,510 F

Br 9121 1.14 .17 920.41.15

.00 3734 4.67.03

16.4

I .06 N02 NO3 .71 64 1.03 PO( B .. . 8.3 Tr 60 H2S nil

113, 000

823 481 3,510 2,690 440 1,930 4,530

47,600 27,400 1200,000 154,000 25, 700 256, 000

Specific conductance

68,600

6.4 158,0006.3 '87M

1.151

0.14

.12 .014

.00030

.00090 .0012

.00001 .0032 .00015

. 000076

pH... 7.2 7.3 Temperature, °C

Density at 20° C_. 1.034

0.15

.38 .017

• 1.015

1.4.012

.028

1.0156

0.17

.27

.012

1.072

0.29

.24

.010

1.214 Ratios by weight: Ca/Na 0.14

.34 0.64 Mg/Ca .20 K/Na .048 Li/Na .00045 HCOs/CP .0066

. 00000

.00002

.0037 .00072

.00028

.0010

.0011 .0014

. 00085

.0077

.00000 .00075 SO«/Cl . 00000 .00087 F/Cl <. 00003 Br/CI .0053

.0012

.0059

. 00003

.0055 .00006

.0081 I/Cl .00005 B/Cl.. .00038

Analysis 8 Michigan Basin

(Sylvania Sandstone) Mich.

9 Playa Huincul, Neuquen Territory, Argentina

10 Hollviken, Scania district, Sweden

Apr. 18, 1944

11 Gevelsberg, Ruhr district, West Germany

12 Boryslaw area, Poland

1926

13 Name of field and location Polasna-KrasnoDate of collection

kamsk, NW. of Molotov City, USSR

SiOa ppm

<20<5

22

2.0

74, 800

9,960

2,650

nil 22,500 19,120

70

506

epm ppm

131635

epm ppm

8 epm ppm epm ppm

7 epm ppm epm

A1-- Fe 43

15

12, 700

1,100

9

1 28,100 919

5.5 28

7820

6,890

571 235

13 20,500 3,950

0.2

716

106 Mn

Ca 3,724

81960.5

9,990 918

84 282

21,70032

3.9

498.5

75.5

1.92

4.11 944

.82 .56

634

90.5

.21

.01

1,22223.5

.79

1.55

343.8

47.0

5.36

.19

982

101.0

.03 39.7

17,300 1,880 863.3

155

16, 000

3,750

798 Mg. 308 SrBaNa 979 233.3

10.1 28.1

75,000 3103,260

7.93

61, 000

1,080 2,654 K..._ 27.6 LiNH« 156 8.65

Total cations 5,850 1,530 1,970 1,430 4,290 3,800 HCOj 876 14.36 187 3.06 61 0.84 COi

SOt 40 208,000 <4

2,910

40

.83 5,870

10 69,400

4 3583

} »

<1<1

.21

1,957.21 4.48

.02

.27

48,900 340152,000 7.084,290 474134, 000

9.87 CI 54, 100 1,526 1,379 3,780 F

Br 36.4

.32 302

.38

.02 2.8

0.3

.04 .00297

15 3.72 1.12

614

17 7.68

I .13 NOj..

NOi

PO« 0.1 B 380 0.8 H>S >0.1 1 140 Total anions 5,910 1,530 1,960 1,390 4,300 3,800

331,000 87,200 113,000 82,800 247, 000 217,000

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F33

Table 13.Chemical analyse s of oil-field waters and other deep-well brines high in sodium and calcium chlorides--Continued

8 Michigan Basin

(Sylvania Sandstone) Mich.

9 Playa Hulncul, Neuquen Territory, Argentina

10 Ilbllviken, Scania district, Sweden

Apr. 18, 1944

11 Oevelsberg, Ruhr district, West Germany12 Boryslaw area, Poland

1926

13 Polasna-KrasnoDate of collection

kamsk, NW. of Molotov City, USSR

pH 6.4

35 27 Density at 20°C. 1.292

3.3

.13

.41 .003

1.088

0.45

.086

.033 .0002

1.193

0.23

.11 .0041

1.172 Ratios by weight: Ca/Na 0.46

.091 .0015

. 00018

0.34

.082 .19

. 00001 .018

. 00000

0.26 Mc/Ca .23 K/Na .018 Li/Na.... HCO3/CI « — .0012 .0022 .00038 StWCl -. - .0019 <. 00002

.014

.00019

.0018

.00014

. 00006

.0052

. 00004

.0035 F/Cl...

Br/CI.- . 00055

. 00004

. 000057

. 00006

.00002

.0020

. 000099

.0046

I/Cl . 00013 B/CL

1 Components mentioned in explanation of table. > Estimated. ' Includes CO3 as HCO3. EXPLANATION FOR TABLE 13

1. Seaboard Oil Co. well S.T.U. 305-13, Raisin City, sec. 13, T. 15 S., R. 17 E., Fresno County, Calif. Water from depth of 4,700 ft; well produces from Miocene Tar Formation (same analysis as in White, 1957b, p. 1664, but locality incorrectly called Seaboard Field). Collected by R. E. Thronson and W. B. Mitchell, Jr., of California Division of Water Resources' analyzed by D. D. Watson,

U.S. Geol. Survey; gas analysis of table 28, analysis 4 (Anderson and Hinson,

1951, p. 50-51) from nearby well from depth of 4,975 ft. 2. Well H. No. 6, South Mountain, Ventura County, Calif.; water from depth of

3,285 ft in sandstone of the Sespe Formation of upper Eocene or Oligocene age (Hudson and Taliaferro, 1925, p. 1076). Recalculated from analysis showing

hypothetical combinations, in grains per gallon.

3. Gulf Oil Corp. well 28-E, 9,500 ft deep, West Bay oil field, Buras Levee district,

sec. 35, T. 22 S., R. 30 E., Plaquemines Parish, La. Producing from 8,366 to

8,374 ft; bottom-hole temperature 87H° C, temperature of sample when collected 42° C. Producing from silty Miocene sandstone, probably of deep-water

deposition, about 200 ft from salt near crest of West Bay salt dome, believed by Dr. Marcus Hanna to be a deep-seated dome generally lacking in an anhydrite cap and little affected by solution of salt (written communication). Hanna believes that the water sample has not been In contact with the salt dome. Collected June 17, 1958, with cooperation of Hanna; analyzed by H. C. Whitehead of U.S. Geol. Survey. Also reported, in ppm: Cu, 0.00; Pb, 0.60, Zn, 5, As, 0.00. Spectrographs analysis of evaporated residue, by Nola B.

Sheffey, converted to ppm in original water: evaporated residue at 180° C,

214,200, Al, 4.3; Fe, 51; Mn, 30; Cu, 0.4; Ni, 2.1; Li, 9.8; Sr, 180; Ba, 17. Analysis not previously published.

4. Well about 2 miles north of Barnhill, sec. 31, T. 2 S., R. 8 E., Wayne County,

111. Water from depth of 3,374 to 3,385 ft In Ste. Genevieve Limestone of Mississippian age (Meents, Bell, Rees, and Tilbury, 1952, p. 33). Highest CI

content reported in about 500 analyses; Na-)-K determined by difference;

total Fe, unfiltered, 0.6 ppm.

6. Brine from Pennsylvanian sandstone, Paintsville, Johnson County, Ky.; depth

not stated. Apparently from an artesian well, producing 2 gpm of brine (Hauser, 1953, p. 67).

6. Tom Campbell farm well 2, 1H miles south of Creston, Calhoun County, W.

Va.; water from depth of 1,402 ft near top of Salt Sand of Pottsville Series of Early Pennsylvanian age (Price, Hare, McCue, and Hoskins, 1937, p. 36, 67,

98). Highest Sr content of about 180 analyses). Analyzed by J. B. McCue, West Virginia Geol. Survey.

7. Location not specified" analysis reported by Dow Chemical Co. to be typical of commercial-brine analyses from vuggy Dundee Limestone of Middle Devonian

age, Michigan basin, Michigan, from depths of 1,500 to 4,200 ft. Most components are recalculated from hypothetical chemical combinations but some were

given as ions.

8. Location not specified; sample reported by Dow Chemical Co. to be a typical brine from Sylvania Sandstone of Early Devonian age, Michigan basin, Michigan, from depths of 2,000 to 5,500 ft. Most components are recalculated from

hypothetical chemical combinations but some are given as ions; also reported

are Cu, <1 ppm; Pb, <5 ppm; and Ni, <5 ppm. K content is notably high. See table 4, analysis 15 for shallow water of low salinity from Sylvania.

9. Test well 23, on border of Playa Huincul oil field, Neuquen Territory, Argentina; producing thermal water from depth of 2,640 to 2,850 ft from Upper Jurassic sandstone associated with shale (Sussini and others, 1938, p. 157; Emmons,

1931, p. 611). Analysis reported with metals given as oxides, converted to ions.

10. Hollviken 1 brine well, Scania district, southernmost Sweden, producing from

depth of 4,050 to 4,140 ft from sandstone of Early Cretaceous (Cenomanian)

age (Brotzen and Assarsson, 1951, p. 222-223; Schoeller, 1956, p. 182-183). Brines

at deeper levels in Cenomanian and underlying Triassic rocks are similar in composition but generally increase in salinity downward. Analysis converted from mg per 1; Cs, 5 ppm.

11. Brine well, near Oevelsberg in Ruhr area, West Germany, producing from depth

of 3,275 ft (Komlev, 1933, p. 208). Rocks at surface are probably of Cretaceous

age; brine probably is from Triassic rocks. K content is surprisingly high; Ra, 1.80 wic per 1; As, 0.06 ppm.

12. Ullman well, in the Boryslaw area, Poland, producing from a depth of 3,100 ft from rocks of Couches de Polanica of upper Oligocene age (Katz, 1928, p. 18, 20). Analysis recalculated from mg per 1; I content is intermediate in range

reported by Katz.

13. Krasnokamsk well 62, in the Kama River region, about 25 miles northwest of Molotov City, U.S.S.R., producing from depth of 3,240 to 3,250 ft from Carboniferous limestone containing some CaSO* and NaCl; overlain by nearly

400 ft of impermeable anhydrite (Kuznetsov and Novikov, 1943, p. 62; Kuznetsov, 1943, p. 151-154; see also Schoeller, 1956, p. 186). All waters of field are high in HjS and contain as much as 900 ppm.
F34 DATA OF GEOCHEMISTRY

Table 14.-—Chemical analyses of waters high in sulfate and bicarbonate associated with oil fields

1 Midway Sunset, Kern

County, Calif. June 22, 1954

2

Coalinga, Fresno County, Calif. Oct. 25, 1955

3

Pilot Butte, Fremont

County, Wyo.

June 18, 1959

4 South Casper Creek, Natrona County, Wyo.

Sept. 15, 1958

£ Coalinga County

Jan. 8

, Fresno Date of collection

, Calif. ,1952

SiOj ppm

59 epm ppm

22 epm ppm

36

1.4

.75

.00

.00 216

99

19.6 >.3

3,250

782.3

11

epm ppm

16.64

.24

.00 .00 266

82'5.7

1.12

378

21.4

.0

epm ppm

61 epm

AlFe - Mn

AsCa - — 501 103

25.0 8.47

407

491 20.3

40.4

10.78 8.1413.27 6.74 40

35

2.0 Mg — 2.9

Sr —

BaNa - 1,0209.8

44.4 0.25

1,800

10 78.3.26

141. 38

2.00

.33

.61

16.44

.64

.06

1,57033

68.3 K — .84 LI

Total cations 78.1 139 163. 24 37.05 74.0 HCOa 112

1,590

1,3000.3

7.7

2.3

1.84

.00

33.1 36.7

.02

.10

.02

336

5,760

500

1.0

5.51

.00 119.9

14.1.05

201

10 6,650 596

6.0

.7 1.3

.00 2.2

.03 26

3.29

.33

138. 45

16.81 .32

.01

.01

156

1,170 3703.5

1.6

.0.00

.0.03

.44

2.56 2,900

415

6120.6

47.5 COj .00 S04 24.36

10.43 .18

8.64 CI - 17.26 F . - .03 Br

IN02 NO3 343 5.53 11 .18 .04 1.4 .02 P04 B 3.9 9.6 13 H2S 62 24

77.3 140 159.26 37.53 73.5 Total, as reported — 5,050 9,350 11,200 2,490 5,680

Specific conductance micrombos at 25° C.

pH -

7 040 13 30C S 290

7.6 25

0.49

.21 .0096

8.3 7.6

Ratios by weight: Ca/Na 0.23

1.2.0056

0.066

.46 .024

.00071 .37

11 .010 .0012

.0022 .044

0.70

.31 .056

.001

.42 3.2

.0095

.0041 .000

.0012

0.025 Mg/Ca .88 K/Na .021 Li/Na HCO3/CI' .086

1.2

.00023

.0059 .0018

.0030

.67 12

.002

4.7 SOt/Cl .68 F/Cl .0001 Br/CI

I/Cl B/Cl .019 .021

Analysis 6 East of Salt Creek, Natrona County, Wyo.

June 16, 1958

7

Ellis Pool, Alberta, Canada

Jan. 8, 1958

8 Bukkszek, Hungary

I Mezokoves

1 Name of field and location 1, Hungary

Date of collection

SiOi ppm

32

1.4.84

.00

.01 3.2

1.5 1.7

1 1.3 1,5504.3

.2

.0

epm ppm

13.85

.04 .00

.23 9.6

151.9 12.2

1,74020

1.2 2.6

epm ppm

550.3

3.3

epm ppm

39 Tr

epm

Al

Fe... Mn

As..

Ca.. 0.16

.12 0.481.23

154

162

.3

.9 9,090

151Tr

3.9

7.68

13.3

.01

.01 395.4 3.86

.00

.22

193653.1

0.04 324

62

1.2 0.7

9.63 Mg 5.3 Sr .07 Ba .00 Na 67.42

.11 .03

75.69

.51 .17

.14

14.09 K 1.58 Li .17 NH, .04 67.84 78.22 420 30.9 HCO3 2,710

22

710

147.3

4.1.00 .0

.12

7.4

44.42 2,650

84 223

830

5.8

3.5.6

.00

.0.12

1.4

43.43 2.80

4.64

23.41

.31

15,200 249 1,250 20.5 COt

SO« .46 20.02

.74

.09

.03

893 5,370

18.59

151.4 26 343

0.54 CI 9.67 F

Br 29

15 .36.12 Tr

.05 .00

I .00 NO2

N03 PO« Tr .3 2.9

1,030

.00 B

COi 3,100 HjS .6 65.76 74.59 419 30.7 6,070 5,600 1 34, 200 1 3, 360 t25° C. 6,8008.0

6,6708.6 37

0.0055

1.6

.011 .00069

3.4

.27 .0070 .0042

.00072

.0017

pH

Ratios by weight: Ca/Na

... °C_. 19.5

0.017

1.05 .017

0.0021

.47 .0028

.00013 3.8

.031 .020

.010 nnss

0.60 Mg/Ca .34 K/Na .19 Li/Na... .0037 HCO3/CI1 2.8

.16 3.6 SO</01 .076 F/ClBr/CI .0054 I/Cl 0097 .0001 B/Cl .10 .0086

1 Includes COj as equivalent HCOa.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F35

EXPLANATION FOR TABLE 14

1. Irrigation well, 250 ft deep, on border of Midway-Sunset oil field, sec. 34, T. 31 S., R. 24 E., Kern County, Calif. Sulfate water used for irrigation. Collected by

J. M. Morris, Jr., California Division of Water Resources; analyzed by D. D.

Watson, U.S. Geol. Survey; analysis not previously published.

2. Sulfate well water, 70 ft deep, west border of Coalinga oil field, NEM sec. 10, T. 20

S., R. 14 E., 6 miles northwest of Coalinga, Fresno County, Calif. In probable marine sandstone of Etchegoin or the Jacalitos Formation, Pliocene age. Sample

collected by California Division of Water Resources, analyzed by U.S. Qeol. Survey; analysis not previously published.

3. British American Oil Producing Co. well 1-E. T., Pilot Butte oil field north west of Riverton, NWM sec. 22, T.3N..R.1 W., Fremont County, Wyo. Drilled in 1942 to 6,395 feet; producing from depths of 5,804 to 5,839 ft and 6,036 to 6,258

ft from Embar Formation of Permian and Triassic age. Collected by K. P. Moore, analyzed by H. C. Whitehead of the U.S. Geol. Survey, who also reported

0.00 ppm Cu, Pb, and Zn; density is 1.007. Quantitative spectrograpbic analysis by Nola B. Shefley, converted to ppm in original water: Cu, 0.08; Ag, 0.003; Fe,

0.2; Cr, 0.01; Al, 0.2; Ti, 0.03; Sr, 9.6; Ba, 0.3; Li, 3.7; Rb, 0.1. Mo, W, Oe, Sn, Pb, Zn, Cd, Sb, Mn, Co, Ni, V, Ga, La, Zr, Be, and Cs are below detection

limits in solids. Analysis not previously published.

4. Pure Oil Co. well No. F-ll, South Casper Creek, west of Casper, Natrona County, Wyo., producing from Tensleep Sandstone of Pennsylvanian age from depths

of 2,585 to 2,630 ft. Collected by K. P. Moore; analyzed by H. C. Whitehead of the U.S. Geol. Survey, who reported Pb, 0.01 ppm; Cu, 0.00 ppm. Quantitative spectrograph^ analysis, by Nola B. Sheffey, converted to ppm in original water: Cu, 0.005; Mn, 0.01; Ni, 0.04; Fe, 0.03; Cr. 0.005; Al, 0.03; Ti, 0.008; Sr, 5.7; Ba,

0.12. Ag, Mo, W, Ge, Sn, Pb, Zn, Cd, Sb, Co, V, Ga, La, Zr, Be are below

detection limits in solids. Analysis not previously published.

6. Carbonate waste water, irom East Side area of Coalinga oil field, SWM sec. 35, T.

19 S. ( R. 15 E., Freson County, Calif. Most oil production of this area is from

Temblor Formation of Miocene age, from stratigraphic traps on east flank of Coalinga anticline. Collected by California Division of Water Resources; analyzed by U.S. Geol. Survey; analysis not previously published.

6. Sinclair Oil and Gas Co. Well 2, 6,014 It deep, northeast of Edgerton, in SWH

sec. 10, T. 40 N., R. 78 W., Natrona County, Wyo. Producing at depths of 4,566

to 4,604 ft from Frontier Formation of Upper Cretaceous age. Collected by

K. P. Moore; analyzed by H. C. Whitehead of the U.S. Geol. Survey, who

reported 0.00 ppm.Pb and Cu. Quantitative spectrograph^ analysis by Nola

B. Shefley, converted to ppm in original water: Cu, 0.06; Ni, 0.04; Fe, 0.1; Cr,

0.003; AL 0.1; Sr, 0.7; Ba, 1.3; Li, 0.3. Ag, Mo, W, Ge, Sn, Pb, Zn, Cd, Sb, Mn,

Co, V, Ga, La, Ti, Zr, Be, Rb, Cs are below detection limits in solids. Analysis not previously published.

7. Conrad Province Well 57-33b, sec. 33, T. 5, R. 15, west 4th meridian, Alberta, Canada. Drilled in 1946 to 3,026 ft; producing from a depth of 3,016 to 3,026 ft from Ellis Sandstone of Jurassic age. Collected by Brian Hitchon of the Research

Council of Alberta; analyzed by H. C. Whitehead of the U.S. Geol. Survey, who also reported 0.00 ppm Cu, and Pb; 0.03 ppm Zn. Quantitative spectro- graphic analysis, by Nola B. Sheffey, converted to ppm in original water: Cu,

0.03; Ag, 0.04; Sn, 0.2; Ni, 0.04; Fe, 0.04; Al, 0.09; Zr, 0.01; Sr, 0.9; Ba, 2.2; Li, 1.1. Mo, W, Ge, Pb, Zn, Cd, Sb, Mn. Co, Cr, V, Ga, La, Ti, Be, Rb, and Cs are below detection limits in solids. Analysis not previously published. Bicarbonate water, from well located at Bukkszek, about 60 miles northeast of Budapest, Hungary; water from depth of 450 ft from beds of probable Cretaceous

age (Telegdi-Roth, 1950, p. 80, 83). Analyzed by K. Ernst, May 1937. Bicarbonate water, from well located at Mezokovesd, about 70 miles east-northeast

of Budapest, Hungary. Water from a depth of 2,870 ft, probably from Cretaceous

or Triassic limestone (Telegdi-Roth, 1950, p. 80, 83). Analyzed by J. Karpat, May 1939. Also reported are ppm, Ti, Cu, As, and HaS; COS, 20 ppm.

8.

9.
F36 DATA OF GEOCHEMISTRY

Table 15.Chemical analyses of spring waters similar in composition to oil-field brines of the sodium chloride type

1 Tuscan, Tehama

County, Calif.

Dec. 14, 1956

2 Wilbur, County

Aug. a

Colusa

, Calif.

,1949

3 Tolenas County

Oct. 3

Solano

, Calif.

,1956

4 Mercey, Fresno County, Calif.

June 13, 1955

5 e Bad Ham

Westp

Gern

Name of springs and location......... Stinking, Springs Box Elder County, Utah

April 5, 1958

m, West

halia, lany

SiOi ppm

150.9.2

.3

19

17 »13

72

7,900

59 •2.0 59

epm ppm

190 10.3 i.l 1.3

1.4 58'.8 •1

9,140 460

14 303

epm ppm

75 0.2

i.l

epm ppm

75 epm ppm48

1.05 .03

.00

946

297 131

14.1

12,600

5716.9 40

epm ppm

10 Tr

20

.2

1,730 262

65 Tr

29,400 360

1133

epm

AlFeMn

Ca 0.95

1.4.30

1.05 344.1

1.61 .29 3.3

0.07 4.7

.18

.01 397.4

11.76 2.0

16.8

454 239

12

1 1.3 6,100

1819.0

0.2

22.65

19.7.27

43

nil9

2.15 47.20

24.4

86.3 Me 21.5 Sr .21 1.47 BaNa 265.4 4.63

1.30

.01

830

7.1 0.1

5

36.1.18

.01 .28

64814.60 .99 2.21,279 K 9.21 LI 1.6 NH« 1.8

353 433 314 38.9 637 1,400

1,060

154 7,390

23

6,340

.3

1331

5

324

111

HCOs 17.4 1,530 5.13 .00

121.2.00

.48

103.9 0.21

1.03 .10

5.31 25.1 COj

SO4 .01 2.31 1,430 29.8 CI 11,800

6 15.3

> 1.3

333

.26

.07

.01

11,000

1.1 15

116

310

.06

.19

.13

7,510

220

3

165

211.8

.11 .25

.10

1,300

.4 None (?) 20

36.7.02

21, 600

1.9

15

1.3.00

.0.00 3.6

609.10

.19

.01

47, 700 1,345 F

Br 17.2 0.21

I.. * .16 .00 NOj

NOj 2.66 .6 .01 POi 0.5 •201

0.02 .2 770.00 B 292 360 10 HjS 172 178 60 Tr

356 432 319 38.2 617 1,400

21.600 29, 100 21, 500 2,350 36, 600 83,300

Specific conductance micrombos at 25° C pH

32,500

8.4 28H

1.009

0.0024

.89 .0074 .00025 .12

.0000

.00036 .00045

.00011 .017

33,600

7.2

671.016

0.00015

41

.050 .0015 .66

.0021 .00009

.0014 .0015 .036

24,600

6.7 20.0

1.012

0.074

.53 .029

.0015

.85

.00004 .0003

.0026 .0017

.048

2,1608.6

46

53,9006.7

48

1.025

0.075

.31 .045

. 00055

.015

.0051

. 000088

. 00069

. 000060

. 00017

Density at 20° C

33

Ratios by weight: Ca/Na 0.051 <.02

.0086

.0001 .058

.004 .0003 <.001(?)

.015 .0076

0.058 Mg/Ca .15 K/Na .012 Li/Na .00037 HCO3/CI > .032 SO</Cl .030 F/Cl . Br/CI .00036

I/Cl .000004 B/Cl ..

Analysis ... ...... Bad Hal

Llnz,

J

1, SW. Of Austria Smrdaky

Breclav, < va

i

, ESE. of 3zechosloria

9 Chokrak, Crimea, USSR

Oct. 1, 1937

10 Toyotomi, Hokkaido Prefecture, Japan11 Isobe, Gumma

Prefecture, Japan

1 Hanmer

Island, N(

2 Name of springs and location.. , South

Date of collection w Zealand

SIOj ppm8.9 Tr

6.1 Tr

244

156

13

epm ppm

29 epm ppm

20 epm ppm20 <0.1

0.6

epm ppm

45

0.3

6

epm ppm epm

Al 1.0 Fe 3.0 Mn

Ca 12.18

12.8.30

81

63 4.04 4.4

495 441

24.7

36.3

76323.79

2.6 220

47 10.98 3.9

10.3 0.50 Mg .02 SrBa

Na.. 6,460

102.3 62

281.0

.26

.33 2.9

9253840.24 .97 '9,640

441 419.311.28 4,200 320

182.7 8.19

10,400 290

452

7.4 379

4.0

16.48 K .10 LiNH« 4.2 0.23 150 8.32 20 1.11 3.0 .17

310 49.9 600 197 475 17.3 HCOs... 426 6.97 410 6.72 1,010 16.5 1,690 27.7 7,610 123.1 196 3.21 COs—

8O4 .00 1178

1,390

.23 2.36

39.2

1.1 139

16,900

.02 4.20

477

<0.5 .00 21 .44 194.7

483

.39 H8 .14 ClF

10,700 302 6,230 175.7 12,700 358 13.61 Br 7839

.03

.98

.31 .00

Present

2.2

13345

1.66 0.36

1724.21 .19 20

47

.25

I 0.02 .37 NOj

NO.

Present Present

11677

PO« 9

128 1,160 B 42

26

18394

279

148 j 49 CO.

H.S

310 48.6 500 204 . 482 17.4 Total, as reported 18,300 3,610 30,100 12,800 32,600 1,150 See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F37

Table 15.Chemical analyses of spring waters similar in composition to oil-field brines of the sodium chloride type—Continued

Analysis Name of spring? and location

.

Date of collection.

Bad Hall, SW. of Linz, Austria Smrdaky, ESE. of Breclav, Czechoslo- vakia

Chokrak, Crimea, USSR

Oct. 1, 1937

10 Toyotomi, Hokkaido Prefecture, Japan

Isobe, Gumma

Prefecture, Japan Hanmer, South

Island, New Zealand

Specific conductance micromhos at 25 °C. PH.

Temperature °C.

Density at 20° C

Ratios by weight: .—

Ca/Na

Mg/Ca

K/Na

Li/Na HCOj/Cl»

SO./C1 -

F/Cl

Br/CI

I/Cl B/Cl -

Cold(?)

0.038 .63

.0015

.00035 .040

.0000

0.084 .65

.041

7.2 Cold

1.02

0.051 .89

.046

7. 42 8.2

16.2 8.049

0.018

.42 .076

0.021

.21 .028

0.026 .03

.011

.29 .0079.060

.000065

.27 .0000 .59

.0017

.41 .039

.0073

.0036

.0039

.0016

.0078

.0027

.0011

.0027 .0038

.024

.0016

.0037 .010 .10

1 Components mentioned in explanation of table.

» Includes C03 as HCO3. EXPLANATION FOR TABLE 15

1. Spring, rising in large concrete-lined pool in southern part of Tuscan area, NEJ4

sec. 32, T. 28 N., R. 2 W., Tehama County, Calif. Probably from rocks of Cretaceous Chico Formation overlain uneonformably by volcanic agglomerate

of Pliocene Tuscan Formation. Flows about 10 gpm; total flow of springs from area about 30 or 40 gpm; no spring deposits, but travertine veins are in bedrock. Analyzed spring has little associated gas but combustible gas is present in nearby "Natural Gas" Spring (Waring, 1915, p. 290). Collected by

R. C. Scott, U.S. Geol. Survey; analyzed by B. V. Salotto, who also found

5.2 wc per 1 Ra and 6 /ig per 1 TJ. He also reported Cu, 0.00 ppm; Zn, 0.00 ppm. Li, NH(, Sr, Br, L and B determined by H. Kramer, C. E. Roberson, and P. w. Scott of U.S. Geol. Survey in sample collected June 9, 1954, having same CI content. Analysis not previously published.

2. Main spring, spring 22, Wilbur, NWM sec. 28, T. 14 N., R. 5 W., Colusa County,

Calif. Discharge of spring is 15 gpm and discharge of group is about 40 gpm

(White, 1957b, p. 1674-1677; Waring, 1915, p. 99-103). From rocks of Knoxville Formation of Late Jurassic age, near serpentine intrusions (W. B. Meyers,

U.S. Geol. Survey, written communication). No spring deposits, but water

is associated with quicksilver and gold deposits. Analyzed by W. W. Brannock

of U.S. Geol. Survey, who also reported 0.0 ppm Sb and 0.0 ppm As. Components determined on later samples of similar chloride content: Determinations of Br and I by Brannock; 0.2 ppm Hg by J. D. Pera of Buckman Laboratories Inc.; Fe; Al; Mn; Cu, 0.00 ppm; Zn, 0.00 ppm; 3 wc per 1 Ra and 0.8 y% per 1 U reported by B. V. Salotto; Sr and Ba determined by spectrographic

analysis; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated residue at 180° C, 23,500; Fe, 0.1; Cu, 0.05; Ag, 0.02; Pb, 1.4; Cr, 0.07; W, 9.4; Li, 12; Rb, 1.2; Cs, 0.7; Sr, 1.4; Ba, 1.9. See table 23, analysis 2, for water analysis from Abbott quicksilver mine, 2 miles to southwest.

3. Spring, near crest of ridge at Tolenas, 4 miles north of Fairfield, sec. 1, T. 5 N., R. 2 W, Solano County, Calif. About M gpm of water and at least as much gas

discharging near crest of travertine ridge, about 200 ft long, on interbedded

shale and sandstone of Cretaceous Chico Formation (Waring, 1915, p. 162-163; Weaver, 1949, p. 106-107). Gas is not combustible and probably is largely CO2; total discharge of water from area is only a few gpm. Analyzed by C. E.

Roberson, U.S. Geol. Survey; As, 0.00 ppm also reported; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180° C, 17,700; Al, 0.2; Fe, 0.1; Cu, 0.02; Sr, 0.7; Ba, 1.3. Analysis not previously published.

4. Main spring, Mercey, SEH sec. 15, T. 14 S., R. 10 E. Fresno County, Calif. Flows 7 to 10 gpm from gravels overlying fractured greenstone associated with

Franciscan Sandstone of Late Jurassic or Early Cretaceous age. The water may rise along a fault zone close to the contact of Franciscan and Cretaceous Chico Formations (Anderson and Pack, 1915, p. 212-213). Spring is 3 miles southeast of Mercey quicksilver mine (Yates and Hilpert, 1945). Analyzed

by H. Almond and S. Berman, U.S. Geol. Survey. Analysis not previously

published.

5. Stinking Springs, also known as Lampo or Connors Springs, NWJ^ sec. 30, T.

10 N., R. 3 W., 6.8 miles northwest of Corinne and immediately north of Great

Salt Lake, Box Elder County, Utah. Sampled spring discharges about 30 gpm and is easternmost and largest spring of a group that has total discharge

of about 75 gpm from near contact of Quaternary sediments and Lower Carboniferous limestone (Emmons, 1893, p. 386). Collected by J. H. Feth, analyzed by J. P. Schuch of U.S. Geol. Survey; also determined are SO3, ppm; As, 0.00 ppm. Spectrographic analysis of evaporated residue by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 37,300; Al,

0.8; Fe,0.2; Mn.0.1; Cu,0.04; Sr,31; Ba,4.1. Analysis not previously published.

6. Well, 2,130 ft deep, near Bad Hamm, Ruhr district, West Germany, in Kreide Formation of Late Cretaceous age (Himstedt, 1907, p. 163). Analyzed by C. R. Fresenius, 1882; methane present.

7. Upper Gunther well, Bad Hall, north-central Austria, 25 miles southwest of Linz (Schmblzer, 1955, p. 197); drilled in area of springs known and used since eighth century. Well is 820 ft deep in Molasse of Tertiary age, overlying Oligo- cene and Miocene sedimentary rocks. Also reported is a trace of Cu. Analysis

of gas from one well is given in table 28, analysis 5 (Grill, 1952, p. 89).

8. Well 6, in spring area at Smrdaky, about 20 miles east-southeast of Breclav, in southwest Czechoslovakia; producing from depth of 990 ft from Burdigalian- Helvetian rocks of early and middle Miocene age (Janacek and Janak, 1956, p. 72-74, 96). Water also contains naphtha, and associated gases include H2S

and CH4 . 9. Resort with drilled wells, about 160 ft deep, in former cold-spring area on east border of Chokrak marsh, 1 mile from south shore of Sea of Azov and about 12 miles north of Kerch, Crimea, U.S.S.R. Water is from shale, limestone, and

dolomite of Karagan and Chokrak Formations of Tertiary age (Fomichev,

1948, p. 221-232). Analyzed by I. S. Krasnikova and M. S. Svemina. Na

reported as 642 ppm, but reported equivalents and strong unbalance of cations and anions clearly indicate that this figure is a misprint for 9,462 ppm. Analysis

is Fomichev's type 2; for his type 1. see table 22, analysis 6. 10. Toyotomi, near northwestern tip of Hokkaido, Japan. Spring discharges from

Pliocene sandstone and mudstone, probably marine (Muto, 1954, p. 408-409). Nearest Quaternary volcanic rocks are those of Pleistocene Rishiri volcano, an

island 25 miles to the west.

11. Isobe, Gumma Prefecture, in central part of Honshu, Japan. Spring discharges

2 gpm from middle or late Miocene sandstone, shale, and conglomerate (Muto,

1954, p. 408-409). Nearest Quaternary volcano is Haruna, 10 miles to the north- northeast (H. Kuno, written communication). Analyzed by Muto (1954, p. 409) except for NH4 and PO<, which are analyzed by Tokyo Hygienic Laboratory, 1930 (Morimoto, 1954, p. 246-247).

12. Springs and well, 300-ft deep, at Hanmer, near south base of Seaward Kaikoura

Range, South Island, New Zealand. Discharge is from thick alluvial gravel overlying graywacke of Mesozoic age (J. Healy, written communication). For gas analysis (Farr and Rogers, 1929, p. 300-308) see table 28, analysis 6.
F38 DATA OF GEOCHEMISTRY

Table 16 .Ohemicat analyses of spring waters similar to oil-field brines of the sodium calcium chloride type

1 London, Lane

County, Oreg.

Sept. 3, 1957

2 Willow Creek, Shasta County,

Calif.

Nov. 30, 1956

3 Utah, Weber

County, Utah

Apr. 5, 1958

4 Saratoga, Sara- toga County, N.Y.

Aug. 7, 1938

6 Tolsona, Copper River

Basin, Alaska

Sept. 21, 1956

6 Wiesbaden, N.

of Mainz, Germany

7 8 Thermopotamos, Tromnshertr.

Date of collection

Euboea Island, Greece Orange Free

State, Union

of South

Africa

SiOj ppm

190.12

.00

.00 .00

.00

.00

.13 48029 •7.9

»5.7

8108.2

.0

.0

epm ppm

22

0.04 1.05

.00 1.05

.00

.00

.00 1,1202.4 •6.6

1.2

2,670

7.5 2.2

21

epm

55.9.20

116.1.19 .32

1.16

ppm

38

0.46

.42 1.9

.00

.01 .00

.00 1,14070 »28

» 1.1 7,030

901

9.9

5.4

epm ppm

133.4

1.8 10.003

epm ppm

160.2

.3

epm ppm

64 epm ppm

580.2

1.1.02

epm ppm

26

1 1

epm

Al . . . Fe 3.0 0.7

0.001 Mn "Tr Cu

Pb

Zn .01 As .08 34448

120.7

2,660

953.5

7.0

Ca 23.95 2.4

56.9 5.8 623

197 31.09

16.2 787

111 151

14 ,66060 >0.5

6.6

39.27 9.13

1.16

.20 202.7

1.53 .07

.31

17.17 4.0

.27

.01

115.7 2.43

.50

.39

1,780 329 88.8

27.1 47320

7.2

1 1 2,670

16 »6

nil

None(?

60

946

4,2503.6 Nil

23.6 Mg 1.6 Sr 0.16 Ba

305.8

23.05

1.43 .30

13 2,030 380

7.6

11

.18

88.3 4 9.72

1.09 .61

.01 Na 35.24

.21 10,000441

.5

1.1

435

11.28

.07 .06

116.1 K .41 Li .8 NHi .00 Total cations 61.8 174 393 147 254 140 562 . 143

760.8

1.2 2,100

.0 3.7

.2.02 9.3

.34 3.0

20

38

6,080

.0

192

189

13, 300

3.2

8.2

.2.00

.0.00

5.1

3,870 143

0.0

1,8700.3

173.7

.00

.07

HCOi 1.25 0.00 595 590 .67

.79

171.5

3.15 63.4 2.34 9.75 9.67 ) 0.00 COi 2.00 so* .02

59.2 3.93375

.17

.10

.00

.66 250.1 0.02

0.21 .03

.00

.01

63

4,590

1.31 129.61,120

18, 500 23.3

522

19.70 CI 2,970 83.8 i 119.9 F .19 Br .05 .00

.00

.15

9.4

1.0 .12.01 2.5.02 1.4 ».6

.03 1.0 234

.03

.00

.01

.01

62

.08

.78

.00 .00 I „

NOi .00 6.6 .11 Nil Nil.00 NOi .00 PO« .04 6.6 338 B 1.8 35 14 COj

H,S .1 .0

fntftl anions 60.7 173 382 147 253 141 556 142

Total, as reported 3,550 10,000 22,900 10, 100 4,800 1 8,730 33,200 8,480

Specific conductance micromhos at 25° C 6,2707.6

Slightly warm

14,3009.0

171.004

0.42 .0022

.0028 .00083

.0066

.0063 .00000

34,3007.3

67

1.013

0.16

.061 .13

.0014

.014 .014

. 00024 .00062

.00002

.00038

23,600

7.1Cold

1.008

0.17

.14

.013 .0001

.016

. 00000

.00003

.0019 .00042 .0039

pH 6.2Cold6.81 65.36.65

78.2

1.025

0.18

.19

.044 .00005

.032

.061

8.95 Temperaturo ° C

Density at 20°

37 Ratios by weight: Ca/Na 0.59

.060

.010 .0000

.036

. 00057

.0000 .0018

.0001 .0014

0.31 .32

.19

.0037

1.3.000

0.13

.14 .036

.0013

.13 .014

0.17 Mg/Ca .042 K/Na .0059 Linsra .0022 HCOs/Cl > .029 SO4/CI .22 F/Cl .00084 Br/CI .0032

.00034

.00054 .00000

.00021

.0034 .00000.0000

I/Cl B/Cl .00030 .001

Analysis 9 Aln Djebel, SSW. of Tunis, Tunisia10 Tiberias, Near

Sea of Tiberias,

Israel

11 Geyser Suyu,

Anatolia, Turkey

12 Staraia Matsesta, Abkhaz, USSR13 Neshkin, Siberia, USSR14 Arima, HySgo Prefecture, Japan15 Name and location . Naganuma,

Yamagata Prefecture, Japan Date of collection

SiO, ppm

2013

5

epm ppm

23 epm ppm

223.2

.06

epm ppm

•17 epm ppm

95

9.3

.1

epm ppm

146

71 167

42

.1.4

.2

3,88038

2.0 59

19,600 4,440

63

44

epm ppm

72

.9 4.3

epm

AlFe 7.8 Mn

Cu

Pb

Zn

AsCa 1,000 275

49.9 22.6 3,930

825

196.1 67.9 3,19065159.2

6.3

638

18029

26.85

14.8.66

3,49025

174.2 2.1193.6 3.13

.05 .86

853

113.6

7.6 2.44

2,310

162 115.2 Mg 13.3 SrBaNa 5,240 283

1

227.9

7.24

.1

6,910

77 300.6

1.97 18,600

1,990 809.1

61.0 3,560

1381.2 8.3

154.7 3.53

.17

.46

6,190 840269.3

21.5

7,080

6541.7

.7

308.0 K 14.16 Li .24 NH< 4.3 .24 .04 308 567 18.025 . 201 467 ' 1,174 451 HCOi 204

400 3,000 8,290

3.34

13.33 62.5 233.8

366 6.98 64

149 36,100

1.05

.00 3.10 1,018

384 6.29 27 0.44 667 9.29 69 1.13 CO,

80« 891

19,200 18.63

641

1.9 6,060.04 170.91.2

16,500 .02 465

0.0

41,700.7

62

.9

1.4

535 370

.9

.00 1,176

.04 .65

.01 .00 .00

4.9

15,900

.10 CI 449 F

Br 68 Tr

0.2

1.2 Tr

.85

.00

.00 .02

1.4 .02 26

3.7

.33 .03

34

17 .43

I .13 NO,

NO, 682.2

1.10 PO( B 13 119 248

3.6

31

4 CO, 96 H,S 0.3 28 Present Total anions 314 666 1,024 178 465 1,186 451 18,800 32,300 60,400 11,300 27,200 1 71,800 26 200

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F39

Table 16.

Chemical analyses of spring waters similar to oilfield brines of the sodium calcium chloride type—Continued

9 Ain Djebel, SSW. of Tunis, Tunisia

10 Tiberias, Near

Sea of Tiberias,

Israel

11 Geyser Suyu,

Anatolia, Turkey

12 Staraia Matsesta, Abkhaz, USSR13 Neshkin, Siberia, USSR14 Arima, Hyogo Prefecture, Japan

15 Naganuma,

Yamagata Prefecture, Japan

Specific conductance pH 6.2

1001.047

0.17

.020

.063

5.8 94.0

(')

0.20

.0097

.23 .0027 .014

.00000 .00002

.0012

.00002

7.7 Density at 20° .. 54.5 61.9 24± 65

(')

0.56

.0071 .14

611.017 Ratios by weight: Ca/Na 0.19

.28

.054

.0002 .12

.36

0.57

.21 .011

0.16

.30 .39

.00034 .063

.00031

0.33 Mg/Ca..__ .070 K/Na .078 Li/Na .00024 HCOi/Cl* .019

.044 .0017.0041 .0016.00007 .0043 S0«/C1 .00031 F/Cl

Br/CI .008 .0000 .00007 .0043

.00061 .0022

.0021 I/Cl .0011 B/Cl .00023

1 Components mentioned in description.

» Includes COi as HCOa. EXPLANATION FOR TABLE 16

1. Main spring, London, NWM sec. 40, T. 22 S., R. 3 W., Lane County, Oreg., discharges about 10 gpm from nonmarine tuffs and basalt flows of Calapooga Formation of Eocene age. Collected by Linn Hoover; analyzed by J. P. Schuch o( U.S. Geol. Survey; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to opm in the original water: evaporated residue

at 180°C, 4,360; Al, 0.2; Fe, 0.4; Ti, 0.03; Cu, 0.004; Sr, 7.9; Ba, 5.7. Analysis not previously published.

2. Main spring of small group on Willow Creek, half a mile above junction with

Crystal Creek, lat 40°40' N., long 122°38' W Shasta County, Calif. Discharge

of spring estimated at 1 gpm, and total discharge of group is 5 gpm; from

fractured quartz prophyry dike cutting pillow lavas of Copely Greenstone

of Paleozoic age. Collected by J. Albers, analyzed by H. C. Whitehead of U.S. Geol. Survey; also reported and included in totals, OH, 3.6 ppm (0.21 epm); spectrograph^ analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated residue at 180°C, 10,700; Al, 0.3; Fe, 0.05; Cu, 0.05; Ag, 0.01; Sr, 6.6; Ba, 0.2. For analysis of gases, see table 28, analysis 7; collected by U.S. Bureau of Reclamation June 8, 1956. Analysis not previously published.

3. Spring, Weber County, Utah: northernmost of four springs near boundary

between Weber and Box Eider Counties and 8 miles north of Ogdeu. Discharges about 25 gpm from alluvium overlying Pleistocene Lake Bonneville

sediments near frontal fault of Wasatch Range. Collected by J. H. Feth; analyzed by J. P. Schuch, U.S. Geol. Survey; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated residue at 180° C, 23,200; Al, 0.7; Fe, 0.1; Ti, 0.1; Cu, 0.1; Sr, 28; Ba, 1.1. Analysis not previously published.

4. Coesa spring, Saratoga, Saratoga County, N.Y.; one spring of group emerging

along fault in Canajoharie Shale of Middle Ordovician age overlying Little Falls Dolomite (Strock, 1941, p. 857); water also tapped by drilling to dolomite. Spring deposits consist 01 travertine. Analyzed by S. Drexler. Mn deter- mined by L. W. Strock (average of Hayes and Orenda springs, very similar

In CI content to Coesa spring); also determined spcctrographically, in ppm:

Zr, 0.4; Sn, 0.03; Ti and V, each <0.0016; Co, <0.0005; Ni, 0.0003; Be, 0.001 (Strock, 1941, p. 860).

5. Southwestern spring, on crest of mud cone 1.5 miles west of V.A.B.M. Shepard and 0.3 mile north of Gl< nn nighway, Gulkana A-4 quadrangle, Copper River

Basin, Alaska. Discharges 1 to 2 gpm 01 muddy water accompanied by little gas, including H2S. Area is underlain by glacial deposits which 2 miles to the south are at least 500 ft thick. Possibly a few hundred feet oi Eocene sand and gravel and probably a few thousand teet of marine silcstone and shale of Matanuska Formation ol Late Cretaceous age beneath the till (A. Grantz,

written communication). Sample collected by F. Robinson and F. Rucker;

analyzed by G. Gaston; Sr and LI analyzed by C. E. Roberson, U. S. Geol. Survey. For gas analysis seo table 28, analysis 8; collected by A. Grantz,

Sept. 7, 1957, analyzed by U.S. Bureau ot Mines. Analysis not previously

published.

6. Kochbrunncn spring, eastern most of the four principal springs at Wiesbaden,

north of Mainz, west-central Germany. Discharges 350 gpm trom fault in mica gneiss (Michels, 1954, p. 113-117). Analysis by Fresenius and Fresenius

(1936, p. 28-35), with NO2 and NOj from a later very simihr analysis (Michels

1954, p. U5). Also icportfld snd included in totals: Rb, 0.4 ppm (0.00 epm);

Cs, 3 ppm 10.00 tpm). For gas analysis see table 28, analysis (Fresenius and Frescn'us. 1936, p. 32).

7. Thermopotamns spring, near northwest end of Euboea Island, Greece. Spring apparently discharges horn fault in Devonian schist overlain by Carboniferous

limestone east ol major antidine (Pertessls, 1937, p. 93-94; D.jprat. 1903). This

is one of the new and hotter springs formed at time of major earthquake under

Gulfof Euboea, April 27, 1894 (Dambergris, 1896, p. 385-393) . Analysis reported

as hypothetical chemical combinations (Pertessis, 1937, p. 93-94), converted

to ppm.

8. T. G. 1 well, 4,700 ft. deep, near Trompsberg, south of Odendaalsrus, Orange Free

State, Union of South Africa; lat 30D03' S., long 25c44' E. Artesian discharge

of 500 gpm (Kent, 1949, table 3, p. 243, 248, 2.13) from norite, probably of Bushveld Complex of Precambrian age, overlain by Dwyka Series; water is highest

in salinity of South African thermal waters. Kent suggests NaCl may be

derived from leaching of Dwyka tillite, ground waters of which are shown by Bond (1946, p. 106-122) to be relatively high in NaCl. Analyzed by W. Sunkel and P. Kok, 1948. Mn, Al, Ba, Li, and B are spectrographic determinations by B. Wasserstein.

9. Spring, Ain Djebel, located 20 miles south-southwest of Tunis, Tunisia; dis- charges IVi gpm from large travertine deposit on Lower Cretaceous and Upper

Jurassic sedimentary rocks near crest of faulted anticline (Berthon, 1927, p. 23, 94-110). Analysis in mg per 1; sp gr not stated; reported quantities probably

should be decreased by about 1 percent.

10. "Open" spring of Old Bath, west side of Sea of Tiberias, Israel, discharging from

basalt of probable Tertiary age (A. Friedmann, 1913, p. 1493-1494; Luke and

Keith-Roach, 1934, p. 401-402).

11. Geyser Suyu, in Kizilca Tuzlasi group of saline springs 3 miles southwest of Ayvacik, near Tuzla, in northwest Anatolia, Turkey (Caglar, 1948, p. 250, 253; Prof. E. Goksu, written communication). Geyser Suyu is not a true geyser but surges regularly to height ol a few feet. Springs emerge along a fault at the base of a mountain chain of Tertiary andesite with marine Mio-Pliocene sedi- mentary rocks to the east; no Quaternary volcanic rocks nearby.

12. Staraia Matsesta well 8, in spring area 2 miles northwest of shore of Black Sea and 6 miles from Sochi, Abkhaz area, U.S.S.R. (Vinogradov, 1948, p. 26-27; Tsebricoff, 1928). Spring emerges from caves near a major fault on a large anticline in Upper Cretaceous marl overlain by Tertiary shale. Discharge of springs in area at least 140 gpm (Martel, 1904, p. 999-1001; Renngarten, 1927). Analysis is of well water and includes S1O2, SjOs (1 ppm), OO2, and H2 S (in- cluding 100 ppm reported as HS) from a very similar analysis reported by

Ovchinnikov (1947, p. 138) from Matsesta well 4. 13. Neshkin spring, about 20 miles south of Neshkin village on Chukchee Peninsula,

Siberia, U.S.S.R. Discharge of two vents is about 80 gpm (Rabkin, 1937, p. 93-101) from crystalline schist of Silurian age; slight odor of H2S. Analysis

given in g per 1; sp gr not given, but analysis converted to ppm by assuming sp

gr of 1.02. 14. Tenmangu-no-yu spring of Arima group, 9 miles northeast of Kobe, Honshu,

Japan (Ikeda, 1949, 1955a, 1955b; Kimura, 1953); spring discharges from lower

or middle Miocene rhyolite near a fault separating rhyolite from granite to the south (H. Kuno, written communication). Nearest Quaternary volcano is a small cone of olivine basalt at Yakuno, 41 miles to the northeast. Water analyzed by Ikeda (1955a, 1955b). Stated in g per 1; sp gr not given but. assumed

to be 1.05; additional components, in ppm: Rb, 3.3 (0.04 epm); Cs, 2.4 (0.02 epm); V, 5.7; Cr, 0.09; Mo, 0.06; Ti, 2.5; Sb, 0; Be, 0.01; Gc. 0; Ga, 0; Ag, 0; Ni,

0.001; Co, 0.001; Bi, 0; Cd, 0; In, 0; Sn, 0.0005; Ra, 212 X10-"; Th, 250X10""; Rn, 510X10-12 in curies per 1. 15. Naganuma, Yamagata Prefecture, northern Honshu, Japan. Springs discharge

35 gpm from alluvium overlying Miocene or Pliocene sediments. Nearest Quaternary volcanoes are Chokai, 20 miles to north-northeast, and Gassan, 20 miles to south-southeast (H. Kuno. written communication). Analyzed by

Yamagata Hygienic Laboratory, 1949 (Morirnoto, 1954, p. 150-151).
F40 DATA OF GEOCHEMISTRY

Table 17.Chemical analyses of thermal waters from geyser areas in volcanic environments

1 2 3 4 5 6 7 Upper Basin, Yellowstone

Park, Wyo.

Oct. 16, 1957

Norris Basin, Yellowstone

Park, Wyo.

Aug. 3, 1951

Steamboat

Springs, Washoe

County, Nev.

Aug. 9, 1949

Beowawe Geysers, Eureka

County, Nev.

Sept. 1, 1957

Morgan, Tehama

County, Calif.

July 29, 1949

Geyser Bight, Umnak Island, Alaska

Aug. 17, 1946

ENE. of Reykjavik,

Iceland Aug. 31, 1958

SiOj ppm

363

.2

.06

.0

1.5

epm ppm

'529 epm ppm

293

1.5 10.05

1 .05 2.7

0.4

5.0

.8

1 .5 653

717.6 <1

epm ppm

373

.0.04

.0.02

epm ppm

233 epm ppm

150 epm ppm

359

.89 .02

.00

.06

epm

Al - -

Fe i.2 1 .1 1.01

3.8 None

40

.2 1.3

350

182 <0.1

Mn . As 3.1

0.1 5.8

.2 '.4

439

748.4

.1

0.29

.02

.00

19.1 1.89

1.21 .00

2.2

.0 79

.8

1 14 1,400

1969.2 <1

3.94

.06

.32 60.9

5.01 1.32

Sb __ Ca .8

.0

0. 352246.2

.0

0.04

15.3

.61 .75

0.25

.06

.01 28.4

1.82

1.10

.8

.0

0. 230

161.3

.5

0.04

10.00

.41 .19

.03

2.00

.02

15.22

.46

.29

.4

.5 1.02

233

11.2

.1

02 Mg _ 04 Sr — Na 10 14 K - .28 Li - 03 NIL - 01 Total cations 16.7 22.5 31.6

5.00

2.08

24.39

.09

.00

.00

10.67 71.6 18.0 10.60

7023

40525

1.5

.3 1.8

1.3 4.4 2.6

27

38 744

4.9

.1.0

305

100 865

1.8 0.2

0.1

116 14989

30

15

.4

.0

.4.07 2.0

5.5

52

79 2,430

1.5 '0.8

10.0

29

10

130 482

1.2

128

102

126

12.2

.0

.0.09

1.1 2.7

HC03 - 2.33

.48 11.42

1.32

.02 .00

.03

0.44

.79 20.98

.26

.00

1.90 4.97

1.85

.85

.79 .00

.01

0.85

1.64 68.5

.08

.01

0.48

.33 2.71

13.59

.06

CO] - 4 27 SO4 2 12 CI 3 55 F .63 Br

INO3 . - None

PO« B 12

.0

22.5

49

4.7 88

0.7

49 H2S

1 17.1 31.6 10.37 71.1 17.2 1 10. 75 Total, as reported 11,310 1,890 2,360 1,030 4,590 1,270 1980

Specific conductance micromhos at 25°C. 1,7909.6

94

0.002

.0.068

.015 .35

.057

.062 .0037

.0007

.011

2,490

7.5 84.5

0.013

.03 .17

.019

.036

.051 .0066

.0001 .0000

.015

3,210

7.9 89.2

0.0077

.2

.11 .012

.35

.12

.0021 .0002

.0001 .057

1,0509.5

96

0.003

.0.070

.0057

143.0

.50

.013 .00

.067

6,920

7.8 95.4

0.056

.01

.14 .0066

.021 .033

. 00061

. 0003

.0000

.036

1,150 pH 1 6.9

101.5

0.11

.005

.051 .006

.10

.26 .0024

9.7 Ratios by weight: Ca/Na

100

0.002 Mg/Ca — 1.3 K/Na .047 Li/Na HCO3/CI > .0004

2.1 SO4/CI .81 F/Cl .10 Br/CI .0016 I/Cl .000 B/Cl .10 .0096

Analysis 8 Reykjanes, SW.

of Reykjavik,

Iceland

Sept. 4, 1958

9 Hveravellir, West-central, Iceland Aug. 31, 1958

10 Shumhaya,

Kamchatka,

USSR

11 Geizernye, Kamchatka,

USSR

Sept. 27, 1951

12 Pauzhetsk, Kamchatka,

USSR

Oct. 18, 1950

13 Tokaanu, North Island, New Zealand14 Name and location Wairakei,

Date of collection

North Island, New Zealand

SiOz ppm

197

.66 .28

.05

.12

epm ppm

609

.55

.21 .00

.05

epm ppm

294

.8 5.0

i.02

epm ppm

256

.0

.0

.0.1

epm ppm

1 190

.0

.0

epm ppm

302

5.7 None

epm ppm

386 epm

AlFeMn

As 1.1 Sb i.l 15

15

i.Ol 45693

Ca 2,20045

15

13, 800

1,920

7.4

1.4

109. 78 3.70

600.3

49.11

1.07 .08

2.0

.5.003

156

15

.2

.1

0.10

.04

6.79

.38

.03

.01

0.75

1.23 273.7

1.35 .30 64

10 3.20

.41 44.4 2.20.03 26 <0.1

1.29 Mg

SrNa 19.84 2.38

597

60 25.961.53

1,01088

44.4 2.25

2,180 216

94.8 5.52

1,130

146

12..9

49.2 K 3.73 Li. 1.73 NH( . .8 .04 .0 1.8 .10 .05

Total cations 764.04 7.35 24.2 129.1 50.2 102.7 66.0

5

128 27,400

.7 98

.5

.9.16

130.2

112

17 178633.3

.0.0

.3.14

.68 2.6

89.0(?) 150 7001.2 8.08138

114 859

37

9.0

83 1,680.8 3.2

.0

70

74 3,410

35

0(?) 35

1,9306.2

HCO3 0.08

2.66

772. 68

.04 1.23

.01

1.84 .57 3.71

1.78

.17

1.46

3.12

19.74

.06

.10

1.33

1.27 2.37 24.22

0.60

.30

1.73 47.5

.04

.03

1.15

1.54 90.2

0.57 CO3

SO, .73 CI 54.4 F_._. .33 Br 1.3

.0

.01

INOs

PO4 B 8.4 21 '31 99 26 H2S 1.1 Total aninris , . 776. 70 8.07 24.5 '29.2 50.2 98.9

""I

56.8

Total, as reported 45,700 1,160 11,840 2,060 3,210 6,400 13,750

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F41

Table 17.

Chemical analyses of thermal waters from geyser areas in volcanic enviroments—Continued

8 Reykjanes, SW.

or Reykjavik,

Iceland

Sept. 4, 1958

9 Hveravellir, West-central, Iceland Aug. 31, 1958

10 Shumhaya,

Kamchatka,

USSR

11 Geizernye, Kamchatka,

USSR

Sept. 27, 1951

12 Pauzhetsk, Kamchatka,

USSR

Oct. 18, 1950

13 Tokaanu,

North Island, New Zealand

14 Wairakei, North Island, New Zealand

Specific conductance

63,800

6.7

100

0.16

.020

.14

.0001 .0002

.0047 .00003 .0036 .00002

.00047

842

8.7 90.5

0.013

.3.096

.0006 2.4

2.8

.052 .000

.000

.011

pH - — 8.4 98

0.033

1.0.20

8.7 98.9

0.045

.14 .10

.0.18

.13

8.4

100.6

0.063

.16 .087

7.4 Boiling

0.020

.009 .099

8.6 Temperature „°C..

Ratios by weight: Ca/Na

Boiling

0.023 Mg/Ca .00 K/Na _ _w» .13 Li/Na .011 HCO3/CI2... .13

.21 .0017

.011

.033

.049

.0005 .0019

.0000 .018

.021 .022.018 SO( /Cl .018 F/Cl .0032 Br/CI .0015

.0000 .024

I/Cl B/Cl . .012 .029 .013

1 Components mentioned in explanation of table.

2 Includes CChasHCCh.

EXPLANATION FOR TABLE 17

1. Spring, 50 feet south of Upper Basin drill hole described by Fenner (1936, p. 228-

281; White, 1955a, p. 103-105); located northwest of Old Faithful Inn and 650

feet south of Three Sisters springs in Upper Basin of Yellowstone National

Park, Wyo. Discharges 10 to 15 gpm from hydrothermally altered dacite obsidian of probable late Pliocene age overlain by 213 ft of Pleistocene sediments and 7 ft of siliceous sinter. A maximum temperature of 180° C was measured

at a depth of 406 ft, the bottom of the hole. Analyst, H. C. Whitehead, U.S.

Geol. Survey; also determined are Zn, Pb, NO2, Ti, and Cu, each 0.00 ppm; OH, 26 ppm (1.53 epm, included in total) ; spectrograph^ analysis on evaporated

residue, by Nola B. Sheffey, converted to ppm in original water: evaporated

residue at 180° C, 1,320, Al, 0.9; Fe, 0.04; Qa, 0.03; Ti, 0.004; Cu, 0.003; Mo, 0.06; W, 0.1; Cr, 0.001; Ge, 0.05; Li, 11; Rb, 0.2; Cs, 0.3; Sr, 0.004; Ba, 0.1. For analysis of gas Irom drill hole see table 28, analysis 10 (Allen and Day, 1935, p. 86). Analysis not previously published.

2. Unnamed spring with small periodic discharge, Norris Basin, Yellowstone

National Park, Wyo. Spring is depositing much silica 200 ft southwest of Pearl geyser (White, 1957a, p. 1640-1641; Allen and Day, 1935, p. 482-483) and

about 700 ft northwest of spring given in table 19, analysis 1. Bedrock is welded

rhyolite tuff overlain by alluvium and sinter. In drill hole, 3,000 ft to north temperature of 205° C was measured at a depth of 246 ft (Fenner, 1936, p. 289-

292; White, 1955a, p. 103-110). Analysts. P. Scott, W. W. Brannock; Sr de- termined by C. E. Roberson, U.S. Geol. Survey. Also reported is Hg, 0.0 ppm. For gas analysis see table 28, analysis 11; sample from similar slightly alkaline spring in northeastern part of Norris Basin (Allen and Day, 1935,

p. 86, 468-469).

3. Spring 8, near east edge of Main Terrace, Steamboat Springs, 10 miles southsoutheast of Reno, NEH sec. 33, T. 18 N., R. 20 E, Washoe County, Nev.

Discharge is 0.25 gpm; total for whole spring system is about 700 gpm. GS-5

drillhole, 250 ft to northwest of the spring, penetrated 84 ft of sinter, 71 ft of altered alluvium and, finally, altered granodiorite. Maximum temperature

of 172° C was found at a depth of 379 ft (White, 1955a, p. 103-104, 110-113; 1957a, p. 1639-1647). Analyst, W. W. Brannock, U.S. Geol. Survey. Fe, Al, Mn,

Sr, and Ba (0.05 ppm) by spectrographie analysis. For gas analysis see table

28, analysis 12; sample from spring of lower temperature (73° C) 130 ft to northwest.

4. Large spring at base of terrace, Beowawe Geysers, Eureka County, Nev., de- scribed by Nolan and Anderson (1934, p. 224-226); periodic discharge ranges from to 75 gpm. Bedrock of terrace is basaltic andesite, overlain by opaline

sinter (Nolan and Anderson, 1934, p. 216-218). Analyst, H. C. Whitehead,

U.S. Geol. Survey, who also determined Cu, Pb, Zn, Ti, NO2, each 0.00 ppm.

Analysis not previously published.

5. Growler spring, Morgan, NEH sec. 11, T. 29 N., R. 4 E., Tehama County, Calif., on east fork of Mill Creek, about 5 miles south of active Mount Lassen volcano (White, 1957a, p. 1640). Discharges 7 to 10 gpm from Brokeofl Andesite (Williams, 1932, map), overlain by alluvium and a little sinter. Analyst, W. W.

Brannock, U.S. Geol. Survey; also determined on other samples from same

spring are Hg (0.0 ppm), Br, and I by Brannock; Sr by H. Almond; U (0.5 ppb), Cr (0.01 ppm) (spectrographie), and Fe (0.2 ppm) by others of U.S.

Geological Survey.

6. Geyser H-l, 4^ miles southeast of Geyser Bight, Umnak Island, Alaska (Byers and Brannock, 1949, p. 720, 726-730). Discharges 175 gpm from monzonite and

Plio-Pleistocene basalt flows of Mount Recbeschnoi, overlain by alluvium. Area is 20 miles southwest of active basalt volcano, Okmok. Analyst, W. W.

Brannock. Also reported is Mo, 0.005 ppm; Fe, Mn, and Sr determined

spectrographically.

7. Sisjodandi spring, which occasionally erupts as a small geyser, about 1,500 ft south of Geysir, near the south end of the thermal area east-northeast ol Reykjavik. Iceland (Barth, 1950, p. 95-100). Discharges from siliceous sinter and

alluvium, probably underlain by late Cenozoic sodic rhyolite and surrounded by basaltic lava flows and breccias. Collected by Gunnar Bodvarsson, State

Electricity Authority; analyzed by O. E. Roberson of U.S. Geological Survey, who also reported Cu, Pb, Zn, NOi, each 0.00 ppm; OH, 30 ppm and 0.18 epm

(included in totals) . Quantitative spectrographie analysis, by Nola B . Sheffey, converted to ppm in original water: Cu, 0.003; Ag, 0.0008; Ge, 0.03; Pb, 0.02; Ni, 0.006; Fe, 0.12; Cr, 0.002; V, 0.003; Al, 0.64; Ga, 0.004; Ti, 0.02; Sr, 0.02; Ba,

0.02; Li, 0.1; Rb, 0.06. Mo, W, Sn, Zn, Cd, Sb, Mn, Co, La, Zr, Be, Cs below

detection limits in solids. Analysis not previously published. For analysis

of gas see table 28, analysis 13; sample from small boiling spring, 150 ft northwest

of Geysir (Thorkelsson, 1940, p. 13, 23).

8. An erupting well about 100 ft north of Gunna and 1,000 ft northeast of "Sea water

geyser," Reykjanes, southwest of Reykjavik, Iceland (Barth, 1950, p. 115, and

G. Bodvarsson, written communication, 1958). The well is 532 ft deep and is in an area of Recent basalt flows, overlying Pleistocene basalt tuff and breccia

of the Moberg Formation. Sample collected by Gunnar Bodvarsson, State

Electricity Authority; analyzed by C. E. Roberson of the U.S. Geol. Survey, who also reported Cu, Pb, Zn, each 0.00 ppm; NO2, 0.06 ppm; additional SiOj

that may have precipitated after collection, but not included in totals, 446 ppm;

density, 1.031. Quantitative spectrographie analysis, by Nola B. Sheffey, converted to ppm in original water: Cu, 0.05; Mn, 2.5; Al, 0.5; Sr, 15; Ba, 11; Li, 6.6; Rb, 3.8. Ag, Mo, W, Ge, Sn, Pb, Zn, Cd, Sb, Co, Ni, Fe, Cr, V, Ga, La,

Ti, Zr, Be, and Cs are below detection limits in solids. Analysis not previously

published. For gas analyses see table 28, analysis 14 (Thorkelsson, 1928).

9. Blahver (Blue Spring) in the southern part of the thermal area, Hveravellir,

west-central Iceland (No. 493 of Barth, 1950, p. 145-146). The area contains

siliceous sinter and many geysers and is underlain by postglacial basalt flows. Collected by G. Bodvarsson State Electricity Authority; analyzed by C. E. Roberson of the U.S. Geol. Survey, who also reported Cu, Pb, Zn, each 0.00 ppm; NO2, 0.03 ppm. Quantitative spectrographie analysis, by Nola B. Sheffey, converted to ppm in original water: Cu, 0.007; Ag, 0.0006; Mo, 0.03; Ge, 0.05; Ni, 0.006; Fe, 0.1; Cr, 0.001; V, 0.008; Al, 0.1; Ga, 0.02; La, 0.05; Sr, 0.003; Ba,

0.01; Li, 0.3; Rb, 0.02. W, Sn, Pb, Zn, Cd, Sb, Mn, Co, Ti, Zr, Be, and Cs are below detection limits in solids. For gas analysis from same area see table 28, analysis 15; analyzed by B. Lindal of State Electricity Authority.

10. Sugar-bowl Geyser (Ustinova, 1949, p. 152, 155), Shumhaya, Kamchatka,

U.S.S.R., discharging from late Tertiary (?) lava near semiactive Semiachinskie Volcano (Piip, 1937, p. 154-156). Mn, Sr, and Sb determined by spectrographie

analysis, which also included Ga, 0.1 ppm; Ti, 0.001 ppm; Be, 0.05 ppm.

11. Velikan (Giant) Geyser, Kamchatka, U.S.S.R.;oneof a vigorous group of geysers; average discharge of geyser about 25 gpm: total discharge of group more than 400 gpm. In alluvium on Quaternary volcanic rocks of southeast Kamchatka

(Ivanov, 1958a, p. 202-207; 1958b, p. 482). Believed by Ivanov to be underlain by Tertiary marine strata. Is near active volcanoes Kikhpin'ch, Uzon, and

B. Semyachik. Analyst, S. S. Krapivina, who also reported Ti, looked for but not found.

12. Paryashchii 1, Pauzhetsk, Kamchatka, U.S.S.R.; a spring discharging 17 gpm

in a group of springs and geysers discharging more than 400 gpm from alluvium

in Quaternary volcanic rocks of southeast Kamchatka (Ivanov, 1958a, p. 202-

207). Near active volcanoes Kosheleva and Kambal'no. Analyst, E. F. Prokofeva, except SiOj and B determined by E. P. Ryabichkina from 1955 sample. For gas analysis, by I. S. Krasnlkova, of nearby Pauzhetsk (New Geyser)

see table 28, analysis 16.

13. Taumatapuhipuhi Geyser, Tokaanu, North Island, New Zealand (Grange,

1937, p. 100-101, 105). Springs emerge near south shore of Lake Taupo from Kakaramea Andesite of Plio-Pleistocene age, overlain by alluvium and siliceous sinter (Grange, 1937, map of Puketi and Omoho districts; Healy, 1942).

14. Drillhole 4, 1,245 ft deep, about 3,000 ft southeast of Geyser Valley (Grange,

1965, map), Wairakei. North Island, New Zealand. In highly altered sediments

of Pliocene(?) Huka formation, overlain by Pleistocene (?) Wairakei pumiceous

breccia and alluvium (Steiner, 1953, 1955). Maximum temperature of 228° C

was measured at a depth of 970 ft (Banwell, 1955, p. 55; Banwell and others,

1957, table 2). Analyst, S. H. Wilson (1955, p. 37): also reported and included

in totals is free COa, 11 ppm. For gas analysis from well 4/1, about 100 ft southeast of well 4, see table 28 analysis 17 (Wilson, 1955, p. 29).
F42 DATA OF GEOCHEMISTRY

Table 18.

Chemical analyses of thermal sodium chloride bicarbonate waters from nongeyser areas associated with volcanism

1 Hot Creek, Mono County,

Calif. May 17, 1967

2 Niland,

Imperial County, Calif.

Feb. 3, 1954

3

Roosevelt, Beaver County, Utah

Sept. 11, 1957

4 Jemez, Sandoval County, New Mexico

Aug. 31, 1949

5 Cerro Prieto, Baja California, Mexico

Feb. 4, 1954

6 Agnano, WSW.

of Naples,

Italy

7 Nalachevskie, Kamchatka,

USSK

8 Kuan-TsuN. of Tai Taiwa

About 1

Ling

Pei, D

933

Si02 - - ppm

131.0.04

.0

.00

1.0 4.4

.2

35020

1.7

.1

epm ppm

75 epm ppm

313<.04

<.04

.0.00 2.0

22

.0

2,500

488

27.0

epm ppm

93 epm ppm

'106 epm ppm

152 epm ppm

125 Tr U.4

'.3

epm ppm

69 epm

AlFe .03 4.2

4.5

.09

.01 383

122Tr

3,050 717

1.5 25

1.1.02

8.3(?) Mn

Pb

As

19.11 10.0

132.7 18.34

.22

5.9

24932

.06

1,060

144

.6

Ca .22

.02

385 580

9.2

47.7

1.10

.00

1386.6

6.88

.54 37023

18.46

1.9

12.43 2.6

8.4

7.8 .42 Mg .64 SrNa - 15.2

.51 .24

.00

7,280

537

18

316.7

13.74 2.6

108.8 12.48 3.9572

70 24.88

1.79

4,580

679

10

199.2

17.37 1.4

46.1 3.68

.03

3,730

1327.7

162.3 K - - — 3.38 Li - .- 1.11 NHi

16.19 400 126.3 34.1 238 181.8 64.8 167.9

4977.9 90

200

10

.7

.4.00

.8

10

.2

1,600

384

12,900

0.4

156

73 4,240

7.5 3.3

.3

.01

112.2 38

735

49 7955.2

66

250 8,170

0.8

1,570 519

445

1,590'.8

6.0 '1.0Tr

Tr

HC03 — 8.15 5,420 .26

1.87

5.64

.63

.01 .00

26.2

7.99

364

.02

2.56

1.52 119.6

.39 .04

.00

.00

.18

12.05

1.02

22.41

.27

1.08 25.7 8.51 88.7 CO3 -- SO) 5.2

230.4

.04

451 5,220 9.39

147.2 9.2744.8

.04

.08

.01

74

2,770

1.54 CI 77.8 F

Br 5.1 0.2

.06 14

13 .17

I .10 NO2 —

NO3 4.9 .08 .8 .01 5.0 .08 PO4 1.4 B 53 11 12 0.2 72 200 H2S

16.46 398 124.3 35.8 237 182.4 62.7 168.3

Total, as reported 1,330 23,800 7,880 2,480 14,300 '11,800 4,250 12,500

Specific conductance

1,6208.3

93

17,8606.4

40

1.013

0.052

1.5

.073

.0025 .12 .030

.00003

12, 700

7.9

' 55

1.001

0. 0088

.00

.20

.011 .037

.017 .0018

.00078

.00007 .0090

3,5607.2 65.5

12, 5705.9 82

1.005

0.081 .062

.15 .0022

.0081

.031

.0001

pH '6.45

73 7 8.3 Temperature 20° C~

Densitv at 20° C

70.5 7

Batios by weight: Ca/Na 0.013

.05

.057 .005 2.6

.45

.050 .0035 .002

.050

0.24

.048 .12

0.13

.32

.24

.00049

.30 .086

0.23

.13 .14

.000

.33

28

'! 0005

.0038

'. 0006

.043

0.0023 Mg/Ca .93 K/Na .035 Li/Na ... .0021 HCO3/CI2 — .92

.062 .0065

2.0 S0</C1 .027 F/Cl

Br/CI .001

. 00004

. 00004

.0051 I/Cl .0047 B/Cl .0041 .013 .0015 .072

1 Components mentioned in explanation of table.

2 Includes C03 as HCOj.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F43

EXPLANATION FOR TABLE 18

1. "Geyser" spring, NEH sec. 25. T. 3 S., R. 28 E., Mono County, Calif.; on east bank

of Hot Creek, 3 miles northeast ol U.S. Highway 395 and 15 miles southeast

of Mono Craters, which consist of late Pleistocene and Recent obsidian and

pumiceous rhyolite (Putnam, 1949); surrounded by Pleistocene rhyolite, in

part, hydrothermally altered. The spring boils vigorously, discharging 5 to 10 gpm and depositing some travertine near center of active zone, 1,500 feet long, on Hot Creek. Analyzed by H. C. Whitehead, U.S. Geol. Survey, who also reported, Cu 0.00 pprn, Zn 0.01 ppm, Ti 0.00 ppm. Analysis not previously

published.

2. Well, at abandoned dry-ice plant 4 miles west-southwest of Niland, Imperial County, Calif., and 1H miles east of the Salton Sea and Mullet Island, which

is one of a group of late Quaternary pumiceous rhyolite domes (Kelley and Soske,

1936; Waring, 1915, p. 41; White, 1955b, p. 1121-1123). Artesian discharge of 20 to 30 gpm from well reported 511 ft deep and entirely in Cenozoic alluvium of basin of Salton Sea. Analyzed by H. Kramer, U.S. Geol. Survey. Water

qualitatively similar to that of thermal well on Mullet rhyolite dome drilled through rhvolite and more than 1,000 ft into underlying sediments, where steam was found (Kelley and Soske, 1936, p. 502; White, 1955b, p. 1123). For analysis

of gas see table 28, analysis 18; sample from well 400 ft deep, In alluvium 4 miles north of Mullet Island (Anderson and Hinson, 1951, p. 50-51). Analysis not

previously published.

3. Springs, 15 miles northeast of Milford, Beaver County, Utah, in fault zone In

granitic rocks overlain to east by Quaternary(?) obsidian (Lee, 1908, p. 20-21). About 1908 the largest spring was discharging 10 gpm at a temperature of 88°C and was "boiling," with steam escaping from crevices; abundant silica was being

deposited in gelatinous and spongy masses (Lee, 1908, p. 20). When visited by

H. E. Thomas in 1950 (oral communication), temperature of main spring was

85°C; discharge was a few gpm; and hard porous opal, as much as 4 in. thick, had precipitated on walls of wooden trough. In September 1957 temperature was only 55°C, discharge was less than 0.05 gpm, and discharge of all springs and

seeps was not more than 2 gpm. Analyzed by H. C. Whitehead, U.S. Geol. Survey; also reported are Cu, Zn, and Ti, each 0.00 ppm; spectrograph^ analysis

of evaporated residue, by Nola B. ShetTey, converted to ppm in the original water; evaporated residue at 180°C, 7,860; Al, 0.02; Fe, 0.06; Cu, 0.02; Ge, 0.08; Li, 20; Rb, 9.4; Cs, 0.7; Sr, 1.8; Ba, 0.01. Analysis not previously published.

4. Spring, in pool behind bathhouse, 12 miles north of Jemez, sec. 22(?), T. 18 N., R. 2 E., Sandoval County, N. Mex. Discharges about 10 gpm (total discharge

of group of springs about 200 gpm) from fault in red beds of Permian age (Stearns and others, 1937, p. 167). overlain by late Cenozoic rhyolite, tuff, and basalt (Kelly and Anspach, 1913). Collected by J. D. Hem, analyzed by J. L. Hatchett

of U.S. Geol. Survey. Analysis not previously published.

5. Springs, Cerro Prieto, Baja California, Mexico, 25 miles south of Mexicali; a spring

in a small sulfur-covered pool discharges about 1 gpm from northwest edge of

saline flat, which also contains other small springs, mud volcanoes, and sulfur

deposits. Springs discharge from fine clastic Quaternary sediments near southeast base of Cerro Prieto, a Pleistocene volcano of hypersthene andesite flows and flow breccias (White, 1955b, p. 1123). Analysed by H. Kramer, U.S. Geol. Survey. Analysis not previously published.

6. Sprudel spring, Agnano, in central part of Phlegraean Plain about 10 miles west- southwest of Naples and 20 miles west of Mount Vesuvius, Italy (Zambonini and others, 1925, p. 434-474; Ventriglia, 1951, p. 282-295). Spring flows from

trachytic tuffs near Quaternary cinder cones that probably are underlain by

thick trachytic tuffs and lavas (Falini, 1951, p. 211). Wells, as much as 300 ft deep, in Agnano area have water of lower temperature than that of spring (Penta,

1949, p. 346). Also reported are Ti, 0.001 ppm; Ba, 0.6 ppm; dissolved CO2,

103 ppm, which are included in totals. Gases, 72.9 cc per 1 of water, included

in table 28, analysis 19.

7. Spring 1, or "Kettle" spring, of Nalachevskie group, near head of Nalacheva River

in southeast Kamchatka, U.S.S.R., about 30 miles from east coast, in area of active Quaternary andesitejand basalt volcanoes (Piip, 1937, p. 130, 247-250; Ivanov, 1958a, p. 199-201). Analyzed by B. E. Kuteinikov, 1933; reported Mn

mav include Zn; Rb and Cs, each reported as ppm; Sb, 0.6 ppm; S2O3, ppm.

F, free CO2, and pH from very similar analysis (Ivanov, 1958a. p. 199-201) except

that I was looked for but not found. For gas analysis see table 28, analysis 20; analyzed by I. S. Krasnikova from sample collected by Ivanov in 1951.

8. Spring in Kuan-Tsu-Ling, north of Taipei, northern part of Taiwan. Discharges from andesite flows and agglomerates of Pleistocene Tatun Formation, overlying Mio-Pliocene marine strata (Juan, 1956, pi. 2). Spring water is milky from suspended matter that consists largely of SiOs, AI2O3, CaC03 , FeO, and TiOj.

Analysis reported in millimoles per 1, converted to ppm, with no correction for specific gravity (Pan, 1952). Also reported are Ti, 0.2 ppm; Zn, 0.2 ppm; Zr,

trace, and Cu, 0.6 ppm.
F44 DATA OF GEOCHEMISTRY

Table 19.Chemical analyses of acid sulfate-chloride springs in volcanic environments and crater lakes

Analysis 1 2 Copahue Volcano, Neuquen Territory, Argentina

3 lcano, Island, R

1955

4 Lower Mendeleev

Kunashir Island, USSR

Oct. 30, 1954

5 6 9 Norris Basin, Yellowstone

Park, Wyo.

Aug. 27, 1954

Ebeco Vc

Paramusbir USS

Aug. 30

Kusatsu Shirane, Gumma Prefecture, Honshu,

Japan

Yakeyama, Nii- gata Prefecture, Honshu, Japan

Iburi Prefecture, Hokkaido, Japan

Feb. 1, 1938

Si02 ppm

369

1.5

} •

epm

0.17

.04

ppm

160

162

f 217

epm

18.0 7.77

ppm

5962

202

373.2

9232

108922.4

5.0 11,790

epm ppm

27093

219

31

.4 15068

121 105

epm

10.4 7.82

1.66

ppm

444

13

} 7.2

epm ppm

640

340

970

epm ppm

480

13

f 35

epm

Al 6.9 7.23

1.99 .12

4.59 2.6

4.70

2.35 .35 .28

1.776

1.5.39

37.8

52.1

1.45 Fe+> - 1.25 Fe+» Mn 1.0 109

17 592

54

.07 Ca 6.5

.0 243

613.2

3.4 17.8

.33

10.57

1.56 .46

.19

7.7

18030

169Tr

8.98 2.5 7.357.45 5.6

5.27 2.68

32

1.3 1,380

2311.2

1.60

.11 60.0

5.91

.03

2,010 520

1,540 380

100.3 42.8

67.0 9.72

5.46 Mg 1.4 Na 25.8 K 1.38 Li .. NH« „ 8.5 1301

.47 2996.9 20.38 20

5.5 .31 H .• 178 78 1431 428 Total cations.. 21.0 344.1 1,807 61.3 147.5 738 37.1 HCO3 86(?) 1.41 HSO» 911 1,150 983

1.2

.3

.0

9.39

24.0 27.78

.06

.00

SO4 454 408

9.45

11.51

12, 700 2,640 264

74.5 996

63,200

7144

.4

20.74

1,7823.74

.55 .00

4,490

1,910 93.5

53.9

8,380

20, 000

173.9 564 274

1,060

5.70 CI 30.0 F .. Br ..

IPOt .6

39 6.9

B. 6.9 Very much 32 115 H2 S

21.0 '344 1,807 61.2 147.4 738 37.1 Total, as reported . 1,570 1 16, 900 66, 800 4,160 8,590 35, 300 • 2, 810

pH.. .. 2.47

87

1 Strongly acid

100

1.7 0.4

88

3.2 Density at 20° C

20 91 911.003 Ratios "by weight: Ca/Na 0.027

.00

.25

.013 .000

1.1

1.1.17 .000.85

.35

.85 .022

1.2

.45

.87

0.023

.041 .17

.0001

1.3.26

.25

0.18 Mg/Ca .16 K/Na .091 Li/Na HCO3CI .081(7) SO«/Cl> F/Cl

4.8 .016

.0011

. 00070

.000006

2.1.0012

.0003

.0000

.033

2.4 .42 .26 Br/CL

I/Cl B/Cl .017 .0057 .037

Analysis . . Yang M

North

Tai

8ing Shan,

f Taipai, wan

9 Taal Volcano, Luzon, Philippine

Islands March 1907

10 Kawah Idjen Volcano, Java, Indonesia

1941 (?)

11 Tjiater, Java, Indonesia12 Frying Pan Lake,

Tarawei"a region. New Zealand June 24, 1932

13 NT»m« and ]nr>aHnn White Island, Bay

of Plenty. New

Zealand

Si02 ppm

322

600

95

epm ppm

0)7,600

5,100

9 0)2,810

318 7,420

125

epm ppm

184 4,130

epm ppm

15766

}

1 182.4

1112468

30

epm ppm

412

42

epm ppm

164 1,880

/10, 500

\ 130

24(?) 2.370

6,770

7,100 926

epm

Al..; 66.7 3.40845 182.6

.48

490 7.34

.97

.09 5.54 2.0 2.96

.77

0.44

.11

208. Fe+» 376.3 Fe+l 1,600 86.0 6.9 Mn 1.3 Ca 263

73

75

11

13.12 6.0 3.26

.28

140.2 26.2

322.2

3.20

783 848 988

791

39.07

69.7 42.98 20.23

14

4 609

51

.70

.3 26.47

1.30

118.3 Mg 556.5 Na 308.8 K 23.7

Li. NHt 1 12 .67 2

1 .8

.11 .817 287.9 H 27 27 '464 460 1740 734 285

119.8 1,980 1,482 16.3 30.2 1 1, 886 HCO3

HSO4 7,600

2,170

57, 300

806

37

5.6

78.4 SO< 3,730

1,490 77.7

42.0

30, 800

47, 500

641 1,339

46, 100

18, 500 960.0

522.0

407 567

13

8.47

15.99 .68

262

878

5.46 24.7445.2 CI. 1,615 F 42.4 Br .5

IPOt 2.9 (') 0.3 B 4.4 None

5.9 H2 S - - 216 28 Total anions 119.7 1,980 1,482 25.1 30.2 1 1, 783 Total, as reported 6,900 102,000 74,900 1,480 2,240 1 i8. 300 pH 1.6

811.006

3.5.28

.14

Strongly acid

1001.072

0.38

.11 .017

Strongly acid 2.25

44

3.1 55 Strongly acid Temperature °C_. 1 Hot. Density at 20° C 1.05

0.79

1.1.80

1 1.08 Ratios bv weight:

1.6.22

.44

0.021 .29

.084

Ca/Na 0.33 Mg/Ca 2.9 K/Na .13 Li/Na HCO3CI .000 SO( C12 2.5 .65 2.5 .72 .30 .023

.17 F/Cl .014 Br/CI .00064 I/Cl .000 .0001 B/Cl .0050 .0001

' Components mentioned in explanation of table. Includes HSO«.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F45

EXPLANATION FOR TABLE 19

1. Green Dragon spring, southern part of Norrls Basin, Yellowstone National Park, Wyo.; discbarges about 40 gpm (White, 1955a, p. 107; 1957a, p. 1640, 1648) from

hydrothermally altered alluvium overlying late Cenozoic welded rhyolite tuff. About 700 ft southeast of spring given in table 17, analysis 2. Analyzed by

H. Kramer, U.S. Geol. Survey; H calculated by difference.

2. Crater lake of Copahue, a Quaternary trachyte volcano, Neuquen Territory, Argentina. Lake is a third of a mile in diameter and heated by volcanic gases (Corti and Camps, 1930, p. 380; Sussini and others, 1938). Area also has sulfur deposits. Analyzed by H. Corti, reported as hypothetical chemical combinations, converted to ionic form; H calculated by difference; also reported is SjOj, 326 ppm (5.82 epm), included in totals.

3. Lake, in central funnel of upper (southern) crater of Ebeco volcano, near north end of Paramushir Island, Kurile Islands, U.S.S.R. (Ivanov, 1957, p. 70). Rocks consist largely of andesite flows and tuffs. Sample analyzed by S. S. Krapivina, who also reported, in ppm, Co, 0.3; Ni, 0.1 ; Cu, 0.03; Ti, 0.2; Sr. 0.8; As, 0.6. H and most of CI reported as free HC1; pH reported —1.7, requiring

50 molar HC1 solution; pH of about —0.25 seems more probable. For gas

analysis see table 28, analysis 21.

4. Main spring, Lower Mendeleev group, Kunashir Island in northern Kurile

Islands, U.S.S.R.; discharge is 115 gpm (Ivanov, 1958b, p. 480). Collected by

Ivanov; analyzed by S. S. Krapivina, who also determined TI, 0.2 ppm;

Cu, 0.09 ppm; As, 0.9 ppm.

5. Main spring of a group near active Kusatsu Shirane volcano, Gumma Prefecture, Honshu, Japan (Yamagata, 1951, p. 159). Springs discharge from pyroxene

andesite flows and pyroclastic rocks of volcano; many active solfataras (H. Kuno, written communication). H calculated by difference; Li, Rb (0.3 ppm), and Cs (0.1 ppm) determined spectrographically. A less complete analysis

of water from the strongly acid crater lake of this volcano was published by Mlnaml and others (1952, p. 4).

6. At southern base of active Yakeyama volcano, Niigata Prefecture, Honshu,

Japan (Muto, 1954, p. 408-409). Spring discharges from hornblende.pyroxene

andesite lavas and pyroclastic deposits of the volcano overlying Miocene or Pliocene sedimentary rocks. H calculated by difference.

7. Main spring of group, Noboribetsu, Iburi Prefecture, southwestern Hokkaido,

Japan. Total discharge of springs is about 1,000 gpm from Miocene sedimentary rocks at west base of Pleistocene volcano Kuttara. This volcano consists

of pyroxene andesite and has a summit caldera lake (Okuno and others, 1938, p.

853, 857-858; Ishizu, 1915; H. Kuno, written communication). HjS, including

3.9 ppm reported as HS, from sample of Sept. 26, 1937; determined by dithizone and included in totals: Cu, 0.16 ppm; Zn, 0.36 ppm; and Pb 0.34 ppm; free COj,

41 ppm. Traces of Cd, Ti, Ni, and Ba determined spectrographically. Other

springs in the area are acid sulfate type given in table 20 (Okuno, 1939, p. 689).

Partial analyses by Usumasa and Morozumi (1955) are reported to be of water from main spring but are neutral and very different in composition.

8. Yang Ming Shan spring, near extreme north end of Taiwan, discharges from

hydrothermally altered Pleistocene basalt overlying Mio-Pliocene marine sedi- ments (Pan, Lin, Hseu, Sun, and Chan, 1955, p. 27-30; Yen, 1955; Juan, 1956).

9. Crater lake of active andesitic Taal volcano, Luzon, Philippine Islands. Sample

collected by Bacon (1907, p. 118), March 1907 (prior to 1911 eruption); H cal- culated by difference. Other pre-eruption analyses reported as much as 332 ppm P01( 401 ppm Si02, and 303 ppm Mn (Neumann van Padang, 1953, p. 36).

10. Crater lake of active Kawah Idjen, a basaltic andesite volcano on shoulder of Merapi, Besuki Residency, eastern Java, Indonesia (Neumann van Padang,

1951, p. 157-158; Bemmelen, 1949b, p. 105-106). Volcano had violent eruption

in crater lake in 1817 and minor eruptions in 1796, 1917, and 1936. Crater lake contains 1HX108 cubic ft of strongly acid water with more than 100,000 tons

dissolved aluminum sulfate. Analyzed 1941, cations reported as grams of oxide per liter, converted to ppm by assuming density of 1.05; H+ calculated by difference.

11. Tjipanas spring 1, in Krawang Residency, western Java, Indonesia. Discharges

1,300 gpm from hot spring deposits of jarosite (KFe3(S04)s(OH)j and iron phosphate high in As (Bemmelen, 1949a, v. 1A, p. 215; v. 2, p. 232-239). These

deposits contain hundreds of thousands of tons and lie on andesite and basalt flows of Tangkuban, an active volcano about 3 miles southwest. The iron phosphate deposits contain about 2 percent of arsenic. Analyzed by Laboratory for Mineral Research, Mining Department, Java; inorganic Fe, 18 ppm;

total Fe, 20 ppm; reported NH3 converted to NHi.

12. Frying Pan Lake, Tarawera region, New Zealand, at site of volcanic eruptions

in 1886 and 1917 (Grange, 1937, p. 93, 103, 105; White, 1957a, p. 1640, 1642, 1648). Discharge is more than 1,000 gpm. Bedrock is rhyolitic tuff and breccia of the Waitahanui Series of Plio-Pleistocene age, overlying Pliocene rhyolite and

overlain by more than 10 feet of basaltic ash from the 1886 Tarawera eruption (Grange, 1937, map of Tarawera district). H calculated by difference; analysis

of gases from small hot spring on edge of lake given in table 28, analysis 22 (Grange, 1937, p. 110-111).

13. Hot spring pool in crater of White Island, an active andesitic volcano in Bay of Plenty off northeast coast of North Island, New Zealand. Some fumaroles have temperatures as much as 500°C. Sample collected and analyzed by S. H. Wilson, New Zealand Department of Scientific and Industrial Research

(1959, p. 37). Reported in g per 1, converted to ppm assuming density of 1.08. Also reported and included in totals: SiOr' (tetrathionate), 157 ppm (1.4 epm); SsOr3 (pentathionate), 9.3 ppm (0.1 epm); As, 5.7 ppm; Sr, 9.3 ppm (0.2 epm). For analysis of gas, same locality but different pool, see table 28, analysis 23.
F46 DATA OF GEOCHEMISTRY

Table 20.—Chemica I analyses of acid sulfate spring waters associated with volcanism

Analysis 1 "The Geysers", Sonoma County,

Calif.

2 Bumpass Hell, Shasta County,

Calif. 1953

3 Norris Basin, Yellowstone Park, Wyo.

Aug. 25, 1954

4 Mud Volcano Group, Yellowstone Park, Wyo.5 Sulphur Springs, Sandoval County, N. Mex.

Aug. 31, 1949

6 Uzon Volcano, Kamchatka, US8R

Aug. 26, 1950

S102 ppm

225

1463

1.4 47

28112

5 1,4009.5

epm

1.67 2.26

ppm

240

31

185.5

epm ppm

1092.4

epm ppm

540

146

17

epm PpTtl 216

56

epm ppm

292

444 412

epm

Al 3.4

.65 .30

0.27 16.2 6.2 49.39 Fe+» - 14.76 Fe+S .8 .04 .91 33

3.3

18552

6.7 24

1.77

.12 9.23 4.2

.29

.61

Mn - .05 2.35

23.1

.52 .13

77.6

9.4

Ca 6.5

5.3 32

13

146.2

.32

.44 1.39 .33

.78

6.2

2.2

2.0

3.0 30

1 14

.11 14

1116

1726

43

.70

.91 .70

• .44

1.44 42.7

83

35 Ul

14 1547

14

4 15 Mg 2.87 Na .09

.08

1.66

14.0

•48 K .61 NHi 30.4 H 13 12.6 14 Total cations . 1117.3 13.8 16.3 64.0 35.1 116.7 HCO3

'0

~~

8iOs .- HSOt...

SO« 5,7101.5

118.9.02718

1.1 14.95 .03

758

15 15.78 .42 3,150 Tr

1

65.6 1,5703.5

1.1

32.7

.10

.06

5,550

12

.4

Tr

2

115.6 CI .37 F - .05 .02 Br..

I . NOj - B. 3.1 .2

20 6.9 H2 S

118.9 15.0 16.2 65.1 32.9 116.0 7.770 1,110 943. 3,980 2,160 7,420

4,570

1.9 65±

28

.28 3.6

pH -. 1.8±

Boiling?

3.9

6.0

.42

1.97 90

1.1

1.5

.0

51

1.86 Temperature C C 79.0

0.20

.81 .41

65

0.88

.78

1.1

60 Ratios by weight: Ca/Na - 18 Mg/Ca 4.2 K/Na 11 Li/Na HCOi/Cl .0

11,000

.0 450

.31

.0 SO( /Cl2 - 650 >1,000>1

460 F/Cl .03 Br/CI .00 I/Cl - .00 B/Cl - 6.2 .11 .46 .00

Analysis 7 Koshelevsk, Kamchatka, USSR

Aug. 15, 1951

8 North Menc

Kunashir Is USSR

Oct. 1, It

eleev, land,

54

9 Yunohanazawa,

Kanagawa Prefecture, Honshu, Japan

10 Nasu, Tochlgi

Prefecture, Japan K

Vo

11 Name and location letetahi, Tongariro

Date of collection...

lcano, New Zealand

SiOj ppm

120 epm ppm

27478

11234

.6

798.7

455

9.6

8.0 20

epm ppm

283

1203.9

epm ppm

14785

/ 28

\ .0.3

64

3122

7.1 3.1

15

epm ppm

1628.9

epm

Al 8.7

6.07

1.22 .02 3.95

.71 19.79 .23

.44 20

13.3

1.40

8.59

1.02

1.00 Fe+» 19 0.67

Fc+' - .7 .04 Mn 1.2 40

1360

18

101.05

.05 2.00

1.06 2.62

.45 5.60

.05

.01 3.19

2.55 .96

.18

.17

14.9

Ca 103

1333

2.9

5.14

1.1 1.44 .07

762863

3.5

374

1.6

3.80 Mg 2.3 Na 2.76 K .09 NH« 20.7 H - 1.6 12.50 61.1 22.5 31.57 32.3 HCO3 - s( o« 2

1,440 602

169.4.00

.000

.000

67

35

0.01

14.83

12.53 4.77

.02

1 103

149 1,220

18

0.92 HSO« 1,590 2.020

93

.9

.4.0

16.4 42.1 2.63

.04

.00

1,54 SOi 5944.8

.0.3

.0

12.36

.13 1,0402.6 21.6

.07

25.3 CI .50 F

Br .00

INOs - B 26 12

44 93 HsS Tr

Total anions 12. 49 61.2 21.7 32.16 28.3 Total, as reported 997 14,840 1,600 2, 780 2,300

Specific conductance (micromhos at 25 °C)... pH 4.3 92.5

0.67

.33 .30

1.70 69.0

0.17

.11

.021 .#....

2.3

78

3.1

.13 .088

1.5 69.9

2.9.48

.32

2.8 Temperature °C 1 70 Ratios by weight: Ca/Na 1.2 Mg/Ca .37 K/Na .060 Li/Na 0005 HCOj/Cl .000 nnn

120 .00 39

.01

.004 .000 .13

RO( /Cl» 400 12.002

.0000 .0000

.33

68 F/Cl. Br/CI .06

I/Cl _- .00 B/Cl E.2

1 Components mentioned in explanation of table.

» Includes HSO,.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F47

EXPLANATION FOR TABLE 20

1. Devils Kitchen spring, "The Geysers," (Allen and Day, 1927, p. 33), 11 miles

east of Cloverdale, Sonoma County, Calif. Seeping discharge from pool on

landslide material underlain by Franciscan graywacke, greenstone, and ser- pentine of Mesozoic age (Bailey, 1946, p. 211-215, pi. 29); no true geysers. Area

is 3 miles west of Cobb Mountain, a Pleistocene (?) rhyolite volcano (Brice,

1953, p. 35, 37). Gas analysis from well 1, 460 feet north-northeast of spring

(Allen and Day, 1927, p. 60, 76; White, 1957a, p. 1648), given in table 28, analysis

24. Analyzed by E.T. Allen, who also reported and included in totals: S20j,0 ppm; Ni, trace; Cr, 2 ppm (0.23 epm). CI and pH determined by H. Kramer,

U.S. Geol. Survey, on sample collected March 24, 1954, which also contained

5,070 pp, of SO» and 2.7 ppm of B.

2. Spring in thermal area, Bumpass Hell, Shasta County, Calif., 2 miles south of Lassen Peak, a dacite volcano last active from 1912 to 1919. Spring, 250 ft north-northeast of junction of principal streams draining thermal area, is in hydrothermally altered Brokeoff Andesite of upper Pliocene or Pleistocene age (Williams, 1932, p. 374-375, map). Sample collected and analyzed by P. S. Bennett of U.S. National Park Service. Analysis not previously published. For gas analysis, apparently from same spring, see table 28 analysis 25 (Day

and Allen, 1925, p. 95, 133).

3. Locomotive Spring, Norris Basin, Yellowstone National Park, Wyo., 80 ft southeast of Congress Pool and 200 ft west-southwest of Norris Basin drillhole (Fenner, 1936, p. 282-310; White, 1955a, p. 103-107). Seeping discharge; bedrock is acid-leached welded rhyolite tuff of Pliocene(?) age. Analyzed by H. Kramer,

U.S. Geol. Survey; also reported is Li, 0.0 ppm. H calculated by difference. Analysis not previously published. For gas analysis from Locomotive Spring

or a nearby spring, see table 28, analysis 26 (Allen and Day, 1935, p. 86).

4. Big Sulphur Pool, 0.2 mile north of Mud Volcano, Yellowstone National Park, Wyo. (Allen and Day, 1935, p. 422, 427) ; little or no discharge. Pool is in glacial material overlying rhyolite of Pliocene(?) age (Hague and others, 1899, Canyon

sheet of geologic folio). For gas analysis see table 28, analysis 27 (Allen and

Day, 1935, p. 86, 418).

5. One of about eight springs in sec. 3, T. 19 N., R. 3 E., Sulphur Springs, Sandoval County, N. Mex., Small discharge, but total for the group (same type?) is about 500 gpm (Stearns and others, 1937, p. 167) in area of late Pliocene or Pleistocene rhyolite overlying Paleozoic sediments. Gas analysis of Alum

Spring given in table 28, analysis 28 (Renick, 1931, p. 89). Analyzed by U.S.

Geol. Survey; H-|- computed from pH. Analysis not previously published.

6. Boiling mud pot in west field of crater of Uzon, a semiactive basaltic andesite volcano in southeastern Kamchatka, U.S.S.R. Crater contains many mud

pots and mud volcanoes (Ivanov, 1958a, p. 195-196; Piip, 1937. p. 171, 172, 248,

267). Sample collected by B. I. Piip; analyzed by M. S. Suetina. Ti, 5.4 ppm is included in total; As, HCO3, Br, I, and B were not detected. Na not determined by Suetina; reported value is from 1933 analysis (Piip, 1937, p. 171-172), probably less than amount actually present. For gas analysis from nearby vent see table 28, analysis 29.

7. Mud pot on upper slopes or in crater of semiactive Koshelevsk volcano of south- eastern Kamchatka, U.S.S.R. (Ivanov, 1958a, p.195-196). Collected by G. A. Gonsovsk; analyzed by E. F. Prokof'eva; As, not found. For gas anlysis

of nearby boiling lake see table 28, analysis 30; poor summation suggests misprint.

8. Lower spring, Northern Mendeleev group, Kunashir Island, Kurile Islands, U.S.S.R. Discharge is about 30 gpm (Ivanov, 1958b, p. 479). Collected by

V. V. Ivanov; analyzed by S. S. Krapivina, who also reported and included

in totals: Sr, trace; Ba, 0.0 ppm, As, 0.7 ppm; Cu 0.03 ppm; Ti, 0.4 ppm.

9. Yoemon-Yu spring of Yunohanazawa group in Hakone caldera, Kanagawa

Prefecture, Honshu, Japan (Kuroda, 1941b, p. 69-74). Springs discharge from

pyroxene andesite on east flank of postcaldera late Pleistocene Kami-yama

volcano (H. Kuno, written communication). Analyzed by K. Kuroda, who

also reported Cu, 0.045 ppm.

10. Yumato spring, Nasu, Tochigi Prefecture, Japan; "gushing out" of southeast

slope of Nasudake, an active andesite volcano (Kimura, Yokoyama, and Ikeda,

1955, p. 201). Also reported, in ppm, and included in totals: Li, 0.01; Rb,

0.01; Cs, 0.01; As, 1.9; Sr, 0.00X; Ba, 0.00X; V, 0.5; Cr, 0.004; Mo, 0.0009; Ti

0.2; Ge, 0.0O0OX; Be, 0.0000X; Ga, 0.0000X; Cu, 0.03; Pb,0.07; Zn, 0.14; Bi, 0.0001 Sb, 0.0001; Sn, 0.0002; Co, O.O00X; Ni. 0.000X; Cd, 0.0001; Ag, 0.001; In, 0.0001 Au, 0.00000; Zr, O.OOOX; NO2, 0.000; HPO( , 6.1; CO2, 66; HSO3, 0.6; S2O3, 0.3 SsOe, 0; SsOs, 0.

11. Ketetahi, one of group of springs and fumaroles in hydrothermally altered area on north flank of Tongariro, a large active andesitic volcano south of Lake

Taupo, North Island, New Zealand (Wilson, 1953, p. 453, 456; J. Healy, written communication). Analyzed by S. H. Wilson; converted from milliequivalents and millimoles per liter; SsO« included by Wilson with S4O8.

Table 21.

Chemical analyses of thermal bicarbonate sulfate waters in volcanic environments

Analysis 1 "The Geysers," Sonoma County,

Calif.

2 Steamboat well GS-7, Washoe County, Nev. May 22, 1952

3 Sulphur Springs,

St. Lucia Island, British West Indies July 1951

4 Yonono, Kagoshima

Prefecture, Kyushu,

Japan

1953

5 Name and location Wairakei well 5, North Island, New Zealand

SiOi —

ppm

66

58

108

186

epm ppm

146.0

9.3 4.5

epm ppm epm ppm epm ppm

191

121.7 230

171.2

.2

epm Ca_. 2.89 8.88

.78

.15

0.30 62

11

} 64

3.09

.90 2.70

41

17

f 25

I 12

2.05

1.4 1.09

.31

0.60 Mg .14 Na - - .40

.12

10.00 K .43 Li .17 NH4- 111 6.15 .1 .01 .01 18.85 0.82 6.69 4.86 11.35 HCO3 176

2.7

763

1.5

2.88 21 None0.34 272 4.46 254 4.17 670 10.98 COs..-

Sj03 .02 15.89

.04 so« 24

.5 Tr

1.3

.50

.01 80

23

1 1

1.67 .65 22

5.1 .46

.14

112.7

3.7

.23 CI. .08 F .19 NOi B 15 2.2 Tr

.5 CO2

H:S 2.4 Total anions 18.83 0.85 6.78 4.77 11.48 Total, as reported 1.330 83.0 513 378 1,140

Specific conductance., .micromhos at 25° C 856.5 U61

0.64

.0

.48

.00 40

50

.0 3

7157.9 Boiling

0.95

.17

pH 7.5 69

1.6

.41 .48

6.7 Temperature °C

Ratios by weight: Ca/Na

100

3.2

1.9.33

Boiling

0.052 Mg/Ca .14 K/Na .074 Li/Na .0052 HCO3/CI 120 510

123.5.0

.05

514.4 250 SO4/CI 4.1 F/Cl 14

B/Cl 10 .44 .02

» Components mentioned in explanation of table. EXPLANATION FOR TABLE 21

1. "The Geysers," Sonoma County, 11 miles east of Cloverdale, Calif.; Witches

Cauldron spring on bank of Geyser Creek about 125 ft southwest of steam wells

1 and 2 and 400 ft north of Devils Kitchen spring (table 20, analysis 1; Allen and

Day, 1927, p. 33, fig. 1) and in same geologic setting; no true geysers in the area. Analyzed by E. T. Allen, who also reported and included in totals: Al, Ni, and

Cr, each ppm; Mn, 0.6 PPm; Fe, trace. See gas analysis 24, table 28, for well 1. 2. Drill hole GS-7, in Silica Pit, western part of Steamboat Springs thermal area. Washoe County, Nev. (White, 1955a, p. 103, 111; 1957a, p. 1649-1650). Drill hole penetrated acid-leached granodiorite for 112 feet, where acid water was

found. Relations indicate high-temperature steam, COj, and other gases rising near bottom of hole, at depth of 402 ft, and condensing in a perched water table that is dominantly of meteoric water. Sample collected near bottom of steamfiUed hole under pressure; analysis by n. Kramer, U.S. Geol. Survey. Analysis

not previously published. For gas analysis see table 28, analysis 31.

3. Sulphur Springs, St. Lucia Island, British West Indies; boiling spring in southeastern part of thermal area, Hi miles southeast of Soufricre at altitude of 800

to 900 ft; little or no discharge (G. Bodvarsson, written communication) . In

Tertiary sandstone and conglomerate overlain by basaltic lava near contact

with siliceous porphyritic plug situated a few miles from Qualibu, an active volcano that erupted in 1766 (Perret, 1939, fig. 1). Sample collected by G.

Bodvarsson; analyzed by U.S. Geol. Survey; boron reported "slightly greater than 1 ppm." Analysis not previously published.

4. Yonono hot spring, in Kirishima volcano group, Kagoshima Prefecture, Kyushu,

Japan; hot spring is in area 150 by 500 ft with many fumaroles of high temperature. In pyroxene andesite lava on southern flank of one of Recent cones of the volcano group. Test boring to 280 ft depth found water at a temperature of more than 125° C. Analyzed 1953 (Subterranean Heat Research Group, 1955, p. 585; H. Kuno, written communication). Also reported is Fe, trace.

5. Drillho'ie 5, western part of thermal area, Wairakei, North Island, New Zealand

(Wilson, 1955, p. 37). Nearly 1\i miles northwest of well 4 (see table 17, analysis

14), in similar bedrock (Steiner, 1955, fig. 6, fig. 10) but hydrothermal alteration characterized by albite rather than by potassium-bearing minerals. Sample

analyzed by S. H. Wilson. Gas analysis, table 28, analysis 32, is from well 6, which has water similar to that of well 5 but is 1,000 ft to the east (Wilson,

1965, p. 29).
F48 DATA OF GEOCHEMISTRY

Table 22.Chemical analyses of spring waters high in sodium bicarbonate and boron

1 2 3 Crabtree, Lake

County, Calif. Oct. 6, 1956

4 Gilroy, Santa Clara County, Calif. June 16, 1955

t E. of Altoona mine,

Trinity County, Calif. Oct. 16, 1956

Mud Springs, Mendocino County, Calif. Oct. 7, 1956 County, Rumania Mar 3, 1943

SiOj ppm

82 epm ppm38 epm ppm

200

.4

.0

.1 1.0 62 208

1,71034

4.1 10

epm ppm

100 epm ppm

16 Tr

2.6

.1 Tr

541 314Tr

1,65033 18.7

epm

AlFeMn —

As .13 48

1693.7

5,400

1702.7

.0

Ca... 409

7.2 3.7 3,520 306

10

20.41 .59

.08

153.1 7.83

1.4

2.40

13.9.08 234.9

4.35

.39

3.09

17.1 211204.6 270

5.1

.2 2.4

1.05 9.87

.10

11.75 .13

.02

.13

27.0 Mg 25.8 SrNa .. 74.4.87

.59

71.8 K - - - .84 Li 1.25 NH«

Total cations 183.4 256 196.1 23.1 126.7

8,370

483 1,350

14,500

26

610

.4

2.1.5

.0

530

3,890

16 1,200

.6

41.6 194

290

1,200

5 130

.4.0

.3

HCO3 137.2 238 63.8 19.7 6,770 111.0 COa. . —

SO< 10.06 38.1

. 54 17^20 .02

.03

.01

.33 33.8

.03 .05

.01 2.04

.10 3.67

.02

3.2

554

.6 2.7

2.5

.07 CI 15.62 F .03 Br - .03

I .02 NOj

NO3 . B 120 13 47 COj. . 2,380 HjS.. <1 .2

185.4 256 1 100.

1

23.5 126.7

Total, as reported 14,700 21,500 7,720 1,870 12,300

Specific conductance micromhos at 25°C 13,6006.8

13.5 1.007

0.12

.018

.087 .0028 6.2

.36

16,7007.3

181.013

0.0089 3.5

.031 .0005 24

.043

.0007

.003 .0025

.87

7,8506.7

41.6

1,3406.8

42 pH (') Temperature "C.

Density at 20°C_ .. 5.5

1.008 Ratios by weight: Ca/Na 0.036 3.3

.020

.0024 3.2

.013 .0005

.003 .0013

.24

0.078

5.7

.019

.0007 9.2

.04 .003

.000

.002

.10

0.33 Mg/Ca

K/Na

.58 .020 Li/Na .0053 HCCh/Cl' 12 SO«/Cl .0057 F/Cl .001 Br/CI .0049

I/Cl .0045 B/Cl .089 .084

Analysis 6 Chokrak, Kerch, Crimea, USSR7 Essentuki, Caucasus, USSR8 9 kkaido,1 Te Aroh

Island, Ne

D Name and location Malkinsk, Kamchatka,

USSR

Sept. 28, 1950

Futamata, Ho

Japan

1936

a, North Date of collection w Zealand

BiOj ppm14 epm ppm epm ppm

204

.0 20

.0 i.4

301

61

epm ppm

51 .7 3.5

epm ppm

115.8 Tr

epm

Al 7 FeMn

As .4

8

4 Ca 7482

3.69

6.7

157847.83 6.915.03 5.0554 35627.64 29.30.40 Mg .3 SrNa 1,770

81 77.02.07 3,440

10

1

149.6.26

.1

728

25 31.66.63

2,390 614103.9

15.70 3,1604015

4

137.5 K 1.02 Li .72 NIL 23

1,990

1.27 5.4 .30 .22 Total cations 90.7 164.7 52.3 176.8 140.2

5,990 2,040 6,440 6,660

199 388

581

HCO3 32.6 98.2 33.48 105.6 109.2 C03 . 6.63 SO< 227

1,620 4.7345.7 Tr691

.6

.1.0

125 2,4402.60

68.6

8.08 CI 2,350 66.3 19.46 .03

.00

16.38 F

Br 16

12 .20

.09 51.1 .06.01 Tr

Tr

Tr

I .3 NOi

N03 B 44

171 •360

1 12 7.9 59

685

132 COj

H2S

Total anions •83.3 164.6 53.0 177.0 140.3

6,480 12,100 4,080 13,700 11,300

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS

Table 22.Chemical analyses of spring waters high in sodium bicarbonate and boron—Continued

F49

Analysis Name and location. Date of collection.

Chokrak, Kerch, Crimea, USSR

Essentuki, Caucasus, USSR

Markinsk, Kamchatka,

USSR

Sept. 28, 1950

Futamata, Hokkaido, Japan

1936

Te Aroha, North

Island, New Zealand

Specifio conductance jnicromhos at 25°C. PH.

Temperature °C_

Density at 20°C

Ratios by weight: Ca/Na

Mg/Ca

K/Na

Li/Na HCOj/Cl» SOJCl

F/Cl

Br/CI

I/Cl B/Cl

Cold

7.3

1.00

0.042

1.1.046

14.0

1.2.14

0.046

.54 .0029 .0003

2.5

.0099

.0074

.027

.0021 .00046

.0051

6.2

5.6

0.41 .20 .034

3.0

.00 .0009

.0001 .0000

.011

6.6

421.008

0.23

.64

.26

2.6

.051

.024

8.3

85 H

0. 0025

.5.013

.002

12.67

.000

.0005

.23

i Components mentioned in explanation of table.

J Includes C03 as HCOs. EXPLANATION FOR TABLE 22

1. Springs, in NWH sec. 19, T. 38 N., R. 5 W., Trinity County, Calif., about 6 miles

east of Altoona quicksilver mine. Discharge about 2 gpm from landslide material on fine-grained diorite of pre-Tertiary age. Collected by E. H. Bailey; analyzed by C. E. Roberson, U.S. Geol. Survey. Springs evolved some gas and deposited a little travertine. Analysis not previously published.

2. Mud Springs, Mendocino County, Calif.; northeasternmost of a group of springs and small mud volcanoes near crest of ridge, 6 miles west of Laytonville (Waring, 1915, p. 176-177; Bailey and White, 1957, p. 1818). Spring is 6 ft in diameter;

discharge is about 0.05 gpm muddy water, from graywacke and shale similar

to Mesozoic Yager Formation and is accompained by abundant gas that is probably largely COs. Analyzed by C. E. Roberson, U.S. Qeol. Survey;

analysis not previously published.

3. Southeasternmost spring of two warm springs In Crabtree area, northeast bank

of Rice Fork of Eel River, In NE>4 sec. 36, T. 17 N., R. 9 W., Lake County,

Calif. Discharges about 20 gpm from serpentine adjacent to shale of Mesozoic

Franciscan Group. Serpentine at creek level is altered to opal and carbonate and contains veinlets of marcasite and realgar. Analyzed by C. E. Roberson,

U.S. Geol. Survey; when combined nitrogen was determined nearly 4 months

after analysis was begun, all of it was nitrite but it probably was NIL when

sample was collected; pH and HCOj were determined immediately after bottle was opened and are considered reliable. Spectrographic analysis of evaporated

residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated

residue at 180° C, 6,140; Al, 0.1; Fe, 0.1; Mn, 0.04; Cu, 0.01; Ge, 0.3; Sr, 0.4; Ba,

1.5. Analysis not previously published.

4. Main spring, EH sec. 36, T. 9 S., R. 4 E„ 200 feet above Coyote Creek, 13 miles

northeast of Gilroy, Santa Clara County, Calif. Discharges about 10 gpm

from Franciscan graywacke near serpentine. Analyzed by H. Almond and

S. Berman, U.S. Geol. Survey; analysis not previously published.

5. Benko cold spring, Arkos area, in southeastern Carpathian Mountains, Haromszek County, central Rumania (Straub, 1950, p. 46, 104-105). Discharges from

Quaternary alluvium in basin nearly surrounded by Cretaceous limestone and

shale that overlie schist. Highest in Li of 51 springs reported by Straub, who

also reported traces of Cu, Ba, and Ag; pH reported as 8.99, which is too high

for reported HCOj and COj, with CO3 absent.

6. Resort with drilled wells in cold-spring area, east border of Chokrak Marsh 1 mile from Sea of Azov and 12 miles north of Kerch, Crimea, U.S.S.R. Water

from Karagan and Chokrak Formations of Tertiary age, consisting of shale, limestone, and dolomite (Fomichev, 1948, p. 227). This is type 1 of Fomiehev;

for type 2, see table 15, analysis 9. Analyzed by I. S. Krasnikova and M. S. Suemina, 1937, who also reported HS, 247 ppm (7.48 epm); HS here included

in HjS.

7. Well 17 at Essentuki resort, Caucasus, U.S.S.R. Water, called "hydrocarbon

water", from marl and clay of early Tertiary age (Ovchinnikov, 1947, D. 116-

117). Boron determination from Shinkarenko (1948), as well as Zn, 0.08 ppm;

Cu, 0.3 ppm; Ba, 2.8 ppm. For gas analysis see table 28, analysis 33.

8. Lower cold CO2 spring with small discharge from southern part of Middle Range

of Kamchatka, U.S.S.R., in Malkinsk area of strongly metamorphosed pre- Tertiary sedimentary, volcanic, and granitic rocks (Ivanov, 1958a, p. 199-201). Collected by V. V. Ivanov; analyzed by E. F. Prokof'eva; Ti and NH» were

looked for but not found; also reported are silicic acid, 2,651 ppm, and arsenic acid 63.6 ppm, which values are considered to be misprints of decimal points, recalculated to SiCh and As. Gas analysis given in table 28, analysis 34.

9. Futamata or Ninomata springs, Tojima area, southwest Hokkaido, Japan (Mori- moto, 1954, p. 33). Discharge 240 gpm from middle Miocene andesite and

altered rhyolite tuff interbedded with sandstone and mudstone (H. Kuno,

written communication). Nearest volcanoes are Recent Yokei, 25 miles to northeast, and active Usu, 25 miles to southeast. Analysis by Tokyo Hygienic

Laboratory.

10. Periodically erupting well, 229 ft deep, in hot-spring area, Te Aroha, North

Island, New Zealand (Henderson, 1938, p. 727, 728). Springs emerge at western

base of Te Aroha Mountain, a salient on fault scrap of east margin of Hauraki

graben. Well penetrated Quaternary alluvium on andesite of Tertiaryt?) age cut by veins of quartz, calcite, and pyrite (J. Healy, written communication). Abundant gas evolved; analysis given in table 28, analysis 35. See

table 11, analysis 10, for analysis of a cold spring at Te Aroha.
F50 DATA OF GEOCHEMISTRY

Table 23--Chemical analyses of thermal waters closely associated with epithermal mineral deposits

1 Sulphur Bank

mine, Lake

County, Calif. Hg, Sb

Mar. 26, 1957

2 Abbott Mine,

Colusa County,

Calif. Hg

Mar. 27, 1957

3 Valley Mine, Napa County,

Calif. Hg

Oct. 18, 1957

4 Amedee

Springs, Lassen County,

Calif. Hg

Oct 22, 1957

5 Boiling

Springs, Valley County,

Idaho Hg

Aug. 5, 1953

6 Ngawha

Springs, North Island, New Zealand Hg, Sb

7 Rose Creek

Spring, Pershing County, Nev. Mn, W

May 22, 1957

8 Abraham

Associated metal or mineral

Springs, Juab

County, Utah Mn

Sept. 12, 1957

SIO2 ppm

42

.6

} «

.1.00 20

551.6 1.3

1,19023

4.4 464

epm ppm

161.6

.0.0

.00

64

443

• .5 1.2

1,50039

1.8 22

epm ppm

95

.1.6

.1.00

1990

4768.2

.0 2.5

epm

0.95

7.40

20.71

.21

.14

ppm

96

.23

.01 1.00

.16

16

.0

.0 1.05

227

6.8

.0.5

27

10 288

1604.5

.2

.1.00

.0.40

4.1

1 .2

epm

0.80

ppm

81 10.1

10.4 0.004

<0.

1

2.2 10.2

epm ppm

119 L°-

:

epm

1

ppm

70

.0

[ «•

.2

.00 62

27

570

19

1.6

.7

epm

3.09

2.2

24.80

.49 .23

.04

ppm

75

.0

.0

.8.06

35249

770

54

.0

.1

epm

Al — --- Fe+> Fe+3 Mn 0.03 As

0.11

.2 . 18

1 0.90

.08 Ca 1.00 4.5 3.19

36.4 17.56 Mg -._ 4.03 SrBaNa 51.8.59

.63 25.7

65.3

1.00 .26

1.22

9.87

.17

.03

74

1.9

1 .02

3.22

.05

.00

689

57 15

129

470

29.97

1.46

.72 7.15

33.50 KX — - 1.38 LiNH» .01

84.2 107.4 29.4 10.87 3.38 40.3 30.9 56.5

3,290

598 644

1.0

1.6 3.2

.0

2,710

467

1,900

1.0 3.8

6.3

144

1,490

16 229

1.3

1.0.8

.0

.3 67 <1

79

27

12

14

11

1,280

102 235

5.5

.2

.0.00

.8.8 9.6

142

704

1,4804.5

1.8

.1.1 2.5 1.O6

.9

HCO3 53.9 44.4 24.4

.33 6.46

.07

.01

.01

.44 .33 6.00

4.51 .24

.00

.00

1.29 .90

.25

.40

.58

7.70 21.0

2.12

6.63

.29

.00

.01

2.33 COj

S04 ~- - — 12.45

18.16 .05

.02

.03

9.72

53.6

.05 .05

.05

.30

.06

332

929

6.91 26.20 14.66 CI 41.7 F _. .24 Br .- Tr .02

I .00 NO2 .00 NOj .5 .01 .04 P04 - B - 620

12 56 <1

.1 <1

677 H2S 9

84.6 108.2 31.3 11.52 3.43 40.8 30.1 59.0

6,970 7,2.50 2,500 841 •304 3,440 2,380 3,640

Specific conductance micromhos at 25° C - 7,4306.8

69.5

8,960

7.1 "26

2,740

6.5 32

1,2708.5

92

321

9.1

88

2,6906.4

22

5,640 pH 6.2

83

6.6 Temperature CC~ 82

Ratios by weight: Ca/Na 0.017 2.7

.012

.0037 5.1

.92

.0015 .0024

.0047

.96

0.043 6.9

.026 .0012

1.4.25 .0005

.0020

.0033 .030

0.040 4.7

.017 .000

6.5

.07

.0057

.0044 .0035

.29

0.071

.00

.030

.000 .29

1.8.028 001 .0006

.026

0.029 0.0

.026 .0003

9.6

.85

.78

0.027

.056 .082

.007 .51

.36

0.11

.44

.033 .0028

5.5

.43

.023

.0009

.000 .041

0.46 Mg/Ca - .14 K/Na - .070 Li/Na - .0000 HCO>/Cl» .096 SO4/CI-. .48 F/Cl .0030 Br/CI .000 .000

.72

.0012

I/Cl .0001 B/Cl - .006 .0006

Analysis 9 Ouray Springs, Ouray County,

Colo.

Mn, W

Sept. 3, 1958

10 Warmwaterberg Springs, Cape

Province, Union of South Africa Mn

11 Akan Mine,

Hokkaido, Japan Mn

12 Poncha

Springs, Chaffee County,

Colo.

Fluorite (Mn, W)

Aug. 29, 1958

13 Ojo Caliente

Springs, Taos County, N. Mex.

Fluorite

14 Doughty

Springs, Delta Coimty,

Colo.

Baritc

15 Mizpah mine, Tonopah,

Nye County, Nev.

Ag, Au

16 Name and location Peitou Springs,

Associated metal or mineral

North of Taipei, Taiwan

Pb

SiO' ppm49

.14 .42

.92

.00

376

6.1 »1.7

1 .05

1118.0

1.0

.3

epm ppm

15 epm ppm46 epm ppm84

.53

} .46

.10 .00

17

.2 1.4

i.l

J 190 \ 6.6

.0

.0

210

20054

11.0

.0

.00 .0

.02

.09

epm ppm

60

.3

1.2

epm ppm

21 0.5

0.7

1.6

epm

f 0.03

\ 0.06

ppm

650.7

.7

epm ppm

167 104

epm

Al 11.6 Fe+» 1 .6.9 0.03

/ _ Fe+s _._ \ 6.7

1.8 0.24.07

151 8.11 Mn 0.03 As

0.85

.02

8.26

.17

Tr

23

9.5

1.4 Tr

996

313.4 Tr

Ca__ 18.76 .50

186.0 18

17

22

8.9 1.2

.90

.49

104

74 5.20

6.10

1.15 .78

.03

43.33

.79

.49

106396.6

13 1,06062

3.1

1.2

5.29

3.21 .15

.19 46.11

1.59 .45

.07

696.33.44

.52

14141 7.04 Mg ._ 3.4 Sr... - Ba . .4 1,010 374

.01 Na 4.83

.20

.14 .02

.781 .23J

' ( 2

) 1493.4 6.48

.09 43.9 Ki - 9.57 LiNH, 205 11.36

(») 157

11 32736

Total cations 24.5 2.43 11.6 9.30 46.6 57.2 10.63 1 149.

128

1,03045

3.0

.0

2(?) .00

.9.06 .23

.0

85

1137

.2

'2,230 ()

151 231

1 16

1 HC03 ..-_ 2.10 1.39 3.44 1, 490

4.16

1.52 0.58

36.5 124.4 2.57 .37

6.81

1.02

C03 S04. 21.4

1.27 .16

.23

1.04

.01

572

307

11.92 8.653.14

6.51

.84

625

701

13.01 19.77 2,730

3,250

56.8 CI 91.7 F

Br 5.2 Tr

.07

I .00 Tr(?) NOj

NO3 .01 1.9

.2

1.2

.01 Tr PO4 10

1.9 47

1.0 B 18 HsS

Total anions 24.9 2.67 9.70 47.0 '57.2 10.77 148.5

Total, as reported 1,760 205 774 3,760 6.190 825 18,250 See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F51

Table 23.Chemical analyses of thermal waters closely associated with epithermal mineral deposits—Continued

9 Ouray Springs, Ouray County,

Colo.

Mn, W

Sept. 3, 1958

10 Warmwaterberg Springs, Cape

Province, Union of South Africa Mn

11 Akan Mine, Hokkaido, Japan

Mn

12 Poncha

Springs, Chaffee County,

Colo. Fluorite (Mn, W)

Aug. 29, 1958

13 Ojo Caliente

Springs, Taos County, N. Mex.

Fluorite

14 Doughty

Springs, Delta County,

Colo.

Barite

15 Mizpah mine, Tonopah,

Nye County, Nev.

Ag, Au

16 Peitou Springs,

Associated metal or mineral

North of Taipei, Taiwan

Pb

Specific conductancemicromhos at 25° C .

.

2,0206.8 162

994

7.6

70 pH - 7.5 45.6 8.052.4 '7.2 '46

1.003

0.023

.41 .031 .0034 9.7

.65

.069

Acid Temperature ° C~

Density at 20° C

171.004

0.1.37

.058

.0029 2.1

.89

41 90

Ratios by weight: Ca/Na 3.4

.016

.072

.009 2.8

23

.067

.000

.004

.001

0.82

.33

.40

0.089

.01 .035

.000 3.9 3.7

.20

.000 .000

.002

0.46

.091 .023

0.14 Mg/Ca 0.71 .29 K/Na .37 Li/Na HC03 /C1> 2.3

.30

.005

5.0

9.1 .000 SO( /Cl- — 1.9 .83 F/Cl

Br/CI .0074 .00 I/Cl .00 .00 B/Cl .0052 .0027 .0053

1 Components mentioned in explanation of table.

> Not reported.

» Includes COj as HCO3. EXPLANATION FOE TABLE 23

1. Spring in Sulphur Bank mine, one of the most productive quicksilver mines in the United States (Becker, 1888, p. 251-269; Everhart, 1946, p. 125-153; White,

1955a, p. 117-120), in SWK sec. 5, T. 13 N., R. 7 W., on shore of Clear Lake, Lake County, Calif. Variable discharge, ranging from about 1 to 15 gpm from

north wall of Herman Pit, about 120 ft below original surface, from bydrothermally altered graywacke and shale of Mesozoic Franciscan Formation,

overlain by Pleistocene lake beds and pyroxene andesite flow. Analyzed by

C. E. Roberson, U.S. Geol. Survey; spectrographs analysis of evaporated

residue, by Nola B. Shelley, converted to ppm in the original water: evaporated residue at 180°C, 5,220; Al, 0.2; Fe, 0.1; Mn, 0.2; Cu, 0.01; Ge, 0.2; Li, 3.6; Sr, 0.6; Ba, 0.3. Analysis not previously published. Tritium content of sample was 1.1 ± 0.2X10-

", determined by F. Begemann, University of Chicago. For gas analysis of sample from Herman Shaft, see table 28, analysis 36 (Becker, 1888, p. 258).

2. Thermal water from Abbott mine, located in NEJ4 sec. 31, T. 14 N., R. 5 W.,

Colusa County, Calif, near crest of ridge 2 miles southwest of Wilbur Springs

(see table 15, analysis 2). Drainage from Reardon Tunnel. 200-foot level, pumped from bottom of main shaft at 300-ft level. Average discharge is about

25 gpm; temperature of 26°C measured at portal of tunnel; temperature at source probably about 33°C (White, 1955a, p. 131). Ore and thermal water, accompanied by some combustible gas, are controlled by fractures and breccia zones in serpentine and Upper Jurassic Knoxville sandstone and shale. Water

sample analyzed by C. E. Roberson, U.S. Geol. Survey; spectrographic analysis

of evaporated residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated residue at 180°C, 6,930; Al, 0.06; Fe, 0.04; Cu, 0.006; Li, 2.1; Rb, 0.06; Sr, 0.5; Ba, 0.2. Analysis not previously published.

3. Water from Valley quicksilver mine, Aetna Springs Resort, Napa County,

Calif., SWH sec. 1, T. 9 N., R. 6 W. (White, 1955a, p. 130; Yates and Hilpert,

1946, p. 260; Waring, 1915, p. 156-159). Water pumped trom shaft of old mine

in opalized silica-carbonate rock (altered serpentine) near contact with Knoxville shale and sandstone. Analyzed by H. C. Whitehead, U.S. Geol. Survey;

spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted

to ppm in the original water; evaporated residue at 180°C, 1,870; Al, 0.08; Fe, 2.1; Mn, 0.06; Cu, 0.2; Ni, 0.02; Ge, 0.07; Li, 0.08; Rb, 0.02; Sr, 0.3; Ba, 0.3. Analysis not previously published.

4. F. W. Dickson spring A-l, 1,000 ft south-southwest ol old Amedee railroad station, east side of Honey Lake, Lassen County, Calif. (Dickson and others, 1957). Cinnabar, metacinnabar, and minor travertine deposited in vent. Total dis- charge of group is about 1,000 gpm from thick alluvium of Honey Lake basin. Collected by J. Feth and S. M. Rogers; analyzed by J. P. Schuch, U.S. Geol. Survey, who also determined Ti, 0.02 ppm; Cu, Pb, Zn each 0.00 ppm; H2 S 0.2 ppm (sample of May 22, 1957). Spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in the original water: evaporated residue

at 180°C, 850; Al, 0.04; Fe, 0.02; Mn, 0.003; Ti, 0.005; Cu, 0.01; Pb, 0.009; Mo,

0.06; W, 0.2; Cr, 0.002; Ge, 0.02; Ni, 0.02; Sr, 0.06; Ba, 0.05. Analysis not

previously published.

5. Largest spring, near north end of spring terrace, Boiling Springs, NW)4 sec. 22, T. 12 N., R. 5 E., on west bank of Middle Fork of Payette River in Valley County, Idaho. Discharges about 30 gpm; total discharge of croup is about

125 gpm. Springs emerge from shear zone in granodiorite of Idaho batholith,

associated with carbonate-cemented terrace gravel, and have deposited small, amount of calcite, cinnabar, metacinnabar, and manganese oxide (White

1955a, p. 124-125). Analyzed by H. Kramer, U.S. Geol. Survey, who also reported Sb 0.1 ppm; Hg, 0.0 ppm; spectrographic analysis, in ppm, indicate Fe, 0.4; Al, 0.1; Mn, 0.004; Cu, 0.01, Al', 0.005; Sr, 0.2; Cr, 0.003; Li, 0.02; and

B, 0.3. Analysis not previously published.

6. Ngawha Springs, North Island, New Zealand; "Jubilee" Bath of area Gof Fleming (1945, p. 255-276) near Tuwhakino Lake. Discharge is apparently slight; temperature at surface is 43°C; at sandy bottom, 83°C. Springs are in late Quaternary lake sediments overlying elaystone of Kaeo Series of Late Creta- ceous to early Tertiary age. Miocene and late Quaternary basalts are within a few miles of the area. Springs have deposited cinnabar and a little stibnite (Henderson, 1944, p. 60; White, 1955a, p. 123-124). Water analyzed by L. R.

L. Dunn, I. C. McDowall, S. H. Wilson, and M. Fieldes of the New Zealand Dominion Laboratory. Li determined by spectrographic analysis; also re- ported are Rb, 0.5 ppm, and Ca, 0.1 ppm. For analysis of gas from Velvet Bath, about 50 feet to south, see table 28, analysis 37.

7. Travertine-spring terrace near north end of East Range, about 2 miles southwest

of Rose Creek and 12 miles southwest of Winnemucca, sec. 28, T. 35 N., R. 36

E. Pershing County, Nev. (White, 1955a, p. 134). Discharges about 1 gpm

from travertine and Quaternary sand and gravel containing as much as 9 per- cent Mn and 0.3 percent WO3. Water sample analyzed by J. P. Schuch, U.S.

Geol. Survey, who also reported 0.03 ppm Ti; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 1,700; Al 0.02; Fe, 0.02; Mn, 0.09; Be, 0.002; Cu, 0.002; Sr, 0.2; Ba, 0.2. Analysis not previously published.

8. Abraham Springs, Juab County, Utah; orifice in east fork of north ditch, about

200 ft north of crest of travertine cone; same as spring 2 of Callaghan and Thomas

(1939, p. 908-912; White, 1955a, p. 133-134), 19 miles north-northwest of Delta. Discharge of spring about 25 gpm; total discharge of springs in area about 1,200 gpm. Springs discharge through Pleistocene Lake Bonneville sediments overlain by travertine-spring deposits containing manganiferous zone about 1 ft below surface. Pleistocene basalt &ow issued about 4 miles northwest of

spring, with flow front only 1,500 ft to west. Water sample analyzed by J. P. Schuch, U.S. Geol. Survey; spectrographic analysis of evaporated residue, by

Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 3,740; Fe, 0.02; Mn, 0.3; Cu, 0.004; Li, 1.1; Rb, 0.2; Sr, 8.2; Ba, 0.2. Analysis not previously published.

9. Spring at southwest edge of Ouray, Ouray County, Colo., and about 40 ft above

valley floor, issuing from terrace of travertine; Mn and Fe oxides lie on Pleisto- cene gravels and Mississippian Leadville Limestone. Discharges about 15 gpm; temperature is 59°C at surface of wood-framed vent; 62°C at 6-ft depth; no

gas. Flocculent deposit from present spring water contains 15 percent Mn, 7 percent Fe, and 0.2 percent W; a high-grade Mn oxide veinlet from the western

part of the terrace contains, in percent: Mn, 50; Fe, 0.1; W, >1; Pb, 1; Cu, 0.05; Zn, 0.3; V, 0.015; Mo, 0.003; Be, 0.03; Ba, 0.7; Sr, 0.5; Sb, 0.5; and La, 0.01. Water

sample analyzed by H. C. Whitehead, U.S. Geol. Survey; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 1,760; Al, 0.05; Fe, 0.03; Mn, 0.9; Ti, 0.02; Cu, 0.02; Ag, 0.002; Mo, 0.02; Sr, 1.7; Ba, 0.05. Analysis not previously published.

10. Warmwaterberg Springs, Cape Province, Union of South Africa. Springs

discharge from Table Mountain Series of Devonian age. Deposits estimated

to contain 600,000 tons, containing (in weight percent): Fe203 , 57H; MnO, 0.55; MnOz, 8.55; BaO, 1.45; and P2O5, 1.18 (Kent, 1949, p. 240, 243, 245, 247). Age of deposit estimated to be 850,000 years, if all Fe and Mn in present water are deposited at constant rate. Analyzed by W. Sunkel and P. Kok, 1947; Mo, 1 ppm; Ba, 7 ppm; Sr, 8 ppm; Li, 0.2 ppm, determined by spectrograph.

11. Akan mine, Hokkaido, Japan; hot-spring deposit is mined for manganese on

south slope of Mea-kan-dake, a pyroxene andesite volcano. Spring is hottest

of 4 manganese-bearing springs; the deposit is more than 6 ft thick, the. ore aver- ages about 25 percent manganese, and one sample analyzed for Co contained

0.2 percent. Analysis from Kimura and Shima, 1954.

12. Largest of several hot springs about a quarter of a mile southeast of Poncha Springs

fluorite deposit and 5 miles southwest of Salida, Chaffee County, Colo. (R. T.

Russell, 1947; 1948). Total discharge of hot springs reported to be 500 gpm and maximum temperature 75^°C (Stearns and others, 1937, p. 133), but pns^ut

discharge of this spring is estimated as 30 gpm and total of the group is perhaps

50 gpm. Springs emerge from fault in Precambrian gneiss overlain by travertine deposit of calcite, minor opal, chalcedony, tungsten-bearing manganese

oxide, and fluorite; Poncha Springs fluorite deposit controlled by same fault; late Tertiary rhyolite and andesite are within a few miles of springs. Water

sample analyzed by H. C. Whitehead, U.S. Geol. Survey, who also reported Cu and Pb, each 0.00 ppm, and Zn, 0.07 ppm; spectrographic analysis of evaporated residue, by Nola B. Sheffey, converted to ppm in original water: evaporated residue at 180°C, 1,250; Al,0.2;Fe, 0.04; Mn, 0.02; Ti, 0.01; Cu, 0.08; Mo,

0.08; Cr, 0.003; Ge, 0.01; Sr, 0.4; Ba, 0.1. Analysis not previously published.

13. Soda Spring, 12 miles northwest of Barranca, Taos County, N. Mex.; total dis- charge of Ojo Caliente springs is about 350 gpm (Steams and others, 1937, p. 167)

.

Springs issue from travertine near fluroite- barite vein containing minor amounts

of gold and silver; an inactive travertine terrace lies about 500 ft above present

springs (Lindgren, 1910); bedrock is fine-grained gneiss overlain by andesite

tuffs. Analyzed by W. F. Hillebrand, 1893 (Clarke, 1924a, p. 192-193), with HCO3 calculated from reported carbonate. Temperature, F, NO], and pH

from similar sample of same spring collected October 6, 1949, and analyzed by

L. S. Hughes, U. S. Geol. Survey.

14. Drinking Spring, 3 miles southwest of Hotchkiss, Doughty Springs, on North

Fork of the Gunnison River, Delta County, Colo. Discharges 5 to 6 gpm
F52 DATA OF GEOCHEMISTRY

EXPLANATION FOR TABLE 23—Continued

(Headden, 1905, p. 1-8, 15-16; George and others, 1920, p. 213, 313). Springs emerge near base of cliff of Dakotaf?) Sandstone of Late Cretaceous(?) age and

have formed a travertine-barite deposit 400 ft long, 115 ft wide, and about 20 ft thick. Deposit near Drinking Spring and several other springs is nearly pure BaSO( . Sample collected and analyzed by W. P. Headden (1905, p. 15-16); total C Oj, 3,080 ppm, of which 1,070 ppm is here assigned by difference of anions and cations to HCO3 and 2,010 ppm considered as free CO2. Phosphate analysis by George; trace of Zn reported by Headden.

15. Water from drill hole, 2,316-ft deep, which was started at 1,500-ft level of shaft of Mizpah mine, Tonopah district, Nye County, Nev., and penetrates to a point

816 feet below that level (Bastin and Laney, 1918, p. 26-30). Silver-gold ores

largely in hydrothermally altered intermediate volcanic rocks of Tertiary age

(Nolan, 1935, p. 1-49; White, 1955a, p. 138-139). Trace of Zn elso reported.

16. One of springs of Peitou group, north of Taipei and near north end of Taiwan;

group formerly known as Hokuto Springs; one of the springs deposited hokutolite, a lead-bearing variety of barite (Okamoto, 1911, p. 21). May be Peitou

Valley hot spring 1 of Yen (1955, p. 136, 139), which has present temperature of 68°C and discharge of 260 gpm. Water issues from or from very near Pleistocene

basalt flows that overlie marine sedimentary rocks of Mio-Pliocene age. Analysis converted from hypothetical compounds, H+ 54 ppm (54 epm) probably

calculated by difference and is included in totals; trace of Pb reported.

Table 24.-Chemical analyses of nonthermal, saline and acid waters from mines and from acii-forming areas

L 2 ? 4 Comstock Lode,

Storey County, Nev. Tonopal

Nye Cou

5 Homestake mine, Lawrence County,

S. Dak.

Dec. 20, 1957

Centennial mine, Houghton County,

Mich.

Aug. 22, 1956

Greenwood mine, Marquette County,

Mich. Date of collection... Mar. 25, 1952

nty, Nev.

SiOj - ppm

19..35

} .06

.00

epm ppm

<10

5.4

1.0 2.5

epm ppm

6.8

.0

1.2

1.9

epm ppm

576 9,000

/ .

epm ppm

15

3

7

epm

Al - 1.000 33 Fe+2 25

1 469

841

25. 20 30.61 Fe+3 -- - -- Mn 75 2 73 Ni _ - Cu - (') 148 4.66 ZnCa _ 5.2

2.4

373

10.3

.4

0.26

.20

16.22 .26 .04

.02

62,900

179

11, 90038

7.0 <10

3,140

14.7 518

.97

1.01

452

155 1,080

54

22.56

12.7 47.0

1.38

1,160 6,240

} 498

57.9 51321.7

249

10

/ 135

I 12

12.43 Mg - .82 Na 5.87 K --- - .30 LiNH< H -

17.00 3.670 '83.8 1,650 22.7 HCO3 884 14.49 24 0.39 28 0.46 HSO4 --- - S04 -- _ 6.7

2.8

38

5.5

.26 .06

.00

3.5

.04

.6

.14

.07 1.07 .29

.00 .00

88 1.83 2.1 .04 78,600 1,636 1,020 21.2 SO3 - --- CI -.- 128,000 3,610 3,030

.4 85.5

.02

120 3.38 65 1.83 F

Br 997

3.2 <1

<25

12.47

.03

0? I . 0? N02 . —

NO3 - - .06 .0

.0

11 PO< - - B 2.5

16.12 3,620 86.0 1,640 23.0

Total, as reported 1,350 204, 000 1 4, 830 97, 700 1,590

Specific conductance micromhos at 25° C.

pH.._

1,4207.6

39

8,380

5.4

13 6.5Cold

1.174

4.3

.0028 .0032

.0006 .00018

. 00069

Acid Cold

1.07

2.3 6.7

Temperature- ° C—

Density at 20°

•>

Ratios by weight: Ca/Na 0.014

.46 .027 .0008 23

.18

.14 .007

.002

.02

0.42

.34 .050

1.8 Mg/Ca .04 K/Na .087 Li/Na HCOs/Cl .0092

.00069

.0001

.00 660

.00 SO4/CP 16 F/Cl

Br/CI .. .0078

.00003

.00002

.00 I/Cl .00 B/Cl .0036

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F53

Table 24.Chemical analyses of nonthermal, saline and acid waters from mines and from acid-forming areas—Continued

6 Butte district, Silver Bow County, Mont.1 8 Cananea mine, Sonora, Mexico

9 1 Kinkei spri Prefectui

1) Red Mountain district, San Juan County, Colo. Dec. 1933

"Poison" spring, Washoe County, Nev.

Qg, Tochigi

e, Japan

SiOi ppm

48

84

epm ppm

66

29

epm ppm

56

22

524

epm ppm

98 epm ppm107

107

/ 284

\ 235

.3.06

1.0

.1

153.2

1

(')

epm

Al 9.33 3.2 2.5

18.76

11.9 Fe+» \ 1400 no

1.6 12

142.0

.36

.02

.06

10.17 Fe+S 160

12

'.5 59 852

13362

40

13

8.59

.44

.00 1.85 26.06 6.63

5.09

1.74

.33

37

.07 1.98 .00

12.6 Mn 153 5.57 .01 Nl .00 Cu - 2.0 .06 60 252

75386

} 198

1.89

7.70 37.57 7.07

8.61

.03 Zn .00 Ca 164.3

4.2

1.1

.79

.35

.18

.03

283

39

f 65

1 -9

14.12 3.2 2.83

.02

.75 Mg .26 Na - .04 K

LiH — 3.3 3.3 3.8 3.8 161.4 9.89 89.7 62.6 39.6 HCOs

HSO« 387

1,690 3.99 8O4... 2,670 55.6 466 9.70 4,460 92.9 3,100 64.5 35.2 SOs

CI 13 .37 22 .62 6.0

1.0

.17 .05 18 .51 F

Br.

I _. NOa

NOj

PO4 B .2 (i)

Total anions .. 56.0 9.70 93.5 64.7 39.7

14,200 629 6,590 4,010 2,850

Specific conductance micromhos at 25° C„

pH 1 Acid Acid Acid 2.45 Cold2.4

9 Density at 20° 1.0011

3.8

.26

.26

1.003 Ratios by weight: Ca/Na 3.3

.47

.33

3.8

.11 4.4.14

.01

15 Mg/Ca .21 K/Na .0 Li/Na HCOs/Cl .0 210

.00 200.00 520

.2

.00 SO(/Cl» 120 F/Cl . Br/CI

I/Cl B/Cl .03

1 Components mentioned in explanation of table.

» Includes HSO». EXPLANATION FOR TABLE 24

1. Water from cavity penetrated by drill hole started at 5,600-ft level, at the thenexisting bottom of Homestake gold mine, Lawrence County, S. Dak. (see Noble, 1950, p. 234, 235). Collected by A. Slaughter of Homestake Mining Co. and analyzed by H. C. Whitehead and J. P. Schuch, U.S. Geol. Survey, who

also determined Cu, Pb, As, Ti, each 0.00 ppm; Zn, 0.04 ppm. Spectrographic

analysis of evaporated residue by Nola B. Shefley, converted to ppm in the

original water: evaporated residue at 180°O, 911, Al 0.03; Fe, 0.01; Cu, 0.0009; Cr, 0.003; Sr, 0.2; Ba, 0.06. Analysis not previously published. Similar to analysis of Noble (1950, p. 234, 235) except that all forms of sulfur are lower.

2. Water from 7,075 ft south on 48 level of Centennial No. 2 shaft of Calumet and

Hecla copper mine, Houghton County, Mich., and about 3,000 ft vertically below surface. Rate of flow about 1 drop per second from back of drift in Kearsarge amygdaloid; water was clear when collected by A. Schillinger, of Calumet and Hecla, Inc. Analyzed by C. E. Roberson, U.S. Geol. Survey.

Spectrographic analysis of evaporated residue by Nola B. Sheffey, converted

to ppm in the original water; evaporated residue at 180° C, 225,000; Al, 4.5; Fe, 3.2; Mn, 0.7; Cu, 0.7; Li, 1.1; Cs, 9.1; Sr, 320; Ba, 4.1. Analysis not pre- viously published.

3. Water flowing from drill hole 162 on 5th level of Greenwood iron mine, Marquette

County, Mich., 183 feet below sea level (Stuart and others, 1954, p. 10-11,

86-87); highest in salinity of analyses reported by Stuart. In bedrock of this area, mineral content of water increases with depth, with CI, in general, increas- ing very rapidly; at first, Na increases in proportion to CI, but at greater depths Ca increases more rapidly than Na (Stuart and others, 1954, p. 86). Water

from Goodrich Quartzite of Upper Huronian age, immediately above the iron- formation. Sample analyzed by U.8. Geol. Survey; also reported and included

in totals are Sr, 6 ppm (0.14 epm); Ba, <0.5 ppm. See table 9, analysis 4, for a water of low salinity in the Cliffs Shaft iron mine of Michigan.

4. Water from Central tunnel of Comstock Lode, Storey County, Nev.; an acid mine water (Rcid, 1905, p. 192) from hydrothermally altered andesite and other

rocks containing pyrite (Coats, 1940; Thompson, 1956; White, 1955a, p. 139-140). Analysis reported as hypothetical oxides in mg per 1, converted to ppm by

assuming a density of 1.07. Also reported are Ag, 0.2 ppm; and Au, 0.004 ppm.

5. Water from West End mine, 500 ft level, Tonopah district, Nye County, Nev.

(Bastin and Laney, 1918, p. 29); water is acid owing to oxidation of sulfides, and

apparently cold, in contrast to deep thermal Tonopah waters (see table 23, analyis 15). An epithermal silver-gold deposit in hydrothermally altered Tertiary volcanic rocks (Nolan, 1935; White, 1955a, p. 138-139). Also reported Is a

trace of As.

6. Water from crosscut on 1,200-ft level, St. Lawrence mine, Butte district, Silver Bow County, Mont. (Lindgren, 1933, p. 62), in oxidizing sulfides of copperbearing hydrothermally altered quartz monzonite of Boulder batholith. Also

reported and included in totals: Sn, 17 ppm (0.57 epm) Cd, 41 ppm (0.73 epm). Co included with Ni; and Sn may have been introduced from sample

container.

7. Water from Genessee-Vanderbilt mine near West Magnolia ore body north of Silverton, Red Mountain district, San Juan County, Colo., from altered andesite with disseminated pyrite (Burbank, 1950, p. 293, and unpublished analysis). Sample collected by W. S. Burbank, analyzed by E. T. Erickson, U.S. Geol. Survey; analysis not previously published.

8. Water from Cananea mine, 900-ft Jevel, Sonora, Mexico; In copper-bearing granitic rocks and porphyry intrusive into Paleozoic limestone (Lindgren, 1933, p. 63, 722-723) ; affected by oxidation of disseminated sulfides.

9. " Poison " spring on west slope of Virginia Range, NEHsec. 35, T. IS N., R.20 E., 3 miles east of Steamboat Springs, Washoe County, Nev. Water issues from

short prospect adit in pyritized andesite of Kate Peak Formation of Miocene

or Pliocene age (Thompson, 1956, p. 62-63, pi. 3) that is bleached near surface by

acid from oxidation of pyrite. Discharges about 2 gpm; sample analyzed by

H. Kramer, U.S. Geol. Survey. Ra03, 715 ppm, determined by spectrographic

analysis to be about 10 percent Fe and 90 percent Al, approximately equal to 400 ppm of metallic ions and 42 epm; Mn, Nl, Cu, and Ag (0.3 ppm) also deter- mined spectrographically. Analysis not previously published.

10. Kinkei Spring, Tochigi Prefecture, Japan; a cold spring at top of Keichyo Mountain, a Quaternary andcsite(?) volcano. Analyst, K. Kuroda (1941a, p. 234-

237); also determined, in ppm: Ti, 0.1; As, 1 (0.04 epm); Cr, 0.07; V, 0.05; Mo,

0.002; Ga, 0.001; Bi present and possibly traces of Li, Hg, and B.
F54 DATA OF GEOCHEMISTRY

Table 25.Chemical analyses of spring waters depositing travertine

2 3 Mammoth, Yellowstone Park, Wyo.

Sept. 5, 1957

4 5 Meskout

stantine Alge

[ Keene Wonder,

Inyo County, Calif. Nov. 7, 1954

Keene Wonder,

Inyo County, Calif. Nov. 7, 1954

Big Horn, Hot

Springs County, Wyo.

Sept. 1957

Lysuholl,

Snaefellsnes Peninsula, Iceland Date of collection -. Sept. 30, 1958

Province,

ria

SiOj - -- ppm

60 epm ppm

'67 epm ppm

60.2.06

.00

.5 272681.4

129

692.3

1.0

epm ppm

36

.4.04

.05

.2 374

741.7

27144

.9

.0

epm ppm

1710.00 2.6

.00

.03 13632

epm ppm

66 epm

Al - FeMn

As ..- .5 20237 Ca 8943

3.5

93242

.8

4.44 3.5

.08 40.54

1.07 .12

123

'38

'1.7

1,04045

.9

1.15 3.1

.04 45.2

1.15

.13

13.57 5.59

18.66

6.1 6.79 2.63

10.08 Mg 3.0 Sr —

.

Na - - 5.61 1.76

.33 .06

11.79

1.13 .13

40629

.5

.0

17.66

.74 .07

.00

205

47 8.92 K - 1.20 LiNH«

49.8 50.8 26.9 37.8 27.89 23.2

1,210

719 514

7.0

.9 8.6

1,07029

796

567

6.0

1.0 9.6

667

501 1702.4

4.3

2.6

756

726

3203.5

.0 7.8

5.5

1,620

38

842.2

.0.57

.2

1372

(') 381 327

HCO3 - 19.8 17.5.97

16.57 15.99 .32

.02

10.93 12.39 24.91 6.10 COj - SOt --- -- 14.97

14.49

.37

.01

10.43 4.79

.13

15.12 9.02

.18

.79 2.37

.12

7.9.1 CI - 9.2>i F .- NO3 - - B - H2S --- - 6.8

49.6 51.4 26.3 36.7 28.19 23.2

Total, as reported 3,630 3,680 11,950 2,620 2,420 1,640

Specific conductance micromhos at 25° C_. 4,6407.4 33

0.095

.48

.045 .0009 2.3

1.4.014

4,7908.4 23±

0.022

1.7

.043

.0009 2.0

1.4

.011

2,220

6.6

72

2.1.25

.53

.018 3.9

2.9

.014

1 . 0041 1.OOO6

.025

3,030

6.2

57

1.4.20

.16

.003 2.4

2.3

.011

2,370

6.4 41.6

0.34

.24

.071 .001

18.45

.026

1.002

1.000 .007

pH

Temperature „° C_-

Ratios by weight: Ca/Na

95

0.99 Mg/Ca .18 K/Na .23 Li/Na .. HCOj/CP 1.1 SO4/CL- - 1.2 F/Cl - Br/CI . I/Cl . B/Cl - .017 .017 .024

Components mentioned in explanation of table.

» Includes CO3 as HCO3. EXPLANATION FOR TABLE 25

1. Keene Wonder Spring, west front of Funeral Range, Death Valley, SH sec. 1, T.

15 S., R. 46 E., Inyo County, Calif. Sampled spring discharges about 30 gpm,

which is the largest discharge of group, near northwest end of a H-mile-long travertine terrace. Vent temperature, 34° C; water sample was collected 150 feet downstream from vent, where first significant amount of carbonate was deposited. Springs discharge through travertine, alluvium, and probably Tertiary and

Paleozoic rocks, including carbonate rocks. Collected by F. M. Byers, analyzed by H. Kramer, U.S. Geol. Survey; analysis not previously published.

2. Same spring and date of collection as that for analysis 1, but about 1,000 ft. downstream from vent, where approximately 11 percent of water has been lost by

evaporation, judging from contents of Na, CI, and B. Most of the Ca, some Sr and Mg, and minor amounts silica have been precipitated. Analysis not pre- viously published.

3. Mammoth Spring, at north end of travertine ridge, west edge of Main Terrace, Yellowstone National Park, Wyo. Discharges about 4 gpm; average total dis- charge of group about 750 gpm (Allen and Day, 1935, p. 59-60). Springs emerge

through very extensive deposits of travertine overlying pre-Tertiary sedimentary

rocks, Including abundant limestone and dolomite; also associated with late Tertiary rhyolite tuffs and basalt (Hague and others, 1899, sheets 10 and 19). Analysis by J. P. Schuch, U.S. Geol. Survey, who also reported, in ppm and

included in totals: Ba, 0; Ti, 0.03; Br, 0.7; 1, 0.1; NO2, 0; PO4O.8. Spectrographs

analysis of evaporated residue, bv Nola B. Shefley, converted to ppm in original water: evaporated residue at 180°C, 1,610; Al, 0.03; Fe, 0.04; Mn, 0.03; Ti, 0.02; Cu, 0.003; Li, 1.1; Rb, 0.2; Cs, 0.2; Sr, 0.4; Ba, 0.1. Analysis not previously published. Gas analysis from Main Terrace given in table 28, analysis 38 (Allen and

Day, 1935, p. 86, 377).

4. Big Horn Spring, Hot Springs County, Wyo.; main spring discharges about 12,600 gpm and is one of largest hot springs in world. Extensive travertine deposit

overlies Triassic red beds of Chugwater Formation near axis of anticline (Darton,

1906, p. 194-200; Burk, 1952, p. 93-95); the thermal water may rise from Tensleep Sandstone of Pennsylvanian age. Analysis by H. C. Whitehead, U.S. Geol. Survey; spectrograph^ analysis of evaporated residue, by NolaB. Sheffey, con- verted to ppm in original water: evaporated residue at 180C C, 2,320; Fe, 0.01; Mn, 0.04; Cu, 0.002; Sr, 0.7; Ba, 0.09: Also reported: NO2, 0.0 ppm; analysis not

previously published.

5. Drilled well in Lysuholl warm spring area, Snaefellsnes Peninsula, Iceland, 16 miles

east of Snaefellsjokull, a late Quaternary glacier-bearing volcano of rhyloite and

basalt (Barth, 1950, p. 122). Discharges about 40 gpm in area of recent travertine

in larger area of siliceous sinter deposited by former springs on hydrothermally

altered granophyre. Springs evolve much gas (table 28, analysis 39), and deposit FesOs as well as CaC03. Collected by G. Bodvarsson, State Electricity Authority. Analysis, not previously published, by C. E. Roberson, U.S. Geol. Survey, who also reported, in ppm: Cu, Pb, Zn, NOj each, 0.00; Br, 0.2; I, 0.0; PO», 0.06.

6. Springs at Meskoutine, 6 miles west of Guelma, Constantino Province, northeastern Algeria. Estimates of total discharge are 1,500 gpm by Braun (1872), 4,000 gpm by Urbain (1953), and 8,000 gpm by Pouget and Chouchak (1925)1 Regardless of exact amount, the Meskoutine group is remarkable for magnitude of discharge and high temperature. The springs issue from very extensive

travertine deposits, about 4 square kilometers in area, with a thickness of perhaps 120 feet, and precipitate about 2 tons per day of CaC03 from a total of about 9 tons of CaC03 in solution (Urbain, 1953). The springs rise along

faults in upper Miocene conglomerate, shale, and sandstone, underlain by

Lower Cretaceous limestone (Joleaud, 1914). The sample, probably from the main spring (Grande Cascade), was collected and analyzed by Guigue and

Betier (1951); 183 ppm CO3 was reported but is here converted to equivalent HCOj.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS

Table 26.

Chemical analyses of thermal waters that are probably entirely meteoric in origin

F55

1 Bowers, Washoe

County, Nev.

March 8, 1954

! Gar-

, Ark.

I f 4 5 Plomblers, France

Aug. 25, 1952

6 Hot Springs land County

Warm Springs, Meriwether County, Ga. June 13, 1935Kristenes, Akureyri

area, Iceland

Aug., 1949

Yuzawa Fukushima

Prefecture, Honshu,

Japan

1951

SiOi ppm

44 epm ppm

46

} 2

47

5.1 4.8

1.6Tr

epm ppm

23 epm ppm109 epm ppm'90 epm ppm

24

.2

.6 2.4

.4

111.7

epm

Al 1 Fe { .01 21

12

1.6 3.6

1.2 6.0

1.8

} 55

Ca 2.8

1.0 49

.4 1.08

0.14

.08 2.13

.01

.01

2.35

.42

.21

.04

1.05

1.0.07 .09

0.30

.15 2.39

4.9

.3

( 81

\ 5.3

0.24

.02 3.52

.14

0.12 Mg .03 Na .48 K .04 Li

2.37 3.02 2.21 2.84 3.92 0.67

3426

35

5.4

168 118 46

2449

13.7

85

76

6.8

171.1

9.4

5.6

HCOi 0.56

.86 .73

.15

2.75 1.93 0.75

.80

1.02 .37

.04

1.39 0.28 COj .04 80« - 7.8

2.5

.4.08

.3

.16

.07 7.31.8

.1.1 «.l

.15

.05

.01 .00

.00

1.58 .19 .20 CI .16 FNOs .01 PO4 .00 B -. .2

2.30 2.99 2.14 2.98 3.16 "0.73

198 284 189 306 1359 >74.3

Specific conductance- .micro-mhos, at 25° C_. 242

9.3

47

0.057

.36

.008

.002

166.5

267

9.3 75

0.11 .33

'7.5

31

13.57

2.3

7.6

65

0.06

.06 .065

9.4 Temperature.. °C..

Ratios by weight: Ca/Na -

64

9.8

.11 .33

.0 67

3.1

.0

.0

.0

.12

28

0.22 Mg/Ca .16 K/Na

Li/Na - HC03/C1> 66

4.1.06

7.3 3.8

.054

13

11 3.4 80«/Cl 1.7 F/Cl

Br/CI..

I/CI B/Cl .04

> Components mentioned in explanation of table.

» Includes CO« as HCOi. EXPLANATION FOR TABLE 26

1. Main Spring, Bowers NWM sec. 3, T. 16 N., R. 19 E., 10 miles south-southwest

of Steamboat Springs Washoe County, Nev. (table 17, analysis 3). Discharges

40 to 50 gpin from fractures in granodiorite in iootwall of basin-range fault, west

side of Washoe Valley. Accompanying gas is minor in amount and spring

deposits are absent. Analyzed by W. W. Brannock, U.S. Oeol. Survey ; LI

determination by H. Kramer, sample of March 8, 1954; analysis not previously

published.

2. Big Iron Spring, Garland County, Ark., largest and hottest of the group of hot

springs (Haywood and Weed, 1902). Discharges 15 gpm from Mississipptan Hot Springs Sandstone, which overlies Devonian Arkansas Novaculite and older Paleozic shale and cherts (Bryan, 1922, p. 426-436). Travertine deposit is as much as 8 feet thick, in places, and contains some manganese oxides (D. F. Hewett, oral communication 1957). Tritium (H3

) content of the water in March

1953 (prior to explosion of first thermonuclear bomb) was 2.5±1.4 T/HX10"

(Von Buttlar and Libby, 1955, p. 83), which is almost that of surlace water. This proves that the water is largely, if not entirely, meteoric in origin and had

a short subsurface travel time. Analysis of associated gases, evolved in proportion of 19.6 cm' per 1 of water, is given in table 28, analysis 40 (Haywood and Weed, 1902). Also reported, in ppm; Mn, 0.3; NHi, 0.04; NO2, 0.002; traces of

Sr, Ba, Br, and I, and absence of As.

8. Warm Springs, Meriwether County, Ga., east source; discharges about 620 gpm

(Hewett and Crickmay, 1937, p. 7, 17, 21). Water Issues from Hollis Quartzite, over lain by Manchester Schist and underlain by Woodland Gneiss, all Pre- cambrian in age. No spring deposits. Sample analyzed by W. L. Lamar,

U.S. Geol. Survey. U (0.6 ppb) and pH determined by U.S. Geol. Survey

from sample collected in 1950. Minor amount of gas accompanies water (see table 28, analysis 41).

4. Flowing well at Reykhusalaug, about 6 miles south of Akureyri in northern Ice- land; discharges about 25 gpm. Temperatures of small springs are about 45°C

(Barth, 1950, p. 127), but higher temperatures are obtained irom wells with

greater discharge. Hot water rises along contacts of basic dikes cutting nearly

horizontal early Tertiary(?)plateau basalts (G. Bodvarsson, written communication). Analyzed by S. Hermannson, Iceland State Electricity Authority. Gas analysis given in table 28, analysis 42, is irom same type ol water from Sydri- Reykir, north of Hvita River in southern Iceland with temperature of 100°C; analyzed by B. Lindal, State Electricity Authority.

6. Romain Spring, Plombiers, Vosges Mountains, France. Apophyllite, chabazite,

opal, chalcedony, tridymite, fluorite, and caicite are reported from pore spaces

of brick and cement of Roman baths built 2,000 years ago; crusts formed in places on masonry surfaces. Glaciated granite bedrock is unaltered (Daubree, 1879; Lovcring, 1950, p. 243). Collected by T. S. Lovering, analyzed by W. W. Brannock, L. Shapiro, and P. W. Scott, U.S. Geol. Survey, who also reported and

included in total 10 ppm of free COj. For analysis of gas of Capuchin Spring, Plombiers, see table 28, analysis 43 (Moureu, 1906). Nearly 0.3 percent of total gases is He (Moureu and Biquard, 1908).

6. Yuzawa, Fukushima Prefecture, Honshu, Japan; discharges 60 gpm from Cretaceous(?) granodiroite (Morlmoto, 1954, p. 193; H. Kuno, written communication). Analyzed by Fukushima Hygienic Laboratory, 1951, which also reported and included in totals: specific gravity, 1.0001; OH, 0.9 ppm (0.05 epm).
F56 DATA OF GEOCHEMISTRY

Table 27.Chemical analyses of waters associated with salt deposits and miscellaneous waters of high salinity

L ! 3 4 Great Salt Lake

Desert, Tooele County, Utah

5 6 Searles Lake brine, Inyo County, Calif. Searles Lake brine, Inyo County, Calif. Bristol Dry Lake, San Bernardino County, Calif.

Trona deposit, Sweetwater

County, Wyo.

Feb. 1958

Glenwood Springs,

Garfield County,

Colo.

Sept. 9, 1957

SiOj -- ppm epm ppm epm ppm epm ppm epm ppm

47

f .00

1 .00

.00

epm ppm

35

.24

.00

.08

.00 526

77 U3

6,630

158

.9

1.2

epm

AlFe } » Mn

As 198

16 243 Ca 0.80 43,300

1,070 962

67,400 3,300

2,160

88.0

21.95 2,60084.4

1,360 1,720 <10

61,600 2,650

1.8

67.9

141.5

.0 2,245

67.8.26

3.7

4.6 1.6

84,700

158

.5 1.3

0.18

.38

26.25 6.3 Sr —

Na — ' 110,000 26,000

81

19

4,790

665

11.7

1.05

119,000 15,60030

5, 220. 00 409

4.3

3,684

4.04 .07

.07

288.4 K . 4.04 Li - - .13 NEU —- .07

5,470 5,630 4,860 2,520 3,690 325

13,800

88,500 HCOi 227 7522,950 12.33 COa -- 1 27, 100 900 38,400 1,280 <10 0.0 OH -—

8-» 386

46,000

121,000

15 86029

24.1 958 3,416

.79 10.76 .22

1,810

49, 400

105, 000

15 580

25

112.9

1,029

2,960.79 7.26

.20

SO(_. 210

173, 000 4.37

4,880

3,680 86,60076.6 2,442167 21,300

1822

8.6

110

1330.0

3.48

601.95 .28

.07

1,160

10, 300

1.6 2.4

.3 1.2

.0

.9

24.2 CI . — — 290 F . .. - .08 Br <10 <10

.0

.0 .03

I .00 NOj .02 PO4 922

3,380

19.44 535 4,09011.28 B <3

H2S -

5,300 5,400 4,880 2,520 3,780 327

'336,000 1 335, 000 279,000 148, 000 209,000 1 19, 600

Specific conductance .mlcromhos at 25° C . _ 103,000

10.0 23

1.204

0.000044

1.2.0019

.00001 9.6

.0078

.00084

.0010 .00040 .0062

27,800 pH 6.6 Cold 52 Densitv at 20° C - 1.11

0.026

1.3.061 .00003

.000 .042

1.011 Ratios by weight: Ca/Na . - - 0.00015 0.75

.025

.057

.079 Mg/Ca - .15 K/Na - .24

.00074

.45 .38

.00012

.0071 .00024 .028

0.13

.00025

.73 .47

.00014

.0055 .00024

.039

.024 Li/Na .00014 HC03/C1 1 . - .073 S0«/C1 - .0012 .11 F/Cl .00016 Br/CI .000

.000 .0000

.00023

I/Cl .00003 B/Cl -- .00009

7 Salado brine, Lea

County, N. Mex.

Sept. 1957

8 Salado brine, Eddy

County, N. Mex.

Feb. 7, 1939

9 Seep from Salado, Eddy County, N. Mex.

July 17, 1958

10 Lyons well, Wayne

County, N.Y. May 3, 1956

11 Aqua de Ney

Spring, Siskiyou County, Calif. Oct. 25, 1957

12 Name and location Budapest well, Hungary

1932

SiOj. - ppm

7.9

57 '350 126

.00 9

56,700

epm ppm epm ppm

9.1 2.4

1.0 1.8

.00 430 2,090 140

95,500 3,180

2.8

1.1

epm ppm

15

.0 14.4 1.2

epm ppm

3,400

.9.00

1. 00

1 .00 2.5

.9 1.2

8,710

116

1.5 122

epm ppm

114.8

.04 .02

epm

AlFe. . Mn..

AsCa 0.45

4,660

97 38,300 4.80 3,150

21.46

172 2,04048713

11,600

107

34(?)

101.8

40.1.30

5052.74 4.9

0.12

.07 414 3,430

.08 4,070

89

.04

20.66 Mg 282 Sr .00 Na 14,300 23,800

1668

622

609

2.3 3.77

143,900

2,090

1,91063.54,154

81.40

.06

378.9

2.97 .22

6.76

177.1 K 2.28 Li .01 NHt Total cations 5,990 6,120 4,430 655 389 482

534 1,380 117 91 4,790 948

HCOj. 8.75 22.6 1.92 1.49 1,080 17.7 COj 159.7 OH 55.7 s-> SO< 6,970

200,0005.5

1,34012

5.5

145.1 5,630.29

16.8.09

.09

222,000

16,800 4,620 474

10,600

157,0003.1 350.6

.00 20

0.0

221 4,430

.16

.44

.60

2,650

21,200

1.2

55.2

598

.06

172 5,9502.0

9.2

5.4

10.00 200

400

3.58

167.9

.10

.12

.04 .20

21,300

627 443 CI 17.68 F

Br .1 .00

INOs 25

.0 .40 4.2

.6

.07 PO4. . .01 B 590 HiS

Total anions , , 5,800 5,120 4,650 655 1398 478

Total, as reported .. 304,000 325,000 269,000 38,300 25,300 31,000

See footnotes at end of table.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F57

Table 27.—Chemical analyses of waters associated with salt deposits and miscellaneous waters of high salinity—Continued

7 Salado brine, Lea

County, N. Mex.

Sept. 1957

8 Salado brine, Eddy

County, N. Mex.

Feb. 7, 1939

9 Seep from Salado, Eddy County, N. Mex.

July 17, 1958

10 Lyons well, Wayne

County, N.Y. May 3, 1956

11 Aqua de Ney

Spring, Siskiyou County, Calif. Oct. 25, 1957

12 Budapest well. Hungary

1932

Specific conductance.. mlcromhos at 25° C. 83,6005.2

178,0006.9 37

1.209

0.0045

4.9

.033 .000029

.00074

.068 .000020 .00022 .000003

.00013

54,000

6.7

10.6 1.027

0.18

.24 .0092

.0029(?) .0043

.13

.00006

29, 700

'10.

9

Cold

1.018

0.00029

.36

.013 .00017

1.6.029

.00034

.0015

. 00091

.034

Cold

1.346

0.0022

400

.048

Cold

Density at 20° C. . 1.263

0.0006

6,000

1.7.0011 .0027 .035 .000028

.0067 .000060

.0030

Ratios by weight: Ca/Na 0.10 Mg/Ca 8.3 K/Na .022 Li/Na - .00001 HC0S /C1> .082

13 1.7 804/C1 34 F/Cl . Br/CI. .0002

I/Cl B/Cl

i Components mentioned in explanation of table.

» Includes COj as HCO3. EXPLANATION FOE TABLE 27

1. Composite brine from interstices of "Upper salt" body, 90 feet thick, at Searles Lake, Inyo County, Calif. Probably representative only of brine from lower

half of stratified salt layer (G. I. Smith, written communication, 1957) Exact

location of sampled wells not known. Analysis by American Potash and

Chemical Corp., with major constituents reported as hypothetical combinations; also reported, in ppm, and included in totals: W 54; Sb 5; Rb, 1; Mo 0.7; Ge 0.3. All carbonate reported as CO3, although some may be HCO3. Analysis, not previously published.

2. Composite brine from "Lower salt" body, 40 ft thick, at Searles Lake, Inyo

County, Calif. Exact location of sampled wells not known. Analysis by

American Potash and Chemical Corp., with major constituents reported as

hypothetical combinations; all carbonate reported as COj. Also reported Is W, 31 ppm. Analysis not previously published.

3. West-central part of Bristol Dry Lake, 6 miles south of Amboy and 1 mile north of

celesite saline deposits, San Bernardino County, Calif. Sample from drain- age canal in salt body of National Chloride Co. (Dun-ell, 1953, p. 13). Analyst, W. W. Brannock, U.S. Geol. Survey.

4. Composite of 126 brine samples from auger holes few feet deep in Great Salt Lake

Desert, Tooele County, Utah. Most of the brines were interstitial in salt deposits and were analyzed principally for K and Mg (Nolan, 1927, p. 39).

5. Seep from shale immediately above main 10-ft trona bed of Intermountain Chemical Co. in Bridger subbasin of Green River Basin, Sweetwater County, Wyo.,

10 miles west and 7 miles north of Green River. Collecting point is about 1,500

feet below the surface; the trona bed is interbedded with shale, oil shale, sandstone, limestone, and evaporites of the 900-ft thick Laney Shale Member of the Green River Formation and is about 100 ft above the base of the member

(Bender Hash, Intermountain Chemical Co., written communication); dis- charge at the site was nil at first but then increased, leading Hash to believe

this water is not connate water from the trona deposits but is meteoric water

from the Tower Sandstone Member of the upper part of the Green River

Formation. Collected by Bender Hash and analyzed by H. C. Whitehead,

U.S. Geol. Survey; spectrographic analysis of evaporated residue, by Nola

B. Shefley, converted to ppm in original water: evaporated residue at 180°C,

205,700; Fe, 1.4; Ti, 0.4; Li, 1.1; Sr, 0.6; Ba, 3.1. Analysis not previously published.

6. Main spring of Glenwood Hot Spring Lodge, Garfield County, Colo. Discharges approximately 1,600 gpm from alluvium overlying Cretaceous sedimentary

rocks. The Paradox Formation of Lower Pennsylvanlan age, consisting of

salt deposits, gypsum, and other interbedded sediments, is believed to occur

at depth. Analyzed by H. C. Whitehead and C. E. Roberson, U.S. Geol. Survey, who also reported Cu and Pb, each 0.00 ppm; Zn, 0.08 ppm: NOa,

0.13 ppm. Spectrographic analysis of evaporated residue, by Nola B. Shefley, converted to ppm in original water; evaporated residue at 180° 0, 19,500; Al, 1.2

;

Fe, 0.1; Cu, 0.02; LI, 1.8; Rb, 0.8; Sr, 13; Ba, 0.4. Analysis not previously

published.

7. National Potash Co. mine, seo. 18, T. 20 S., R. 32 E., in Carlsbad area, Lea County, N. Mex. Brine seeping at 1,700-ft depth into new workings from clay on bot- tom and lower sides of postore epigenetic halite that has replaced part of the

rock salt in middle "barren" part of Tenth Ore Zone, 650 ft below top of Salado

10

11

12

Formation and 920 feet below top of Upper Permian evaporates (C. L. Jones, U.S. Geol. Survey, written communication). Discharge of about 1/40 gpm

eventually ceased. Collected by C. L. Jones; analyzed by C. E. Roberson,

U.S. Geol. Survey; spectrographic analysis of evaporated residue, by Nola B.

Shefley, converted to ppm in original water; evaporated residue at 180°O,

422,000; Al, 35; Fe, 350; Mn, 26; Ga, 0.005; Ti, 1.9; Zr, 0.06; Be, 0.002; Cu, 0.5; Pb, 0.04; Co, 0.007; Ni, 0.04; Cr, 0.1; V, 0.08; Li, 3.3; Rb, 33; Cs, 13; Sr, 0.004(?); Ba, 3.4. Analysis not previously published. The brine was accompanied by a

small amount ofodorless gas, probably similar to gas given in table 28, analysis

44, and collected elsewhere in the Salado Formation by Jones.

8. Test well Yates 1, 195 ft deep, SEMSWH sec. 24, T. 25 S., R. 26 E., Eddy County, N. Mex. Sulfate water found at 142 and 145 ft; after standing, water flowed over

casing from 142-ft zone. Water from evaporite deposits of Permian age, perhaps gypsum and anhydrite of Castile Formation ("lower Salt Series"). Sample

collected by W. B. Lang, analyzed by W. W. Brannock, U.S. Geol. Survey; Na determined by difference. Analysis not previously published.

9. Brine seep in sandbar, half a foot above level of Pecos River, near Malaga, NEJ4

sec. 20, T. 24 S., R. 29 E., Eddy County, N. Mex. Discharges about 0.1 gpm;

Probably meteoric water that has come in contact with saline deposits of Salado Formation of Permian age (C. L. Jones, written communication). Collected by C. L. Jones; analyzed by H. O. Whitehead, of U.S. Geol. Survey, who also determined Cu, Pb, and NOj, each 0.00 ppm. Spectrographic analysis of evaporated residue, by Nola B. Shefley, converted to ppm in original water: evaporated residue at 180° C, 276,500; Fe, 1.4; Mn, 0.8; Cu, 0.6; Li, 1.4; Sr, 40; Ba, 2.5. Analysis not previously published. Well, 393 ft deep, town of Lyons, Wayne County, N.Y.; penetrated the Salina Formation of Silurian age from depths of 130 to 371 ft; Salina generally consists

of shale, marly sandstone, and impure limestone, all impregnated in places with

salts. Collected by R. Heath; analysis by G. F. Scarbro of U.S. Geol. Survey, who reported total Fe and Mn, Zn, each 0.2 ppm; Cu, 0.00 ppm; Ra, 11 ft/ic per 1; U, 5.9 ppb. Analysis not previously published. Aqua de Ney Spring, Siskiyou County, Calif.; main spring is 5 miles southwest

of Mount Shasta, on the north bank of Ney Springs Creek of the Weed quadrangle. Discharges from serpentine in schistose rock (Waring, 1915, p. 264-

265). Collected by J. Feth and S. Rogers; analyzed by J. P. Schuch, U.S. Geol. Survey (Feth, Rogers, and Roberson, 1961). Water is remarkable for its very

high pH and Si02 , which may be highest on record); analysis verified 5 times at

2 laboratories. In other respects, the water strongly resembles probable connate

waters given in table 15. Also determined and included in totals: SOs 439 ppm

(10.89 epm); NO?, 0.00 ppm; Cu, 0.30 ppm; Pb, 0.00 ppm; Zn, 0.20 ppm; re- ported Mn and As from 1958 sample. John D. Hem determined Eh, —0.11;

total CO2, 2,500 ppm; and SiOj, 3,400 ppm. Spectrographic analysis of evaporated residue, by Nola B. Shefley, converted to ppm in the original water: evaporated residue at 180° C, 30,400; Al, 3.3; Zr, 0.3; Cu, 0.03; Mo, 0.09; Li, 4; Sr, 0.2; Ba, 1.1. Ferencz Joseph "bitter" mineral water from shallow well in southern or south- western suburb of Budapest, Hungary. According to Vendl (1951, p. 188-196), the water comes from middle Oligocene Kiscell Clay. Analyzed by J. Jendrassik, who also reported Ti, 0.01 ppm; free COj 15 ppm.
F58 DATA OF GEOCHEMISTRY

Table 28.Chemical analyses of gases accompanying or related to waters of tables 12 to 27, in volume or mole percent

No. and locality of sample

Related

water

analysis Tempera- ture (°C) COj CO CH«

CtHo and

re- lated gases

Ha HjS SOi NHi Oj N. A He HjBOj Total

HiO

(mole

per- cent Table Analysis

of

total gas)

1. Cymric field, Kern Co.,

Calif 12

13

15

15

16

2

7

11

17

12

2

6

6

1

2

3

7

8

9

12

14

2

6

7

3

12

13

1

2

3

4

5

6

7

2

5

7

810

16

3

5

2

3

4

5

7

60±

73±

20

Cold50±

17 Cold65±

95±

90± 80±

95±

95±

95±

98.6 97±

40±

70±

74.8

10055±

95±

150± 79± 90±

65±

65±

96.0

97.8

161 175± 14±

6.6 85±

75±

83±

70± 41± 64±

31±

10065±

2.10

6.0

.2

1.9 0.2

.5

.0

.2

84.24

95.10

89.20

97.7

80.1 93.8

81.7

3.50

82.73

97.0 80.3

93.43

91.31

94.0

86.3

63.60

93.06

97.40

98.90

77.9

85.8

»66.02

98.3

98.06

89.1

98.6

98.80

89.34 90.6

97.90

93.0

35.4

.59 6.7

1.0

.3

0.0

.0

.00

79.63 85.6

93.9

95.2

99.8

96.5

81.6

66.9

.49

.10

.55 <.03

.4.14

.6

2.07

.11

2.6

18.27

1.0 100.00

100.00

100.00

100.00 100.0

100.02

100.0 99.9

99. 9959

100. 00

100.00

100.15

100.0

100.0

100.0

100.00

100.00

100.0

100.0

100.00

100.00

100.0

100.0

100.10

99.95

100.00

100.1

100.0

100.25

91.00(7)

100.0

99.997

99.7

100.0 100.02

100.00

100.02

100.00

100.0

100.0

100.00

100.1 100.0

100.0

2. Hajduszoboszlo, Hungary.

3. South Kwanto fields, Chiba Prefecture, Japan.

4. Raisin City field, Fresno County, Calif

0.7

.7

1.4

.0

17.7

15.2

.0

.0

'2.9 15.7

32.6

14.74 4.15

16.55

1.6

'17.0 4.1

112.3

> 94. 43

1.65 1.4 16.3

15.83

12.10 4.5

11.9 3.53

6.38 U.60

U.OO

1.9

'6.2

»0.19

11.5

1.89

3.0 1.40

1.90

'2.49 U.8

•1.65

6.0

'45.1 85.50

193.3

88.65

97.1

1.5

.0 0.05. Bad Hall, Austria 0.0

6. Hanmer, S. Island, New

.12

7. Willow Creek, Shasta County, Calif -. 1.1.0

.0 1.6 Tr.

.52

.00

1.40

.2.3

.3

8. Tolsona Spring. Copper 0.0 0.1

.005

.1

.0009 River Basin, Alaska

10. Upper Basin, Yellowstone

17 .10

2.30

.03

.2.06

.1

.55

.00

.5 2.0

1.6

5.3

.00

8.36

11. Norris Basin, Yellowstone

12. Steamboat Springs,

.04 <.05

99.95

16. Pauzhetsk, Kamchatka,

USSR .—

-

17. Well 4/1, Wairakei, New

.39

.0

2.37 5.36 0.03 99.96

18. Niland, Imperial County,

Calif 18 .0 3.4

20. Nalachevskie, Kamchatka, USSR .

1.00

.00

.74

.00

.6

.0

15.29

.20

.20

.10

.0

7.6

24.33

.00

Tr. (7)

7

2.0

1.69

.55

.75

.10

20.1

.4

0) Present

i

.63

.3

.0

.0

.23

.02

.00

21. Ebeco Volcano, Kurile

Islands, USSR 19 .00

.00

.46

.25

.4

9.8

14.67

.45

.00

.00

.0

.1

.18

5.34 .00

.5

22. Frying Pan Lake, New

Zealan d

23. White Island, New Zea24. "The Geysers", Sonoma

County, Calif 20 1.28

.25

.05(7)

.00

1.1

(.14±) 98.06

25. Bumpass Hell, Tehama

0.7

26. Norris Basin, Yellowstone

27. Mud Volcano group, Yel- lowstone National Park, Wyo

28. Sulphur Springs, Sandoval

.024

.0 <.001

29. Uzonskie, Kamchatka,

USSR

30. Koshelevsk, Kamchatka, USSR

31. Steamboat Springs, Washoe County, Nev.

32. Well 6, Wairakei, New

21 .1

.2

.12

7.0

.0

.05 .06 .007 99.49

33. Essentuki, Caucasus, USSR 22 1.04 '.06

34. Malkinsk, Kamchatka,

USSR

35. Te Aroha, New Zealand . .02 .30

36. Sulphur Bank, Lake

23 7.94 6.6

.00

Present

37. Ngawha, New Zealand 1.0

.00

1.0

38. Mammoth, Yellowstone

25 .45

39. Lysuholl, Snaefellsnes,

40. Hot Springs, Garland

26 .0 19.5

13.91

41. Warm Springs, Meri0. 42. Svdri-Revkir, Iceland . 0.0 .0 <1 99.85

43. Plombiers, France . 8.90

.8

1.45

.2

.3

.0

44. Salado Fm., Lea County, N. Mex 27 1.4 .2 .0 .0

Includes inert gases not reported. » Includes HjS as well as COj.
CHEMICAL COMPOSITION OF SUBSURFACE WATERS F59

Table 29.

Approximate median ratios and contents, by weight, of analyses in tables 12 to 26, compared to ocean water

Table Number of analyses

Ca/Na Mg/Ca K/Na Li/Na •HCOj/Cl SCVC1 F/Cl Br/CI I/Cl B/Cl

Total

re- ported ppm

SiOi (ppm)

Total reported N as NH«

pH

0.038

.04

.3

.05

.2

.03 .06

.8

1.5

1.

.05

.04

.5

1..2

3.2

.4

.15

.5

.1

.06

.1.3

.4.2

.6

.5

.3.3

.2

0.036

.015 .02

.03

.05

.10 .13

.2

.4.4

.02

.03

.07

.15

.1

0. 00001

.0003

.0002

.0003

.0005

.006

.002

.01 .00

.005

.002

.001

.001

.001

0.0074

.02

.001

.2.03

.1.3.00

.00

50.

5.

2.

.3

.2

15.

0.14

.0005

.0008

.002

.005

.1.06

.7

400.

10.

.05

.4

.5

1.4

4.

0.00007

.0002 .00002

.0003 .00005

.002

.001

.01 .03

.0

.001

.006

.02

.01 .06

0.0034

.003 .005

.0015 .002

.0015

.003 .0006 .004

0.000003

.002 .00008

.002

.0001

.0000 .0006

.0000 .000

0.00024

.003 .0002

.015 .0005

.02

.01 .01 .3

.4

.1

.1

.002 .02

.1

34,500

30,000

120,000

20,000

20,000

2,000

10, 000

9,000

2,000 500

12,000

3,000

2,000

2,000 200

7

30

10

30

25

300

110 300

200

70

80

90

6060

60

0.05

40 200

40

7

1±

1±

6301±

5

201±

1

8.0

Oil-fleld brines: NaCltype 12

13

1516

1718

1920

21

22

23

2325

26

a

13

12

15

14

8

13

115

10

6

66

6

7 Na-Ca-Cl type 6.7 Springs that may contain connate

water: NaCl type. 7.8 Na-Ca-Cl type 7 1 Springs that may contain volcanic

water:

8 4

7 ? Acid S0«-C1 type 2.2 Acid SO< type 1 9 Acid HCO3-SO4 type 7 n Springs that may contain metamorphic water, NaHCO-boron type.. Miscellaneous waters: Springs associated with mercury deposits

.002

.002

.001 .003

.002

.003

.000

.000

6.8

7.0 Springs associated with manganese and tungsten deposits Springs depositing travertine... 6.8

6.6

9 ?.

' Includes COi as equivalent HCOj.

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CHEMICAL COMPOSITION OF SUBSURFACE WATERS F63

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F64 DATA OF GEOCHEMISTRY

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INDEX

A

Page

Acid-forming areas and mines, analyses of nonthermal, saline and acid waters from F12, 62 Alabama, analyses of subsurface water from: Birmingham. 22 Center Point 23

Iron dale 22 Linden 20 Sylacauga 25 Tuscumbia 22 Alaska, analyses of subsurface water from: Copper River Basin _ 38 Umnak Island 40

Algeria, analyses of subsurface water from Meskoutine Springs, Constantino Province 13,54 Alluvium, analyses of subsurface water from.

.

8, 28

Argentina, analyses of subsurface water from Neuquen Territory 32-33, 44 Arikaree Sandstone, analyses of ground water

from 18 Arizona, analyses of subsurface water from: Buell Park 16 Douglas 28 Gila Bend 29 Mesa 28 Mexican Water 18 Arkansas, analyses of subsurface water from: Garland County 55 Hot Springs 7,24 Melbourne 18 Monticello 20

Austria, analyses of subsurface water from

Linz 36

B

Baltimore Gneiss, analyses of ground water

from 26 Bangor Limestone, analyses of ground water

from 22 Bayport dolomitic Limestone, analyses of 2 ground water from 22 Benton Shale, analyses of ground water from.. 20 Bicarbonate ions, general discussion 3-4 Big Fork Chert, analyses of ground water

from 24 Biwabik Iron Formation, analyses of ground

water from 24

Brazil, analyses of subsurface water from

Itabira District, Minas Gerals.. 8, 12,26 Brevard Schist, analyses of ground water from. 26 Brines, analyses of. 32-33 British West Indies, analyses of subsurface water from St. Lucia Island 47 Brule Siltstone, analyses of ground water from. 20 Brunswick Shale, analyses of ground water from 20 Bushveld Sandstone, analyses of ground water from 18 Bushveld ultramaflcs, analyses of ground

water from 16

C

Face

Calcium in solution, general discussion F3-4

California, analyses of subsurface water from: Abbott Mine, Colusa County 60 Crabtree Springs, Lake County 12,48 Cymric oil field, Kern County 11,30 Fresno County 29,30,32,34,36 Imperial County 42 Keene Wonder Springs, Inyo County 13, 54 Lassen County 50 Mendocino County 48 Midway Sunset oil field, Kern County... 34 Mono County 42 Morgan Springs, Tehama County 12,40 Napa County 50 Nipton 26 San Bernardino County 58 Santa Clara County 48

Searles Lake, Inyo County 13,56 Shasta County 38,46 Siskiyou County 66-57 Solano County... 30,36 Sonoma County 11,46,47 Sulfur Bank mine, Lake County 12, 50 Trinity County 48 Tuscan Springs, Tehama County 36 Ventura County 32 Wilber Springs, Colusa County 11,36 Camillus Shale, analyses of ground water from 20 Canada, analyses of subsurface water from

Alberta 34 Carbonate ions, general discussion 3-4 Caseyvilie Sandstone, analyses of ground

water from 18 Castile Formation, analyses of ground water

from gypsum 24

Castle Hayne Limestone, analyses of ground

water from 22 Catahoula Sandstone, analyses of ground

water from 18 Chicopee Shale, analyses of ground water

from 20

Classification of subsurface waters 1-2 Cockeysville Marble, analyses of ground

water from 25 Colorado, analyses of subsurface water from: Doughty Springs, Delta County 13, 50-51 Fort Morgan 29

Garfield County 66 Monument 18 Ouray County 50-51 Poncha Springs, Chaffee County 13,50-51 San Juan County 63 Columbia River Basalt, analyses of ground

water from 16 Conasauga Limestone, analyses of ground

water from 22 Connate waters 2,9-10 Connecticut, analyses of subsurface water

from: Manchester 18 Willimantic 26 Copper Ridge Dolomite, analyses of ground

water from 23

Page

Crater lakes. See Springs. Czechoslovakia, analyses of subsurface water

from Breclav FJfl

Dakota Sandstone, fluoride content of water

from 6 Dawson Arkose, analyses of ground water from 18 Deccan Basait, analyses of ground water from. 10 Deep-well brines. See Oil and gas fields.

E

Ecca Shale, analyses of ground water from. . 20 Edwards Limestone, analyses of ground water

from 22 Epithermal mineral deposits, analyses of thermal waters associated with...

11-12, 50-61 EutawClay, analyses of ground water from... 20

Florida, analyses of subsurface water from:

Brooksville 22

Gainesville 22 Lake City 22 Fort Union Formation, analyses of ground

water from lignite.. 24

Fossil water 9 France, analyses of subsurface water from

Plombiers 65 Franconia Sandstone, analyses of ground

water from 18

G

Gasconade Dolomite, analyses of ground

water from 23 Gases accompanying or related to subsurface

waters, analyses of 68-59 Gas fields. See Oil and gas fields. Georgia, analyses of subsurface water from: Meriwether County 55 Suwanee 26

Glacial outwash, analyses of subsurface water

from 8, 28 Gravel, unconsolidated, analyses of subsurface water from 8,28 Greece, analyses of subsurface water from Thermopotamos, Euboea Island.. 10, 38 Grenville Gneiss, analyses of ground water

from 26 Guelph Dolomite, analyses of ground water

from 22 H

Hattiesburg Clay, analyses of ground water from 20 Hawaii, analyses of subsurface water from Oahu Island— 16 F65
F66 INDEX

Paga

Homewood Sandstone, analyses of ground

water from F18 Hungary, analyses of subsurface water from: Budapest #

13, 30, 56-57 Bukkszek 34 Debrecen 30 Mezokovesd 34

I

Iceland, analyses of subsurface water from: Akureyri area 65 Lysuholl Springs, Snaefellsnes Peninsula. 12, 54 Reykjanes, Reykjavik 10,40-41 West-central _. 40-41 Idaho, analyses of subsurface water from: Bear 17 Bruneau 28 Clayton 14 Eden - 16 Grandview 14 Shoshone 16 Valley County 60 Igneous rocks, analyses of ground water from. 5-6, 14-17

Illinois, analyses of subsurface water from Wayne County.. 32

India, analyses of subsurface water from Puma, Hyderabad 16 Indonesia, analyses of subsurface water from

Java 12, 13, 44 Ions in ground water, general discussion 4 Iowa, analyses of subsurface water from: Clinton 28 Malcolm 29 Iron in solution, general discussion 3

Israel, analyses of subsurface water from near Sea of Tiberias 10, 38-39

Italy, analyses of subsurface water from

Naples 42

J

Jackson Shale, analyses of ground water from. 20 Japan, analyses of subsurface water from: Arima, Hyogo Prefecture 10,38 Chiba Prefecture 30 Fukushima Prefecture 55 Gumma Prefecture 36,44 Hokkaido Prefecture. 36,48-49,50-51 Iburi Prefecture.. 44 Kanagawa Prefecture 46 Kogoshima Prefecture 47 Niigata Prefecture 44 Tochigi Prefecture 46,53 Yamagata Prefecture. 38-39 K

Kansas, analyses of subsurface water from: Gaylord 28 Lyon County 20 Kentucky, analyses of subsurface water from: Bardstown 22 Dawson Springs.. 18 Johnson County 32 Park Lake 20 L

Lakebeds, analyses of subsurface water from.. 28 Laurel Limestone, analyses of ground water from 22 Lebanon Limestone, analyses of ground water from 22 Louisiana, analyses of subsurface water from: Lafourche Parish 30 Plaquemines Parish 32 M

Magmatic waters 2, 10-11 Magnesium in solution, general discussion 4

Page

Maine, analyses of subsurface water from

Vassalboro F26

Marble, analyses of ground waters from 25 Maryland, analyses of subsurface water from: Arcadia 26 Baltimore County 25,26 Clear Spring 28

Ellicott City 14 Lake Roland 16 Laurel 16 Waterloo 16 Massachusetts, analyses of subsurface water

from: Chicopee . 20 New Bedford 14 Meagher Limestone, analyses of ground water from 22 Metamorphic rocks, analyses of ground water from 8, 25-27 Metamorphic waters 2,11 Mexico, analyses of subsurface water from: Baja California 42 Sonora 53 Michigan, analyses of subsurface water from: Carleton 18

Cliffs Shaft Mine 25 Grand Rapids.. 22 Houghton County 62 Marquette County 52 Michigan Basin 9,32-33 Morris Mine 26 Mines and acid-forming areas, analyses of nonthermal, saline and acid waters from 12, 52 Minnesota, analyses of subsurface water from: Eden Valley.... 28 Grand Rapids 24 Mound 18 Mississippi, analyses of subsurface water from:

Collins 18 Prentiss 20 Missouri, analyses of subsurface water from

Alley 23 Montana, analyses of subsurface water from: Bow County 63 Ennis 22 Garrison 24 Mutual Quartzite, analyses of ground water from 25 N

Navajo Sandstone, analyses of ground water from 18 Nebraska, analyses of subsurface water from: Crawford... 18 Harrisburg 20 Nevada, analyses of subsurface water from: Beatty... 14 Bowers, Washoe County.. 55 Eureka County 40 Nye County 50-51,52 Pershing County 50 Pigeon Spring, west of Lida 28 "Poison" spring, Washoe County 63 Steamboat Springs, Washoe County... 11,12,40 Steamboat well GS-7, Washoe County... 47 Storey County 52 New Hampshire, analyses of subsurface water

from Plymouth 28 New Jersey, analyses of subsurface water from Wyckofl 20 New Mexico, analyses of subsurface water

from: Eddy County 56-57 Lea County 56-57 Los Alamos 14 Ojo Caliente Springs, Taos County 13, 50-51 Red Bluff 24 Roswell 22 Sandoval County 42,46

Page New York, analyses of subsurface water from: Bloomlngdale . F28 Lake Pleasant 17 Sand Lake 18 Saratoga County 38 Syracuse 20 Wayne County 66-67 New Zealand, analyses of subsurface water

from: Aroha 28 Bay of Plenty 44 Ngawha Springs, North Island 12, 60 North Island 40-41,47,48-49 South Island 36 Tarawera region 44 Tongariro Volcano 48 Niagara Dolomite, analyses of ground water

from 23 North Carolina, analyses of subsurface water

from: Asheboro 17 China Grove 17 Harrisburg 16 Mebane 14 New Bern 22 Pekin 20 Webster 16 Wilkesboro 26 Yanceyville .. 26 North Dakota, analyses of subsurface water

from:

Belfleld 24 Langdon 20

O

Oakville Sandstone, analyses of ground water

from 18 Ocala Limestone, analyses of ground water

from 22 Ohio, analyses of subsurface water from: Bainbridge 23 Columbus 28 Cuyahoga County 20 Fort Recovery.. 7,23 Ohio Shale, analyses of ground water from 20

Oil and gas fields, analyses of subsurface water

from: General discussion 9 Sodium chloride dominated 30-31 Sodium and calcium chlorides, high in 32-33

Sulfate and bicarbonate, high in 34-35 Oklahoma, analyses of subsurface water from Enid 28 Oregon, analyses of subsurface water from: Burns 14 Cave Junction 28 Farmington 16 London, Lane County 10,38 Sheaville 20

Pahasapa Limestone, analyses of ground water

from 22 Peebles Dolomite, analyses of ground water

from 23 Pennsylvania, analyses of subsurface water

from: Bucks County . 25,26 Jamestown 18 Nottingham 16 Worthington ._._ 18 pH, general discussion 3-4 Phosphorla Phosphate, analyses of ground

water from 24

Pierre Shale, analyses of ground water from.. 20

Philippine Islands, analyses of subsurface water from Luzon 44
INDEX F67

Pooono Sandstone, analyses of ground water from F18

Poland, analyses of subsurface water from: Boryslaw area — - 32-33

Qallcla 30 Pomiarkach - - 30 Port Deposit Gneiss, analyses of ground water

from 26

Pretoria Quartzite, analyses of ground water

from 25 Q

Quartzite, analyses of ground waters from.... 25 R

Rensselaer Oraywacke, analyses of ground

water from 18 Rhode Island, analyses of subsurface water

from West Warwick M

Rumania, analyses of subsurface water from: Haromszek County 48 Molnestl 30

8

St. Peter Sandstone, analyses of ground water

from - 18 Salado Formation, analyses of water from salt deposits of 13,66

Salt deposits: Analyses of subsurface water associated with 13, 56-67 Waters of 13 San Andres Limestone, analyses of ground

water from 22

Sand, unconsolidated, analyses of subsurface water from 8,28 Sedimentary rocks, analyses of ground water from 6-8, 18-24 Siamo Slate, analyses of ground water from 26

Silica In solution, general discussion 3

Sioux Quartzite, analyses of ground water

from 25 Snake River Basalt, analyses of ground water

from 16

Soil, chemical character of ground water af- fected by 2 South Carolina, analyses of subsurface water

from: Georgetown 20 McCormlck County... 14 South Dakota, analyses of subsurface water

from: Lawrence County 62 Rapid City 22 Sioux Falls 25

Page

Springs, analyses of water from: Acid sulfate associated with volcanlsm.. Fll, 46-47 Acid sulfate-chloride In volcanic environ- ments and crater lakes 10-11, 44-45 Composition similar to oil-field water,

general discussion 0-10 Sodium, bicarbonate and boron, high

In 11, 48-49 Sodium calcium chloride type 38-39 Sodium chloride type 36-37 Travertine depositing 12-13,64 See also Thermal waters. Stormberg Basalt, analyses of ground water

from 16 Sweden, analyses of subsurface water from

Scania district 32-33 Sylacauga Marble, analyses of ground water

from 25 Sylvania Sandstone, analyses of ground water from 18 T

Tabulated data, source and selection 4-6 Taiwan, analyses of subsurface water from

Taipei 10,12,42,44,60-51 Tennessee, analyses of subsurface water from Mt. Juliet 22 Terminology and units, discussion 6 Texas, analyses of subsurface water from: Kennedy 18 Pecos 29 Uvalde 22 Thermal waters, analyses of: Associated with epithermal mineral deposits 11-12 Associated with quicksilver deposits 11 Bicarbonate sulfate In volcanic environ- ments 11,47 Epithermal mineral deposits 60-51 Geyser areas associated with volcanism. 10, 40-41 Meteoric 13,55 Sodium chloride bicarbonate type associ- ated with volcanlsm 10,42-43 See also Springs. Tunisia, analyses of subsurface water from Aln

Djebel, Tunis 13,38-39 Turkey, analyses of subsurface water from

Anatolia 38-39 U

Union of South Africa, analyses of subsurface water from: Barberton 16 Cape Province 20,60-51

Irene, Pretoria, Transvaal 23 Monzi, Zululand 18 Paddysland, Transvaal 26

Pretoria district 16, 18 Stellenbosch 14 Transvaal 14, 18, 20, 25 Trompsberg, Orange Free State 10,38

Page

U.S.S.R., analyses of subsurface water from: Abkhai F38-39 Caucasus . 48-49 Crimea 36, 48-49 Kamchatka 40-41,42,46,48-49 Kazakh district 30 Kunashlr Island 44,46 Molotov City 32-33 Neshkin, Siberia 10,38 Paramushir Island 44 Units and terminology, discussion 6 Utah, analyses of subsurface water from: Abraham Springs, Juab County 13,50 Box Elder County 36 Kamus 25 Roosevelt Springs, Beaver County 12,42 Tooele County 66 Weber County 38

Vernon Shale, analyses of ground water from.. 20

Virginia, analyses of subsurface water from

Chester 14 Virgin Islands, analyses of subsurface water from St. Croix Island 29 Volcanlsm, analyses of waters associated with.

See Springs and Thermal waters. W

Warsaw Limestone, analyses of ground water from - 22 Washington, analyses of subsurface water from: Camas 16 Moses Lake - 16 Spokane ... 14 Tonasket 26 Vancouver 28 West Germany, analyses of subsurface water

from: Ruhr district 32-33 Westphalia 36 Wiesbaden, Mainz 10,38 West Virginia, analyses of subsurface water from Calhoun County 32

Willard Shale, analyses of ground water from.. 20 Willimantic Gneiss, analyses of ground water from 26 Wisconsin, analyses of subsurface water from: Kaukauna 18 Waukesha 18 West Allis 23 Wissahickon Schist, analyses of ground water from 26 Wyoming, analyses of subsurface water from: Fremont County 34 Hot Springs County 54 La Prele 20 Natrona County 34 Sweetwater County 56 Yellowstone National Park 40,44,46,54







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