Structural Geology and Geothermal Investigation of the White Sulphur Springs Area, Montana

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Master's Theses Graduate College

4-1987

William G. Gierke

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Recommended Citation Gierke, William G., "Structural Geology and Geothermal Investigation of the White Sulphur Springs Area, Montana" (1987). Master's Theses. 1217. https://scholarworks.wmich.edu/masters_theses/1217

This Masters Thesis-Open Access is brought to you for free and open access by the Graduate College at ScholarWorks at WMU. It has been accepted for inclusion in Master's Theses by an authorized administrator of ScholarWorks at WMU. For more information, please contact [email protected]. STRUCTURAL GEOLOGY AND GEOTHERMAL INVESTIGATION OF THE WHITE SULPHUR SPRINGS AREA, MONTANA

William G. Gierke

A Thesis Submitted to the Faculty of The Graduate College in partial fulfillment of the requirements for the Degree of Master of Science Department of Geology

Western Michigan University Kalamazoo, Michigan April 1987

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. STRUCTURAL GEOLOGY AMD GEOTHERMAL INVESTIGATION OF THE WHITE SULPHUR SPRINGS AREA, MONTANA

William G. Gierke, M.S.

Western Michigan University, 1987

Sevier thrusting in the White Sulphur Springs area was

associated with le ft-la te ra l movement along the Lewis and Clark

lin e . During Middle Miocene time, the Lewis and Clark line

exhibited right-lateral movement, forming extensional features

that either truncated Sevier structures or followed preexisting

Sevier zones of weakness.

The Smith River Valley is a pull-apart basin that is filled

with Tertiary volcanic ash and clay-rich sediments that are

thermally nonconductive relative to surrounding rocks.

Hydrothermal activity in the area is associated with a

structurally controlled circulation system accompanied by a high

thermal gradient. Thermal discharge is constrained along the

north-trending White Sulphur Springs normal fa u lt. Calculated

reservoir temperatures ranging from 52° C (Na-K-Ca-Mg) to 99° C

(Quartz) indicates that variable degrees of mixing occur. The

estimated reservoir temperature (72° C ± 10° C) lim its thermal

development in the area to space heating and recreational use.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ACKNOWLEDGEMENTS

I would like to acknowledge the following people who provided

assistance during the formulation of this thesis. Foremost thanks

go to Dr. John Sonderegger of the Montana Bureau of Mines and Geology

(MBMG) for providing this thesis topic, field assistance, necessary

literature, constructive criticism, and pleasant hospitality. I am

obliged to the MBMG for financial support and analyses of water

samples; Michael Stickney (MBMG) for contributing his gravity data

and interpretations of the White Sulphur Springs area; John Gogas

(Montana College of Mineral Science and Technology) for supplying

his gravity maps, models, and interpretations of the area; S. L.

Groff (MBMG, retired) for sharing his knowledge of the area studied;

and Mitchell Reynolds (USGS) for his structural advice and geologic

contributions of the area.

Special gratitude is given to my committee chairman Christopher

J. Schmidt (Western Michigan University) for his assistance in the

fie ld and direction throughout this project; Western Michigan Univer

sity professors Dr. W. Thomas Straw, Dr. William Sauck, Dr. John

Grace, and Robert Havira fo r th e ir support and contributions; and

Mark Sheedlo (Western Michigan University) for his geologic advice

and moral support.

I would like to thank Frank Murphy, Howard Zehtner, Mr. Bodell,

Mr. and Mrs. Saunders, Bob Hanson, Ronald Jackson, and the people of

White Sulphur Springs for their hospitality and kindness. Thanks

i i

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. also to Sue Gibson for typing the thesis. Finally, I would like to

thank my wife Suzanne for her steadfast support, motivation, and

encouragement.

William G. Gierke

i i i

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Structural geology and geothermal investigation of the White Sulphur Springs area, Montana

Gierke, William Gordon, M.S.

Western Michigan University, 1987

UMI 300 N. Zeeb Rd. Ann Arbor, MI 48106

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Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. TABLE OF CONTENTS

ACKNOWLEDGEMENTS ...... i i

LIST OF TABLES ..... v iii

LIST OF FIGURES . ix

LIST OF PLATES ...... xi

CHAPTER

I. INTRODUCTION ...... 1

Location and Description ...... 1

Objective and Procedures ...... 1

Previous and Related Works . . . 3

I I . GEOLOGIC SETTING ...... 7

Regional Setting ■.'...... 7

Local Stratigraphy ..... 11

Introduction ...... 11

Precambrian Belt Supergroup ...... 13

Paleozoic Strata ...... 14

Mesozoic Strata ...... 1 5

Tertiary Sediments ...... 16

Lower Miocene Fort Logan Formation ...... 17

Upper Miocene Deep River Formation ...... 18

Quaternary A llu v iu m ...... 19

Igneous A ctivity ...... 20

Castle Mountain Stock and Related Volcanics . . . 20

Basaltic Volcanism ...... 22

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Table of Contents—Continued

CHAPTER

I I I . STRUCTURAL GEOLOGY ...... 24

Precambrian Features ...... 24

Belt Basin ...... 24

Lewis and Clark L in e...... 25

Fold and Thrust Belt Tectonic Setting ...... 27

Description of Thrust Faulting ...... 30

Moors Mountain Thrust Z o n e...... 30

Minor Faults ...... 38

Pinchout Creek Thrust ...... 41

Mission Canyon Fault ...... 42

Fourmile Creek Thrust ...... 42

Horse Butte Thrust Zone...... 43

Minor F a u lts...... 45

Description of Folding ...... 45

Willow Creek Syncline ...... 45

Cottonwood Creek Syncline and Associated Folds ...... 46

Post-Fold and Thrust Belt Deformation in the White Sulphur Springs Area ...... 48

Regional Setting and History ...... 48

Description of Faulting ...... 54

White Sulphur Springs Basin-Bounding Fault System ...... 55

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Table of Contents—Continued

CHAPTER

IV. RECONNAISSANCE GRAVITY SURVEY ...... 58

Objective ...... 58

Data Acquisition and Processing ...... 58

Interpretation of the Bouguer Anomaly Map ...... 59

V. HYDROGEOLOGY ...... 62

General Statement ...... 62

D ra in a g e...... 62

Aquifers ...... 63

Ground Water Hydrology ...... 65

VI. GEOCHEMICAL SURVEY ...... 67

Objectives and Procedures ...... 6 7

Water Chemistry ...... 68

Geochemical Thermometers ...... 73

V II. WHITE SULPHUR SPRINGS HYDROTHERMAL SYSTEM ...... 79

General Statement ...... 79

Thermal Gradient and Heat Source ...... 79

Circulation System ...... 82

Controls on Recharge-Discharge ...... 84

V III. THERMAL DEVELOPMENT ...... 88

Present Development ...... 88

Potential for Development ...... 88

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Table of Contents—Continued

CHAPTER

IX. SUMMARY AND SYNTHESIS ...... 92

Tectonic H isto ry ...... 92

Hydrothermal ...... 94 APPENDICES ...... 95

A. Conversion Factors for Units Used in This Paper .... 96

B. Stereographic Analyses of Folds ...... 98

C. Gravity Data ...... 104

D. Stratigraphic Profiles ...... 108

E. Chemical Analyses of Well Waters...... I l l

BIBLIOGRAPHY...... • • • • ...... I 42

v ii

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. LIST OF TABLES

1. Chemical Analyses of Ground Water From Wells in the White Sulphur Springs Area, Montana ...... 69

2. Calculated Reservoir Temperatures and Analytical Data for Thermal Well Waters in White Sulphur Springs (W .S.S.), Montana ...... 74

v iii

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. LIST OF FIGURES

1. Index map and general geographic setting of the White Sulphur Springs area ...... 2

2. Structural provinces and regions of western Montana . . . 8

3. Locations of basins and ranges in western Montana and southeastern Idaho ...... 10

4. General stratigraphy of the White Sulphur Springs area, Montana ...... 12

5. Photograph showing the low-angle unconformable contact between the Precambrian Spokane Shale and the overlying Cambrian Flathead Sandstone ...... 15

6. General tectonic map showing the relationship between the Belt Basin, the Lahood Formation, and Late Precambrian f a u l t s ...... 26

7. A - Photograph of the Moors Mountain thrust zone and Pennsylvanian Quadrant klippens northeast of White Sulphur Springs; B - Sketch of structural features in the photograph . 32

8. A - Sketch showing a change in slip movement which may be associated with convex-eastward thrust faults in west-central Montana; B - Sketch illustrating dilation or extensional features that would be expected i f predominant dip-slip movement occurred along the length of a thrust that had an arcuate trace ...... 34

9. Diagrammatic sketch showing the outline of the Helena structural salient and inferred oblique slip ...... 35

10. Diagrammatic sketches which illu s tra te that variations in the observed deformation of allochthonous thrust plates may be related to different erosional levels ...... 3 7

11. Diagrammatic sketch of the sequence of faulting in the White Sulphur Springs area ...... 38

12. Sketch showing the relationship of folding to thrusting along the Horse Butte thrust zone ...... 48

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. List of Figures—Continued

13. Generalized block diagrams illu s tra tin g the possible relationship between preexisting Laramide zones of weakness and Cenozoic basin-range extensional features at the eastern margin of the Lewis and Clark line 50

14. Schematic diagram showing A) Laramide fa u lt geometry, B) extensional post-Laramide reverse drag forming a lis tr ic normal fa u lt, and C) deposition and downwarping of post-Middle Miocene sediments ...... 52

15. Generalized block diagram showing the possible relationship between Laramide thrust faulting and post-Laramide normal faulting in the Smith River Valley ...... • • ...... 53

16. Graph for estimating magnesium correction temperature to be subtracted from the Na-K-Ca calculated reservoi r temperature...... 77

17. Generalized diagrammatic sketch of the White Sulphur Springs hydrothermal circulation system ...... 8 3

18. Photograph of solution breccia in the upper member of the Mission Canyon Limestone ...... 85

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. LIST OF PLATES

1. Geologic Map of the White Sulphur Springs Area, Montana

2. Geologic Cross Sections of the White Sulphur Springs Area, Montana

3. Relative Bouguer Anomaly Map, White Sulphur Springs, Montana

4. Water Table Map, White Sulphur Springs, Montana

5. Isothermal Contour Map, White Sulphur Springs, Montana

6. Isoconcentration Map, Fluoride, White Sulphur Springs, Montana

7. Isoconcentration Map, Specific Conductance, White Sulphur Springs, Montana

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER I

INTRODUCTION

Location and Description

The White Sulphur Springs area is located in west-central Montana

east of the Big Belt Mountains, northwest of the Castle Mountains, and

south of the L ittle Belt Mountains (Figure 1). U.S. Geological Survey

quadrangle maps that encompass the map area include the White Sulphur

Springs, Willow Creek, Manger Park, and the Catlin Springs Quadrangle.

The study area encompasses approximately 103 square miles and extends

from 110° 46' 45" to 110° 56' 52" W latitude and from 46° 24' 23" to

46° 37' 19" N longitude.

The hot spring, for which the town is named, is located near the

intersection of U.S. Route 12-89 and Main street about seventy feet

southeast of the Spa Motel. To the north and across the street from

the Spa Motel is the thermal bank well (Plate 1).

Objective and Procedures

This study is part of an investigation by the Montana Bureau of

Mines and Geology to determine the potential for thermal development

in the vic in ity of White Sulphur Springs. To assess the thermal

potential of an area, the characteristics of the hydrothermal system

must be identified. These features include the geologic controls on

recharge-discharge patterns, geochemistry, hydrogeology, reservoir

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 1. Index map and general geographic setting of the White Sulphur Springs area.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. characteristics, and the heat source of the thermal system. Field

work in the area was designed to use various disciplines of geology

in order to understand the system and its potential for development.

Field work was done in the White Sulphur Springs area during

the summers of 1981 and 1982. Work accomplished the fir s t season

included detailed geologic mapping north and east of town, a well

water inventory, static-water level measurements, and a water sampling

program. In the second fie ld season the following fie ld work was

done: reconnaissance gravity survey of the Smith River Valley,

detailed geologic mapping south of town, and completion of the water

sampling program with well waters from the Castle Mountain Lumber

Company and the home of Ralph Jordon.

Geologic mapping was done on 1:20,000 twelve by twelve inch

black and white aerial photos, and then transferred to 1:24,000 U.S.

Geological Survey quadrangle maps. Existing geologic maps that were

used included thesis maps by Dahl (1971) and Phelps (1969), and a

reconnaissance map by Groff (1965). Sampling procedures and data

acquisition for the water sampling program and gravity survey w ill be

discussed in their designated chapters.

Previous and Related Works

Previous research on the origin and controls of thermal waters

in the White Sulphur Springs area has been very lim ited; however,

other types of geologic work, including mapping, stratigraphic in ter

pretation, and petrology have been conducted in the area. Geologic

work in the area was f ir s t done by Grinnell and Dana (1876), who

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. primarily studied Tertiary deposits in the Smith River Valley. The

f ir s t geologic report of the Castle Mountain mining d is tric t was made

by Weed and Pirsson (1896) and included lithology, petrology, and

general geology of the area. Proterozoic Belt Supergroup rocks in

the area were la te r named and described by Walcott (1899). Koerner

(1939) mapped Tertiary deposits in detail and older rocks in a more

general manner along the western margin of the Smith River Valley.

The fir s t geologic map that included stratigraphic and structural

detail of the area was done by Tanner (1949). Pardee (1950) b rie fly

discussed the Smith River Valley in a paper in which he attributed

the origin of the basin to the effects of crustal downwarping. A

paper by Wolfe (1964) discussed the geomorphic history of the Smith

River Valley. The paper related Late Cenozoic uplift of west-central

Montana to the formation of mountains and intermontane basins.

Winters (1965) published a report on the geology and ore deposits

of the Castle Mountain mining district. The district is located

approximately 4 miles southeast of White Sulphur Springs.

Groff (1965) conducted a reconnaissance geologic and hydrologic

study of Meagher County. The majority of his hydrologic study was

concentrated around the White Sulphur Springs area. Master's theses

in the area that were completed under the direction of S. L. Groff

include Phelps (1969), Birkholz (1967), and Dahl (1971). The detailed

map areas included within these theses are mainly north and west of

White Sulphur Springs.

The fir s t reservoir temperature and energy estimates of the

White Sulphur Springs hydrothermal system were made by Renner, White,

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. and Williams (1975). Chemical data used for their derivations were

obtained from the U.S. Geological Survey. Chemical analysis of ther

mal waters in White Sulphur Springs was done by Mariner, Presser, and

Evans (1976). Water that was analyzed consisted of the Brewers

spring (now Spa Motel w ell) area. A soil temperature survey was

la te r completed by Chadwick, Galloway, and Weinheimer (1977) in an

e ffo rt to determine the areal extent o f thermal influence. The study

was concentrated on the c ity block that includes the hospital and

Spa Motel. In 1978, the First National Bank of White Sulphur Springs

thermal well was d rille d . A geologic report by Dunn (1978) presented

hydrologic and lithologic data for the w ell. Pump tests, temperature

p rofiles, geophysical logs, and d rillin g evaluation of the bank well

was done by Stoker and Niemi (1978).

Reynolds (1979) was the firs t to identify the Smith River Valley

as a fault-bounded basin. He discussed the tectonic origin of the

valley and its relationship to thermal activity. A metallogenic map

showing the general geology of the White Sulpur Springs Quadrangle

was published by McClernan (1980). Woodward (1981) b rie fly discussed

the Scout Camp-Willow Creek (now Moors Mountain) thrust zone and its

relationship to the disturbed belt of west-central Montana.

Estimated reservoir temperatures and discharge values for the

Spa Motel and bank wells were b rie fly discussed on the Geothermal

Resources of Montana map (Sonderegger & Bergantino, 1981). A more

detailed discussion of thermal a c tiv ity in White Sulphur Springs was

done by Sonderegger and Schmidt (1981). A re s is tiv ity survey involv

ing Schlumberger soundings was done in 1981 by Montana Tech students

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. under the direction of Charles Wideman. The purpose of the survey

was to delineate areas of hydrothermal a ctivity and associated s tra ti-

graphic controls.

Gogas (1984) conducted a gravity survey of the Smith River Valley.

His paper includes interpretations regarding the structural geology

and geometry of the Smith River Valley based on gravity data and

two-dimensional modeling.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER I I

GEOLOGIC SETTING

Regional Setting

The White Sulphur Springs area is located at the margin of two

major structural provinces in west-central Montana: the Late

Cretaceous-Early Tertiary Montana disturbed belt and the Late Ceno-

zoic Basin and Range Province. The eastern end of a regional linear

structural element, the Lewis and Clark line or Montana lineament,

is also located in the area (Figure 2). With exception of the

Volcano Valley fault to the northeast, the Moors Mountain thrust in

the White Sulphur Springs area is the easternmost thrust exposed in

the Montana disturbed belt (Plate 1). The eastern margin of this

belt corresponds closely with the eastern lim it of Proterozoic Belt

Supergroup deposition and with the western margin of the stable

craton (for example, Harris 1957; Harrison, Griggs, & Wells, 1974;

Mudge, 1970; and others). The Helena structural salient is a pro

nounced eastward bulge in the disturbed belt (Figure 2). The convex

eastward geometry of the salient closely follows the Proterozoic

depositional margin of the Belt trough or Helena embayment (Harrison

et al., 1974). This embayment is bordered on the north and south by

Archean gneisses and schists. Thrusts involving Beltian and Phanero-

zoic rocks appear to have impinged on these bounding basement rocks,

accentuating the convex eastward shape of fold and thrust features in

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Ij4° 112° 110° "T" ' T T

Canada Unltad Statu

ROCKY MOUNTAIN FORELAND PROVINCE

BASIN AND RANGE PROVINCE H.l.na Study Area

•Pi? A/#,?

Wyoming

100 MILES Tertiary and Cretaceous 100 Km Intrusive rocks Eastern limit of Eastern limit of '*1 Pre Belt (Archean) fold-and-thrust Basin-Range metamorphic rocks belt deformation faulting

Figure 2. Structural provinces and regions of western Montana (modified from Schmidt & Hendrix, 1981).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. the Helena salient. West of the craton's margin, Paleozoic and

Mesozoic sediments comprise the Cordilleran miogeocline.

Basins and ranges in Montana are considered to be a northern

continuation of extensional tectonism of the Great Basin region of

Nevada, western Utah, and southeastern Idaho (Chadwick, 1981;

Reynolds, 1979). The normal fa u lt from which the White Sulphur

thermal spring discharges occurs at the northeastern lim it of basin

and range faulting mapped in west-central Montana (Figure 3; Reynolds,

1979). The Smith River Valley may be a graben bounded by faults

associated with extensional features south of the Lewis and Clark

line (Reynolds, 1977, 1979). The range front fa u lt along the eastern

margin of the Smith River basin (Figure 3) corresponds with the

eastern extension of the Lewis and Clark line (Reynolds, 1979).

The Smith River Valley is bounded by the Big Belt Mountains to

the west, the Little Belt Mountains to the north-northeast, and the

Castle Mountains to the east (Figure 1). The Big Belt Mountains form

a broad, northwest-trending, doubly plunging arch. The Big Belt

Mountains are probably a culmination of folded thrust faults that are

mainly developed in Belt Supergroup rocks; however, in many portions

of the arch, Beltian strata have been thrust over Paleozoic rocks

(Lageson, Dresser, Schmidt, & Welker, 1982). Many thrusts in the

northern Big Belt Mountains are intensely folded (Shaffer, 1971;

Woodward, 1981) making regional correlation of thrusts d ifficult. On

the southwestern flank of the arch a northwest-trending escarpment

consisting of Beltian and younger sedimentary rocks are folded and

thrusted (Lageson et al., 1982). Rocks as old as Chamberlain Shale

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 10

LITTLE XlncoTn'xtj^ BELT MOUNTAINS

‘'Sulphur

^THREE -ii ^ i^pftlr-FORKSV^A % X .'S vW xp

MONTANA J Wyoming I YELLOWSTONE I PLATEAU

Figure 3. Locations of basins and ranges in western Montana and southeastern Idaho. (From Reynolds, 1979).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (Figure 4) may crop out near the center of the Big Belt Mountains

indicating a thick Belt Supergroup sequence in the area (Reynolds,

personal communication, 1982). Northeast of White Sulphur Springs

the L ittle Belt Mountains form a broad east-west-trending arch

(Figure 1). The L ittle Belt u p lift exposes Belt Supergroup and

Paleozoic rocks which are cored with Archean gneisses and schists

that have been intruded by Tertiary plutons. Southeast of the Smith

River Valley, the Early Miocene Castle Mountain stock truncates

Paleocene (Laramide) folds and thrusts.

Local Stratigraphy

Introduction

Because the primary objective of this thesis is to define the

geothermal potential and structural geology of the area, only a brief

description of stratigraphy w ill be presented here. Detailed s tra ti-

graphic descriptions of the area were given by Birkholz (1967),

Hruska (1967), Phelps (1969), and Dahl (1971), and on U.S. Geological

Survey maps of the Ringling and Black Butte Quadrangles (McGrew,

1977a, 1977b). Detailed stratigraphic depositional and paleostruc-

tural history of rocks in the area were presented by Sloss (1950);

Ross, Skipp, and Rezak (1963); McMannis (1965); Harrison (1972);

Harrison et a l. (1974); Suttner, Schwartz, and James (1981); and

Peterson (1981).

Sedimentary rocks exposed in the White Sulphur Springs area

range in age from Late Precambrian to Late Tertiary (Figure 4).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. GENERAL STRATIGRAPHY OF THE WHITE SULPHUR SPRINGS AREA , MONTANA i- QUATERNARY ALLUVIUM (Qal)t Gravel» sand, s ilt, end clay In the Smith River Valley at < QUATERNARY ALUUVUM ------e levat ions nonor.il ly lean than 5000 ft. 11524m). Gravel may he well sorted, 3 subrounded to rounded. o - LANDSLIDE DEPOSITS (Ols): Debris flows and colluvlum conslstino of poorly sorted clay LANDSLIDE DEPOSITS to houlder si 2 e material. locally found on the flanks of Castle Mountain.

lil TERTIARY SEDIMENTS UNDIVIDED (T a li FOPT LOGAN ANN DFKP RIVER FORMATIONS. Z TERTIARY Lower, Mtocene Fort Looan Formation - lloht tan-oranoe clay, sand, and con- UJ nlomeratic tuffaceous slltstones Interhedded with lloht oray volcanic -ash, lake o SEDIMENTS bed clays and channel connlomerates. o Upper Miocene Deep River Formation - Similar in composition to the Fort Lonan UNDIVIDED Formation with a oreater occurrence of channel deposits, lam er volcanic qlass >• 2 fraoments, more hornblende and plaaioclose. t r VOLCANO BUTTE VOLCANO BUTTE BASALTS ( T v b ) t h la c k b a s a lt w e a th e rin n o ra y in h -h ro w n j f i n e l y c r y s t a l < BASALTS lin e, occasionally vessictilar. H RHYOLITB PORPHYRY (Trp): Lloht-oray weatherinn to huff-tan with concentric red and QC RHYOUTE PORPHYRY oranae stains, fIne-orained rhyolite porphyry with sanidlne and nuartz U1 phenocryats (.25-0.5cm)• Locally found In the vicinity of the Castle Mountain I- n to c k . CASTLE MOUNTAIN CASTLB MOUNTAIN GRANITE AND SYENITE ( T c q ) : Fine to medium o ra ln e d o r a n it e and o r a n lt e porphycy dom1nanti other compositiona include diorite, oranodiorlte, monzoqite GRANITE AND SYENITE porphyry, and syenite porphyry.

ANDES1TB ( T a d ) : Dark o ra y is h -b ro w n fin e - o r a ln e d a n d e s lte . Locally found as sills ANDESITE th a t accompany f a u l t i n q . Not abundant in map a r e a .

CRETACEOUS - UNDIVIDED ( Xu) I HOWRY AND THERMOPOLIS SIIALESi FRONTIER FORMATION m p w r y . a n d tiikrmofolis - SHALE (Kmt)i Park-oray shale and siliceous mudstone. Interhedded oray to nreenish-oray, medium to coarse-orained sandstone in upper oc CRETACEOUS part? orayish-oranne ledoe-formina quartzite at base. Upper part mostly HI covered • (0 CL FRONTIER FORMATION (KF): Lioht-nray to yellowish and orecnlsh-nray, flne- 3 Q. UNDIVIDED to-coarse oralned sandstone* weathers dark-qray and brown with "salt and pepper" o 3 appearance. Xnterbodrieri dark-aray shale and siliceous mudstone, thin dark-oray UJ quartzite, dark-oray chert pebble connlomerate, siliceous limestone, and fossil o oyster banks. Sandstones and connlomerate beds oenerally form ridnes. Shales < and mudstone oenerally covered. 1“ KOOTENAI______FORMATION - I Kk) -. - I -Gray, red and nurnle mudstone mottled with white tines. UJ KOOTENAI Interbedded 1 iaht-oray sandstone, chert pebble conalomerate, and llnht-orav oc Freshwater oastropod bearinn limestone nodules in upper part. At base Is a oray, "salt and pepper” arkosic chert-rich fine-orained to con- o FORMATION uloirerat ic sandstone with some red and yellow iron-stain band inti. Upper part oenerally cowered, basal sandstone oenerally fort's a ridne. Thickness approxi mately 400 feet (122m) E UJ MORRRISON MORRISON FORMATION (J m )t L in h t- n r a y and y e ) lo w is h -o r a n o e , c a lc a re o u s n u a rtz o s e OC CL locally crossbedded sandstone* weathers rusty-brown. Cray fresh water limestone 3 CL FORMATION beds and nodules in upper part. Red mudstone and niltstone contalnlna thin beds 3 of rusty-brown sandstone in lower part. Thickness 150-200 feet ( 46-film) Qu a d r a n t QUADRANT QUART2ITB (Pq)t White to tan ouartzites extremely resistant-ridae former. QUARTZITE Th ic kn e ss 5^ f e e t - ( 1 7m) . AMSDEN FORMATION (P a ) t L lo h t- o r a y , w e a th e rln a to w h ite , t h in to th ic k bedded d o lo - mite* Interbeds of pale-oraylsh-oranoe fine-orained nuartzitlc sandstone in AMSDEN FORMATION upper part. Ped sandstone, slltstone, mudstone, and shales Interbedded with arav limestone in lower part. Thickness 320-600 feet (98-lB3m)

TYLER SANDSTONE I P t l i Tan Fo ru g ty -h ro w n f i n e to medium o ra ln e d s an d s to n e . la rn e TYLER SANDSTONE seale crossbeddI no with local llmonitlc pebble cnnnlomerntes. ToFal thickness 45 f e e t 1 14m)

BIG SNOWY GROUP - UNDIVIDED iH b s li HEATH (u p p e r ), OTTEP (p id d le ) and KI PREY (lo w e r) FORMATIONS. BIG SNOWY GROUP HEATH-IUack limestone and interhedded shales locally disrupted by faultinn and OC intrusiues. FJonresistant-poorly exposed. UJ z CL OTTKP - nray Ish-areen and orav, shale with minor thin interbeds of oray lime < CL UNDIVIDED stone. Generally poorly exposed. 3 KIRREY - Ped sandstone - is not exposed in the area and may he absent. Total E estimated thickness of Rio Snowy Croup is 500-700 feet pwl52-213m) £L MISSION CANYON LIMESTONE (Mm): dray to Itaht-orav cherty massive llrestone. Red- CO MISSION CANYON slltstone f K11 eH cavernous zones, paleo karst limestone solution breccia beds CO LIMESTONE locally In upper part. Generally forms steep hillsides and cliffs. Thickness <0 500-800 feet (152-244m) CO LO D G F P O I F LODCEPOLE LIMESTONE (M l)> Gr Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. uuw..», , .-tiic iu jir I'oun y enpcmwii • KIRREY - Perl sandstone - is not exposed in the area and may he absent, T o ta l o. estimated thickness of Bio Snowy Group Is 500-700 feet Fwl52-213m) a MISSION CANYON LIMESTONE tM»>: c.rav to llnht-orav cherty wasalve lloestone. Reri- MISSION CANYON ------siltstone Filled cavernous rones, paleo karst limestone solution hreccia herls 55 locally In upper part. Generally forms steep hillsides and cliffs. Thickness co LIMESTONE 500-800 feet ( 152-244ie> co co LODGEPOLE LIMESTONE (M l): Gray to lioht-qray, thin to medium hedded limestone. Minor LODGEPOLE thin shale beds. Fossils abundant! locally chertv inodules). Thickness 500-700 LIMESTONE feet 1152-213m)

THREE PORKS FORMATION ( H D t ) : Y e llo w c a lc a re o u s s i l t s t o n e , o ra y lim e s to n e , and THREE FORKS dark-oray and qreon mudstone and shale. Formation is oenerally not exposed in FORMATION the area. Thickness 50-100 feet (*M5-30m) z oc < UJ JEFFERSON DOLOMITE ( D i l i R ro w n ish -q ray f e t i d d o lo m ite and in te rh e d d e d n ra y lim e s to n e . a. JEFFERSON Thick hedded to massive. Stromatolite heds locally common, fossi1iferous. z a . Thickness 400-500 feet (122-152m| o 3 DOLOMITE > RED LION AND HAYWOOD FORMATIONS je D d li Ped l.ion F o rm ation -Y e llo w and re d d ls h -o ra n a e UJ thin 5erided limestone - upper memheri dark hlack shale - lower member. Maywood a s i RED LION AND MAY Formation - Gray to off-white and reddish-nray dolomite with red siltstone and 2 oray to Greenish shale. Roth formations are nonresistant and rarely exposed. WOOD FORMATIONS Total thickness 50-100 feet (*»15-30m) UJ Q. PILGRIM LIMESTONE (6pl)i Lloht-brown to oray massive limestone or dolomltic lime- stonei Some orayish-oranoe and yellow mottlinns. Locally oolitic and O. PILGRIM LIMESTONE fossiliferous; flat-pebhle intraformational connlomerate common. Generally O forms steep ririaes or c liffs . Thickness 350-41S feet (107-l27m)

PARE SHALE (epa)i Dark oraylsh-green micaceous shalci sparse thin oray limestone PARK SHALE lenses.Contains abundant worm burrow and trail casts alona with occasional z fossil (i.e. trllohite) franments. Thickness 200-210 feet (61-fi4n) < MEAGHER LIMESTONE I6ah Gray, thin to medium hedded limestone with abundant tan to £ MEAGHER nrayish-oranoe mottllno. Occasional oolitic beds and Fossil fraaments. Reddlnn m LIMESTONE commonly has a defined crumpled appearance. Forms low rldnes. Thickness s 170-200 feet (52-71m) < WOLSEY SHALE 16x): olive orecn, brown, and purple, friable, micaceous shale inter- o bedded with ollve-to brownlsh-oray thin bedded and lenticular nlauconitic WOLSEY SHALE siltstone and fine-orained sandstone In the lower part. Abundant "worm-cast" markione. Ncnr“si«»-*nt-ferr* valleys - centrally puorly exposed. Thickness 150-200 feet F*46-6lm)

FLATHEAD SANDSTONE Cef)> I.ioht vellowish-nray, white, tan, to pink, fine to coarse FLATHEAD oralned, thfn to thlckbedded, locally crossheridert nuartzose sandstone and quartzite. Occasional bands of purple from iron staininq. locally, conolome- SANDSTONE rate in lower 20 feet. Very resistant - forms ridaes. Thickness 170-200 feet <52-61m)

SPOKANE SHALE ( p 6 a ) : Ped, Grayish-red and occasionally 1 Inht-nrayIsh-qreen shale* SPOKANE SHALE sparse thin oray to reddish oray limestone with occasional stromatolite heds? sparse oray to yellowish qray sandstone. Thickness 2,200-3,200 feet (671-976m)

z GREYSON SHALE ( p € q ) j Upper member { 1,400-1,500 ft. thick) - Gray to yellowish-oray < quartziteand sandstone. Interhedded oreenish-oray micaceous shale oray- £ ish-red shale, and thin to medium bedded nray limestone in upper part. GREYSON SHALE Lower memher ( 3,000-3,400 ft. thick) - Cray and oreenish nrav, brown to black, to thin bedded, fissile shale and siltlte. Minor calcareous slttntone, fine- s orained sandstone and quartzite. Total thickness 4,400-4,900 feet 1^915- < 1037m) o tu NEWLAND LIMF.STONE (p C n ): T h in to medium bedded impure m i c r i t i c lim e s to n e , d o lo m itic oc NEWLAND limestone, and calcareous siltstone. Typical color, bluish-black on fresh a. surface with huff weathered surface. Limestone may be interhedded with medium UJ LIMESTONE to coacse-nralnert calcareous nanristone that is medium to thick bedded and has m minor amounts of feldspar, pyroxene, and rock franments. Reds of sandstone often have ripple marks. No‘complete section exposed in the area. Thickness 2,000-3,500 feet F*610-10fi7m)

NOT TO SCALE MODIFIED FROM McGREW 1977a;1877b. FIGURE 4

DO Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. The total thickness of the section is approximately 15,220 ft

(4634 m), excluding Quaternary sediments; however, Belt Supergroup

strata and Paleozoic carbonates are the predominant rocks seen in

the outcrop.

An outcrop of Chamberlain Shale and possibly Neihart Quartzite

surrounds a pluton that cores Mt. Edith in the Big Belt Mountains

(Reynolds, personal communication, 1982). Exposures of these older

Belt Supergroup rocks (Plate 1) suggest that a thick Precambrian sec

tion exists below the Smith River Valley. Archean basement rocks are

not exposed in the area. The nearest exposure of Archean rocks is

about 27 mi (43 km) north of White Sulphur Springs, near the town of

Neihart.

Precambrian Belt Supergroup

Belt Supergroup rocks in the area have a total thickness of

approximately 9000 f t (2744 m) and consist of the Newland Limestone,

Greyson Shale, and Spokane Shale. The thickness of the Newland Lime

stone is not precisely known because its lower contact has not been

identified in the area. The Newland Limestone contains lenses of

siltstone and locally thick beds of sandstone. The Greyson Shale

conformably overlies the Newland Limestone. Its lithology ranges

from micaceous shale (lower unit) to thin-to-medium bedded sandstone

with interbeds of micaceous shale and irregular beds of dark gray

limestone (upper un it).

The contact between the Greyson Shale and the overlying Spokane

Shale is gradational. I t is generally placed just below the fir s t

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. thick reddish-purple shale layer which is the typical color of the

Spokane Shale. The unconformity between the Precambrian Spokane

Shale and Cambrian Flathead Sandstone is low-angle. A spectacular

exposure of this contact can be seen at the Newlan dam, about 6 mi

(9.3 km) north of White Sulphur Springs (Figure 5).

Harrison (1972) suggested that Belt strata were deposited in an

intracratonic shallow marine basin that began to form about 1500 Ma

ago; however, a nonmarine origin has been postulated for some of the

units near the basin's margin (Boyce, 1975). Zieg (1986) described

Belt strata of the Helena embayment as a complete transgressive-

regressive depositional sequence. Structural controls on Belt

deposition w ill be discussed in Chapter I I I .

Although low-grade metamorphism has made the Belt rocks dense

and hard, Belt strata have a mechanical behavior similar to that of

Paleozoic and Mesozoic carbonates and shales. Examples of this may

be found in the Pinchout Creek (Plate 1) thrust fa u lt just east of

White Sulphur Springs which juxtaposes Greyson Shale against other

Belt strata, and in the tig ht folding of Newland Limestone beds in

portions of the Moors Mountain thrust sheet (NE% sec. 5, T.9N., R .7E.).

Paleozoic Strata

More than 3800 ft (1170 m) of Paleozoic rocks (Figure 4) overlie

the Belt Supergroup in the study area. Paleozoic rocks are primarily

limestones and micacefous shales with sandstones, dolomite, and si 11-

stones. All of the Paleozoic rocks were formed from sediments

deposited in a shallow marine environment with the possible exception

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 15

Figure 5. Photograph showing the low-angle unconformable contact between the Precambrian Spokane Shale and the overlying Cambrian Flathead Sandstone (looking south from the New!an Dam).

of the Tyler Formation. Maughan (1984) suggested that the Tyler

Formation is a combination of fluvialacustrine, deltaic, and litto r a l

marine deposits. The Tyler Formation in this area consists of the

lower Stonehouse Canyon Member which was probably deposited in a

delta near shore or fluvialacustrine environment (Maughan, 1984).

Ordovician, Silurian, and Lower Devonian rocks are nonexistent

in this area as rocks of these ages are generally absent in western

Montana. As is common in much of the disturbed b e lt, Paleozoic rocks

in this region commonly form the footwall rocks of major thrust sheets.

Mesozoic Strata

Mesozoic sedimentary rocks (Figure 4) in the area are approxi

mately 1650 ft (500 m) thick and are mainly associated with the

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 16

Willow Creek and Cottonwood Creek synclines (Plate 1). Because Upper

Cretaceous rocks are only p a rtia lly exposed in the extreme southeast

corner of the map area, they were grouped into a single map unit.

Triassic rocks do not exist in the map area because the margin

of Triassic deposition was about 80 mi (128 km) south of White

Sulphur Springs (McMannis, 1965; Peterson, 1981). Middle to Upper

Jurassic E llis Group rocks are also absent from the study area. A

large island mass which was part of the Big Belt Island complex

occupied much of Meagher County and prevented the deposition of

E llis Group sediments in the area (McMannis, 1965; Meyers, 1981;

Peterson, 1981). This island mass did not prevent deposition of

Upper Jurassic Morrison sediments as approximately 150 f t (45 m) of

Morrison Formation is present in the White Sulphur Springs area.

Tertiary Sediments

General Statement: Widespread deposition of Tertiary sediments in

western Montana began by Late Eocene to Oligocene time (Kuenzi &

Fields, 1971). The first terrigenous sediments were deposited in

rather broad fla t valleys, some of which were interconnected (Pardee,

1950; Wolfe, 1964). The Helena and Smith River Valleys were once a

continuous area of deposition before Late Cenozoic basin and range

tectonism uplifted the Big Belt Mountains (Reynolds, 1979; Wolfe,

1964). Evidence supporting this is the presence of Oligocene and

Early Miocene strata on the flanks of the Big Belt Mountains

(Koerner, 1939; Mertie, Fisher, & Hobbs, 1951; Reynolds, 1979; Wolfe,

1964). These exposures of volcanic ash, clay, s ilt, and isolated

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. conglomeratic deposits do not occur extensively at higher elevations

in the Big Belts because of their high susceptibility to erosion. No

evidence of extensional faulting in the area during or prior to the

Oligocene is known.

Faulting that formed basins and ranges such as the Smith River

basin and the Big Belt Mountains began in Middle Miocene time

(Reynolds, 1979). During Middle Miocene time, erosion caused by

regional u p lift and a hiatus in volcanic a c tiv ity prevented sediment

deposition in western Montana (Rasmussen, 1973). This hiatus in

deposition has been recognized in the White Sulphur Springs area

(Koerner, 1939; Wolfe, 1964).

Tertiary deposits in the Smith River Valley consist of the Lower

Miocene Fort Logan Formation and the Upper Miocene Deep River Forma

tion. These units are separated by an unconformity that is related

to the Middle Miocene hiatus. Because of the poor exposure of T e rti

ary sediments in the area, the Upper and Lower Miocene Formations

were mapped as one unit. The exact thickness of both formations are

unknown because they are poorly exposed. A gravity survey and model

ing by Gogas (personal communication, 1983) gave an approximate

maximum depth of 2000 f t (610 m) for the basin.

Lower Miocene Fort Logan Formation

The Fort Logan Formation is composed primarily of lig h t tan-

orange clay, sand, and conglomeratic tuffaceous siltstones in te r

bedded with lig h t gray volcanic ash, lake bed clays, and channel

conglomerates. Coarse-grained components in the sandstones and

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. conglomerates include clast! derived from Belt Supergroup shales and

sandstones, Paleozoic sandstones and limestones, and Tertiary porphy-

r it ic igneous rocks. A conglomerate containing these clasts is

exposed in a roadcut two miles northeast of White Sulphur Springs.

Lake bed clays of the Fort Logan Formation form the eastern margin of

Lower Miocene lake bed deposits in Montana (Reynolds, 1979). These

lake bed clays were possibly deposited when u p lift occurred more

rapidly than erosional processes, producing ponded areas in the Smith

River Valley (Wolfe, 1964). Kuenzi and Fields (1971) interpreted

sim ilar deposits in the Three Forks-Jefferson River basins as over

bank deposits from sediment-choked water courses, and occasionally

as lacustrine, d eltaic, or paludal deposits.

Fields, Rasmussen, Tabrum, and Nichols (1985) suggested that the

"Fort Logan Formation" is an informal name (name applied without

designation of type section) and should probably be included in the

Renova Formation. The Fort Logan beds are equivalent to the upper

part of the Renova Formation, which is dominated by fresh volcani-

clastics and montmorillonite mudstone.

Upper Miocene Deep River Formation

The Deep River Formation has a sim ilar composition and uncon-

formably overlies the Fort Logan Formation. Deep River beds are

time equivalent to the lower part of the Sixmile Creek Formation

(Fields et a l., 1985). According to Koerner (1939), the Deep River

Formation has larger glass fragments, more hornblende and plagioclase,

is less well cemented, and has a darker brown color than the Fort

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Logan Formation. He also recognized a greater abundance of stream

channels in the Deep River.

Clay-rich deposits are common in both Miocene deposits. Many

clay deposits are probably water-laid or ash fa ll tuffs that are

partially altered to bentonite or montmorilIonite. According to

Pardee (1950), many "lake bed" deposits in western Montana basins are

water-laid tuffs or volcanic ash mixed with terrigenous material that

is partially or completely altered. Fields et a l. (1985) identified

Lower Miocene Renova Formation equivalents (Fort Logan beds) as

being dominated by fresh volcanielastics and montmoril Ionite mud

stones, whereas Upper Miocene Sixmile Creek Formation equivalents

(Deep River beds) are characterized by coarse elastics locally

derived from developing fault-block mountains.

Quaternary Alluvium

A thin veneer of allu vial sediments cover a large area of the

Smith River Valley and associated drainages (Plate 1). These sedi

ments are primarily bedded stream deposits interbedded with flood

plain silts and ponded clays. The alluvium may be associated with

colluvial materials, especially near the margins of the basin. The

presence of gravel, sand, s ilt , and clay in deposits of Quaternary

age makes them extremely difficult to distinguish from Tertiary

sediments in water well logs, primarily because many water well logs

are exceptionally vague in their sediment descriptions. Therefore,

the thickness of the Quaternary is not well defined in this area.

On the basis of existing well data the w riter estimates the maximum

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 20

thickness of Quaternary alluvium to be 125 f t to 150 f t ; however,

Tertiary sediments are generally encountered below 40 f t . Alluvium

may exceed 150 f t in thickness west of White Sulphur Springs near

the junction of the main Smith and North Fork of the Smith River.

Deep wells do not exist nor are they necessary in this area due to

the shallow water table and high specific yield of gravels.

Igneous A ctivity

Castle Mountain Stock and Related Volcanics

According to Reynolds (personal communication, 1982) the emplace

ment of the Castle Mountain stock occurred in Early Eocene time

(-54 Ma). Late phase rhyolitic or rhyodacite extrusives that post

date the main intrusion have been dated at 47.6 Ma ± 1.8 Ma

(Chadwick, 1980). These volcanics form lith ic flow breccias and

welded tu ff deposits in the area (Phelps, 1969).

The stock intruded sedimentary rocks that range in age from

Beltian to Late Cretaceous. Emplacement of the stock truncated

Pal eocene thrust belt structures such as the Moors Mountain thrust

zone near the western margin of the intrusive. This margin has a

fa ir ly regular contact, dipping more than 60° to the west (Tanner,

1949).

The Castle Mountain stock is mainly composed of fine-to-medium

grained granite and granite porphyry although other compositions

include d io rite , granodiorite, monzonite porphyry, and syenite

porphyry (Dahl, 1971; Winters, 1965). Diorite and granodiorite are

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. the dominant rock types of the Blackhawk stock which predates and is

east of the Castle stock (Tanner, 1949; Winters, 1965). Granodiorite

also occurs in s ills near the margin and within the Castle stock.

Syenites and monzonites are present in s ills and near the intrusive

margin where the country rock is limestone or dolomite.

Because of the granitic composition of the Castle Mountains,

Chadwick (1972, 1981) associated the intrusive with alkalic rocks

derived from the foreland portion of the Idaho-Montana porphyry b elt.

Many of these intrusives seem to be aligned zones that may be related

to deep-seated zones of weakness (Chadwick, 1981). Andesitic and

basaltic rocks commonly intrude fa u lt zones in the White Sulphur

Springs area (Dahl, 1971; this paper). This fault-intrusive relation

ship suggests that structures in the area may be deep seated.

Because these structures are probable extensions of the Lewis and

Clark line, the intrusives may be related to deep zones of weakness

controlled by this lineament.

Early Cenozoic igneous activ ity in west-central Montana may have

been related to the low angle of subduction associated with the

Laramide orogeny; hence, the low subduction angle may have caused

arc magmatism to occur farther inland where the subducted plate has

subsided deep enough for partial melting. Intrusives of west-central

Montana that have a sim ilar age, composition, and eastern extent as

the Castle Mountain stock include various plutons in the L ittle Belt

Mountains (Marvin, Witkind, Keeker, & Mehnert, 1973), and a grano

diorite intrusive in the Big Belts west of White Sulphur Springs

(Daniel & Berg, 1981).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Metamorphism related to the Castle intrusion is generally

restricted to the low-grade aureole near the margin of the stock.

Limestones contain minor amounts of epidote and are marble near the

contact of the stock. The Greyson Shale is the primary country rock

in contact with the western flank of the Castle Mountains and is

baked to a brittle hornfels near the contact. Chloritization and

epidotization is common in Belt rocks near the stock.

Deformation of country rocks related to the Castle intrusion is

restricted to the proximal area of the stock’s margin. Emplacement

of the stock has caused minor folding and small vertical offsets

(.5 mm - 10 mm) in bedding laminae of the Greyson Shale. Many jo in t

sets are also found in the baked Greyson Shale near the west margin

of the stock.

Basaltic Volcanism

Three separate basalt flows are located northeast of White

Sulphur Springs, the closest flow being 8 mi (13 km) from town.

These flows were mapped by Tanner (1949) and Dahl (1971) and are

named the Volcano Butte, Crater Lake, and Smoky Mountain basalt

flows respectively. The small flow in the northeast corner of the

map area (Plate 1) is part of the Volcano Butte basalt flow. This

flow yielded a whole rock K-Ar date of 29.1 Ma (Chadwick, 1978);

however, the sample was slig h tly chloritized with some fille d

vessicles, yielding some uncertainty to the date. This flow pre

dates the proposed Middle Miocene age (Reynolds, 1979) of basin-

and-range faulting in the area. Basalts in the Big Belt Mountains

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. west of the map area are interpreted to be Pliocene in age as they

lie unconformably on Miocene strata (Reynolds, 1979).

Oligocene basalt flows in the White Sulphur Springs area may

represent the onset of extensional tectonism in the area. Further

fie ld work and additional radiometric dating is needed to determine

the relationships between basalt flows and extensional tectonism in

the area.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER I I I

STRUCTURAL GEOLOGY

Precambrian Features

Belt Basin

The most prominent structural feature in western Montana during

Precambrian (Proterozoic) time was the Belt basin. The tectonic

history and origin of this basin is not completely understood,

prim arily due to the immense thickness of Belt and Phanerozoic rocks

that s t ill cover the old basin margin; therefore, exposures of pre-

or syn-Belt basin structures are rare.

The general consensus is that the origin of the Belt basin is

related to rifting of a proto-North American continent (Burchfiel &

Davis, 1975; Kleinkopf, 1977; McMannis, 1963; Schmidt & Garihan,

1986); however, Harrison et a l. (1974) suggested the Belt basin was

not a great aulocogen, but was subsidence of a continental crustal

block which was not necessarily a failed arm of a triple junction.

Burchfiel and Davis (1975) suggested that two periods of rifting are

responsible for the Belt-Purcell Supergroup and the Windemere Group.

Regardless of the time of riftin g , Belt sedimentation occurred

between 1400-1500 Ma and 850 Ma (Burchfiel & Davis, 1975; Harrison,

1972; Harrison et a l. , 1974).

In west-central Montana the Belt basin has an eastward-trending

embayment (Helena embayment) that was bordered on the north and south

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. by Archean crystalline rocks (Figure 6 ). The southern border of this

embayment was an active tectonic zone during Late Precambrian time

(Harrison, 1972; McMannis, 1963; Schmidt & Garihan, 1986), resulting

in the deposition of the clastic northward-thinning Lahood Formation.

The inferred basin-bounding feature responsible for this activation

is called the Willow Creek fa u lt (Harrison, 1972; Robinson, 1963).

The geometry of the Helena embayment and the presence of Archean

crystalline rocks north and south of the embayment were dominant

factors in controlling the extent and orientation of post-Belt struc

tures in the Helena salient. Harris (1957) was the fir s t to recog

nize the relationship between Belt sediment distribution and the

scope of post-Beltian tectonic features. Other controlling factors

of post-Beltian deformation may include the presence of Late Precam

brian northwest-trending faults (Schmidt & Garihan, 1986; Schmidt &

O'Neill, 1982). These previously established zones of weakness are

found in the southwest Montana transverse zone near the southern

margin of the Helena salient.

Winston (1986) attributed the formation of the Helena embayment

to graben blocks that were offset from the inferred Townsend lin e , a

northwest-trending Proterozoic fault line that extends from the north

end of the Bridger Range, northwestward along the Townsend Valley.

Winston (1986) inferred a west-northwest trending line/termed the

Joco lin e , to be a dominant structural control near the northern

margin of the Belt basin. The Joco line is interpreted to be a zone

of Proterozoic growth faults that is evidenced by linear trends of

abrupt stratigraphic thickening that coincide with separated loci of

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. MOUNTAIN FORELAND \ N ^ ■ ' - N / \ 'f. \> / \ / ' /

embayment jBASIN Helena £ O § o ' c or LoHood w ° > Formation

Inferred zone MONTANA ' o f basement r i f t i n g WYOMING

Isopach countour Interval 3 5000 ft.

Figure 6. General tectonic map showing the relationship between the Belt Basin, the Lahood Formation, and Late Precambrian faults. (Modified from Schmidts Garihan, 1984.)

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission 27

soft-sediment deformation. Similar basement controlling faults may

be present near the northern margin of the Helena salient associated

with the Lewis and Clark lin e .

Lewis and Clark Line

The Lewis and Clark line (Figure 2) has been a prominent struc

tural feature, exhibiting movement from Precambrian through Holocene

time (Reynolds, 1977, 1979). Sinestral movement occurred along the

west-northwest-trending line from Late Cretaceous to Early Cenozoic

time whereas dextral movement occurred during Late Cenozoic extension-

alism (Reynolds, 1979). Cenozoic right lateral displacements associ

ated with the Osborn and St. Marys fa u lt segments of the lin e are

estimated to be 26 km and 13 km respectively (Harrison et a l., 1974).

The relationship of the Lewis and Clark line to disturbed belt and

basin and range features in the White Sulphur Springs area w ill be

discussed in later sections.

Fold and Thrust Belt Tectonic Setting

The Laramide orogeny (~75-45 Ma) probably occurred when a more

rapid westward motion of the North American plate accompanied an

accelerated northeast-to-southwest convergence between the North

American and Farallon plates (Coney, 1978; Dickinson, 1979).

Compressional features in the White Sulphur Springs area are princi

pally folds and thrusts of the Montana disturbed belt. The disturbed

belt (Cohee, 1962; Mudge 1970) is a term used to designate the

structural style of folds and thrusts between the Rocky Mountain

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 28

foreland and the Cordilleran miogeosyncline in northwest and west-

central Montana. Structures of the fold and thrust belt formed when

supracrustal rocks in the geosyncline moved re la tiv e ly eastward and

impinged against the western margin of the foreland (Figure 2).

Thrusts in the disturbed belt typically dip to the west or southwest

and have a tectonic style that ranges from steep imbricate thrusts

in the Sawtooth Range and northern Big Belt Mountains (Bregman, 1976;

Mudge, 1970; Shaffer, 1971) to low angle thrusts such as the Eldorado

thrust in the Beartooth Mountain area northeast of Helena. These

thrusts have been interpreted to be listric in nature and possibly

merge with a main or sole thrust (Mudge, 1970; Woodward, 1981).

The majority of disturbed belt thrusts in west-central Montana

juxtapose Belt Supergroup strata (hanging wall) against Paleozoic and

Mesozoic footwall rocks; however, some thrusts have Belt rocks in

both the footwall and hanging wall (McGrew, 1977c, 1977d; Shaffer,

1971; and this paper). Ages determined for thrusting in the disturbed

belt range from 72 Ma to 56 Ma (Hoffman, Hower, & Aronson, 1976).

The Helena or central Montana salient is a prominent eastward

bulge in the disturbed belt (Figure 2 ). Fold and thrust features in

the salient have a distinctive convex eastward geometry that was

probably formed by a regional west to east compressive force. Con

trols on the geometry of the salient include the shape of the Precam-

brian Helena or Beltian embayment (Figure 6) and the buttressing

effect of the stable foreland. Beutner (1977) associates salient

features in the Wyoming and central Montana salient to foreland

impingement. Both salients have reentrants of the foreland

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. associated with them. The possibility of radial divergent gravity

gliding produced by the emplacement of the Boulder batholith may have

added to the kinematics of salient structures (Smedes & Schmidt, 1979);

however, thrusts in the salient range in age from pre- to post-batholith

time (78-68 Ma; Robinson, Klepper, & Obradovich, 1968) indicating the

intrusion was not a primary influence in forming the Helena salient.

The northern boundary of the salient is part of the Lewis and

Clark lin e , a suspected zone of le ft-la te ra l movement during thrust

ing (Reynolds, 1979; Smedes & Schmidt, 1979). The salient's southern

boundary is part of the southwest Montana transverse zone which has a

significant rig h t-latera l s trik e -s lip component (Schmidt, 1975;

Schmidt & Hendrix, 1981; Schmidt & O 'N e ill, 1982). These structural

margins appear to be oblique and lateral ramp zones respectively in

the thrusts of the Helena salient (Schmidt & Garihan, 1986). Accord

ing to these ideas, thrusts in the White Sulphur Springs area should

display similar sinestral slip when parallel to the Lewis and Clark

lin e.

Major thrusts in the salient are interpreted to merge into a

decollement or sole fa u lt that is near the base of Belt sediments

(Birkholz, 1967; Schmidt & O 'N e ill, 1982; Shaffer, 1971; Woodward,

1981; and others). This decollement was formed when the Belt sedi

mentary prism, along with younger rocks, was detached from the pre-

Belt basement floor and transported eastward approximately 15 km to

20 km (Schmidt & O'Neill, 1982). Resultant deformation was an

imbricate fold and thrust system that merged into the major decolle

ment. Mudge (1970) indicated that a sim ilar decollement exists in

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. the disturbed belt north of the Helena salient. An expanded discus

sion of Laramide features in the White Sulphur Springs area is

presented in the following section.

Description of Thrust Faulting

Statement regarding nomenclature: The thrust which was referred to

as the Scout Camp-Willow Creek thrust fa u lt by Birkholz (1967),

Phelps (1969), Woodward (1981), and others is interpreted by Reynolds

(personal communication, 1982) to be miscorrelated and is probably

the Moors Mountain thrust by his nomenclature. Reynolds can demon

strate by mapping southeast from the northern Big Belt Mountains that

previous workers miscorrelated the fa u lt; therefore, the name Moors

Mountain thrust fault will be used in this thesis.

Moors Mountain Thrust Zone

The Moors Mountain thrust zone was fir s t mapped in the White

Sulphur Springs area by Weed and Pirsson (1896) who called the thrust

the Willow Creek Fault. Other portions of the fa u lt zone were

studied in greater detail by Tanner (1949), Hruska (1967), Birkholz

(1967), Dahl (1971), Phelps (1969), Shaffer (1971), and Reynolds

(unpublished mapping, U.S.G.S.). The Moors Mountain thrust zone in

this area brings allochthonous Belt rocks (Newland Limestone and

Greyson Shale) against Paleozoic strata. The trace of the thrust

extends for approximately 55 mi (89 km) from the northwest corner of

the Castle Mountains to the northern flank of the Big Belt Mountains.

The thrust has an estimated minimum stratigraphic throw of 2.2 mi

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (3.5 km) and dips roughly 45° to the west and southwest at the sur

face. The steep dip is interpreted by the author to be from ramping

of the thrust from a decollement fa u lt at depth.

In the White Sulphur Springs area the Moors Mountain thrust

changes trend from west-northwest to north-south at its eastern mar

gin (see Figure 7) where i t is truncated by the Early Eocene Castle

Mountain stock (Plate 1). The change in trend occurs in a relativ ely

short distance of 4 mi (2.5 km). A relationship between the trend of

the Moors Mountain thrust and a minor change in slip direction seems

evident. An oblique sinestral slip component possibly exists where

the thrust trends west-northwest, and a predominant dip-slip compo

nent is present where the trend is more northerly. Evidence support

ing le ft-la te ra l movement on the thrust was f ir s t recognized by

Birkholz (1967). He measured minor folds in the hanging wall of the

thrust and suggested that the northwest trend of the folds implied a

left-lateral component for the west-northwest-trending thrust on the

eastern flank of the Big Belt Mountains. A sim ilar group of folds in

the Newland Limestone north of White Sulphur Springs (NE*s, sec. 5,

T.9N., R.7E.) plunge 40° to the southwest (Appendix B, p. 99). This

orientation indicates a possible minor left-lateral component as the

fold axis is southwest and slightly oblique to the fault trace.

Further evidence supporting a sinestral component of movement along

the west-northwest-trending segment of the Moors Mountain thrust is

scarce; however, predominant dip-slip movement may be inferred on the

basis of fie ld evidence for north-trending segments of the thrust.

Such evidence includes the orientations of the overturned Willow

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Figure 7. A - Photograph (looking northwest) of the Moors Mountain thrust zone and Pennsylvanian Quadrant klippens northeast of White Sulphur Springs. B - Sketch of structural features in the photograph. Rock units: Mz - Mesozoic rocks; p€g - Precambrian Greyson Shale; Pq - Pennsylvanian Quadrant Formation; Pz - Paleozoic rocks; Ts - Tertiary sediments.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 33

Greek syncline and minor folds in the Amsden Formation (see Plate 1)

which comprise footwall strata.

The abrupt change in strike and the indication of predominant

dip-slip movement for the north-trending thrust segment, suggests the

west-northwest-trending thrust segment is an oblique ramp with some

sinestral movement. I f predominant dip-slip movement occurred along

both fault segments, northeast extensional or dilational features

should exist between the two segments (Figure 8 ). Northeast-trending

normal faults do exist west (Birkholz, 1967) and south (see Plate 1)

of White Sulphur Springs; however, such features are not evident near

the expected zone of dilatio n . Predominant dip-slip movement along

both thrust segments should not be ruled out as Tertiary and alluvial

sediments cover much of the expected zone of extension.

Woodward (1981) reviewed information regarding the thrusts in

the Helena salient, including the Moors Mountain and Scout Camp

thrusts (Figure 9). He also suggested that a sinestral component

exists where these thrusts trend west-northwest and a dominant dip-

slip component where the trend is to the north. Similar interpreta

tions have been made for the Montana transverse zone as the southern

margin of the Helena salient, with the exception that strike-slip

movement was dextral (Schmidt, 1975; Schmidt & O 'N eill, 1982).

Figure 9 is a diagrammatic sketch showing the relationship between

the slip component to trends of faults in the Helena salient.

The Moors Mountain thrust is interpreted to be a possible folded

thrust on the northern flank of the Big Belt Mountains (Shaffer,

1971). No evidence was found for folding of the Moors Mountain

/ Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 34

arrows Indicating relative lateral movement sense

PRINCIPAL SHORTENING DIRECTION mmA sawteeth indicate predominant dip- slip movement

PRINCIPAL SHORTENING DIRECTION w

diverging arrows indicating extension or dilation

Figure 8. A - Sketch showing a change in slip movement (oblique le ft-la te ra l when trending west-northwest and predominant dip-slip movement when trending north) which may be associated with convex-eastward thrust faults in west-central Montana. B - Sketch illustrating dilation or extensional features that would be expected i f predominant dip-slip movement occurred along the length of a thrust that had an arcuate trace.

/ Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. While

PRINCIPAL SHORTENING DIRECTION

x. • — ----- Jefferson Canyon fault

1 „ . V I..

\ \

Figure 9. Diagrammatic sketch showing the outline of the Helena structural salient and inferred oblique slip. (Modified from Woodward, 1981).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 36

thrust in this area; however, several Pennsylvanian Quadrant klippen

in the southwest limb of the Willow Creek syncline (Plate 1) and the

Fivemile Creek klippe to the east (Dahl, 1971) suggest that thrusts

in the area become subhorizontal in dip and may be connected to a

roof fa u lt (see Figure 11).

Observed deformation in the hanging wall block is not extensive

in the White Sulphur Springs area. The lack of observed deformation

in the ramp portion of the thrust is probably related to minimal

exposure of the hanging wall due to Tertiary normal faulting.

Another less lik e ly explanation is the removal of the more intensely

deformed portion of the ramp by erosion; hence, the observer sees a

lower structural level where deformation is generally minimal.

Figure 10 uses the Lombard and Moors Mountain thrusts as examples

for differences in observed deformation due to dissim ilar levels of

erosion. The fact that deformation of allochthonous rocks is

greatest near the nose of the ramp region of a thrust was well docu

mented by Morse (1977).

Upper Cretaceous (lower Colorado Group) rocks are involved in

folding associated with the Moors Mountain thrust suggesting that

thrusting occurred between Late Cretaceous and Early Eocene time

(age of Castle Mountain stock). The thrust is probably late Paleo-

cene in age (Reynolds, personal communication, 1982; Schmidt,

personal communication, 1982). The age of thrusting in the disturbed

belt of Montana ranges from Late Cretaceous to Late Pal eocene time

(Hoffman et a l., 1976; Mehnert & Schmidt, 1971).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 37

Mesozoics

Paleozoics

Mesozoics

Paleozoics

Figure 10. Diagrammatic sketches which illu s tra te that variations in the observed deformation of allochthonous thrust plates may be related to different erosional levels. Examples used include (A) the Lombard thrust near Toston and (B) the Moors Mountain thrust near White Sulphur Springs. Rock units: p€g -Precambrian Greyson Shale; p€s - Precambrian Spokane Shale; Kk - Cretaceous Kootenai Formation.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 38

Sequential development of the Moors Mountain thrust zone along

with the Pinchout Creek and Fourmile Creek thrusts is illu strated in

Figure 11. This sequence and type of faulting explains the Quadrant

klippens (Plate 1) and the Fivemile Creek klippe just east of the

map area (Dahl, 1971). Imbrication and duplexing also explains the

folded Moors Mountain thrust near the northern flank of the Big Belt

Mountains (Shaffer, 1971). This sequence of thrusting is only a

preliminary interpretation of local structures in the area as regional

relationships must be known to accurately define the sequential

development of thrusts; however, folding of the Moors Mountain thrust

in the Big Belt Mountains (Shaffer, 1971) and klippens in the White

Sulphur Springs area suggest that thrusting is not formed by the

piling up of imbricate thrusts (Woodward, 1981) that appear progres

sively younger to the west, but is due to imbrication from duplexing

(Figure 11), forming thrusts that may be progressively younger to

the east.

Minor Faults. Two minor faults are associated with the Moors

Mountain thrust zone within the map area. The fir s t and more exten

sive of the two is a footwall splay of the Moors Mountain thrust

zone that is along the western margin of the overturned Willow Creek

syncline (see Plate 1). This thrust mainly places Amsden Formation

and Madison Limestone against the Cretaceous Kootenai Formation. The

inferred Craig thrust (Plate 1)—as designated by Phelps (1969)—

causes repetition in Madison Group bedding in the northwestern corner

of the area and may be a westward extension of this minor thrust

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. S \/ 7 \U){ CO CL CM CL Q. /vs. '/ CO CL CM V/ '\ V/ V/ m cm ui>| Q.

CM III z MS Reproduced with permission ofthe copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.

i i P P FM FM FMK P i P i MM PC NS P i HB ss Pz Note: Note: shifted was thrust Each due to right from sequence crustal problems to shortening; le therefore, special ft lateral the to (NE to X symbol SW) accommodate shifting , is of a sequence. each point of reference for the (1) Pre-tectonic setting with in itia l stratigraphic and trace succession of fault plane; (2) Development of(2) Butte Horse Development thrust fault related and roof fault near the Paleozoic-Mesozoic (5) Continuation of duplex imbrication of and development the Fourmile Creek thrust; (6) Present SS, SS, Smith River Southern basin; Butte HB, Horse thrust;Creek thrust; thrust; Mountain Moors NS, MM, northern FM, Fourmile Creek Smith thrust; River units: Rock basin; Fivemile FMK, PC, Pinchout Creek Klippe. - Mz rocks, Mesozoic Pz - Paleozoic (-700 rocks, S - f Shale, t )- G Spokane . Shale, Greyson contact; of (3) the Development Creek Pinchout thrust forming a decollement near the Greyson- erosional erosional the surface possible showing relationship thrust between faults and lis tric normal faults. Spokane Shale contact with Spokane associated folding of the roof fault; (4) of the Development Moors N N - - Limestone, Ch Shale, overlying and Newland Chamberlain A - basement Neihart Archean Quartzite Mountain thrustMountain with a of large crustal amount shortening along with folding of previous structures; Figure'll. sketch of of Diagrammatic the sequence faulting-in the White Sulphur Springs area.

thrust, and the eastern margin of the fault is also truncated by the

Castle Mountain stock. The thrust is relatively steep at the surface

(45°-50° dip) and has a stratigraphic throw of approximately 350 ft

(107 m). The inferred relationship of this fault to the Moors Moun

tain thrust is shown in Plate 2 (section B-B').

The second minor fa u lt is located between the Moors Mountain and

Craig thrusts 2.5 mi north of White Sulphur Springs. The trend of

this fault ranges from northwest to northeast, and is interpreted to

merge with the Moors Mountain thrust at its western margin and the

Craig thrust at its eastern margin. The fa u lt forms a connecting

splay according to Boyer and E llio tt's (1982) terminology. Movement

on the fau lt is not well understood due to its poor exposure which

may be related to late r downdropping of the hanging wall of the Craig

thrust. Evidence to support recurrent normal movement along the

thrust plate includes the deposition of Tertiary sediments and collu-

vium over hanging wall s trata, and two small exposures of Quadrant

formation in contact with older Madison Group Limestone. This

younger on older relationship may re fle ct la te r normal movement along

the preexisting zone of weakness formed by the minor thrust fa u lt.

Therefore, downdrop symbols were placed on the thrust and the two

Quadrant splays to indicate la te r downward movement (Plate 1).

A minor hanging-wall splay is inferred between the Moors Moun

tain and Pinchout Creek thrusts north of town (see Plate 1). This

thrust explains the abnormally thin Belt Supergroup section present

between the Moors Mountain and Pinchout Creek thrusts. The thrust

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. is probably near the Greyson Shale-Newland Limestone contact although

its presence is highly speculative.

Pinchout Creek Thrust

This fault has not been previously mapped in the area; therefore,

the name Pinchout Creek thrust w ill be applied to this fa u lt because

it traverses a portion of the creek east of town. The existence of

the thrust explains the close spatial relationship between the

Spokane Shale-Flathead Sandstone outcrop on the north edge of town

to the Greyson Shale penetrated in the bank thermal well at a depth of

35 f t , and in the roadcut ju st east of town (Reynolds, personal

communication, 1983). The outcrop of Spokane Shale and Flathead

Sandstone are inferred to be part of footwall rocks, with the Greyson

Shale comprising hanging wall rocks (section A-A', Plate 2). South

east of White Sulphur Springs the Greyson Shale forms both the

hanging wall and the footwall of the thrust, accounting for the dis

cordant attitudes in the eastern half of sec. 21, T.9N., R.7E. The

fault has a convex-eastward shape that is sim ilar to the Moors Moun

tain thrust zone. Due to the lack of exposure, the attitude of the

thrust surface is not known. The lack of surface control and the

indication that the fault is a bedding plane thrust makes a determina

tion of the stratigraphic displacement d iffic u lt. The thrust may be

a hanging-wall splay (see Figure 11) of the Moors Mountain sheet.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Mission Canyon Fault

The Mission Canyon thrust was fir s t mapped by Tanner (1949) and

was named the Fourmile fa u lt. Phelps (1969) la te r named the fau lt

the Mission Canyon thrust. Because the fa u lt has a large le f t -

lateral separation, the name Mission Canyon fa u lt w ill be used. The

fa u lt lies in the northern portion of the map area and trends north

east (Plate 1). This fa u lt is terminated by the Craig thrust to the

southeast, and is interpreted to be a secondary tear in the thrust

sheet north of the Fourmile Creek thrust. Apparent le ft-la te ra l

separation along the fa u lt is approximately 335 m, suggesting a

significant sinestral component of movement. Based on map data

(Dahl, 1971; Phelps, 1959), the fa u lt appears to be steeply dipping

(65°-75°). The eastern margin of the fault is covered by the Oligo-

cene (Chadwick, 1978) Volcano Valley basalt flows.

Apparent separation along the fa u lt may have increased during

Cenozoic extension although conclusions regarding normal movement

could not be made with existing data. More detailed study of the

fault surface is needed to understand the kinematics and origin of

the Mission Canyon fa u lt.

Fourmile Creek Thrust

This thrust was named the Fourmile Creek fa u lt by Tanner (1949)

as i t is well exposed in the Fourmile Creek area about 8 miles (12.8

km) east-northeast of White Sulphur Springs. I t w ill be referred to

as the Fourmile Creek thrust in this paper (see Plate 1). Using

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Boyer and E llio tt's (1982) terminology for thrusting, the Fourmile

Creek thrust is interpreted to be a divergent splay. The existence

of the thrust explains the discordant attitudes and apparent offset

between the northern limb of the Willow Creek syncline which is cut

by the North Fork of the Smith River. The fau lt trends westerly in

this area, but bends to the south in the Fourmile Creek area, sim ilar

to the trend of the Moors Mountain thrust. The fa u lt does not follow

the North Fork of the Smith River as indicated by previous workers

(Dahl, 1971; Tanner, 1949). The fact that the northwest-trending

hinge of the Willow Creek syncline is not offest in the area (SE%,

sec. 34, T.9N., R.7E.) confirms th is. Because this fa u lt is hidden

by Tertiary sediments, andesite, and Quaternary alluvium, its loca

tion is inferred.

Horse Butte Thrust Zone

Previous reconnaissance mapping in the southern portion of the

study area was done by Weed and Pirsson (1896), Tanner (1949), and

Groff (1965); but the majority of faults in the area were not id en ti

fied or named. These northwest-trending faults can be traced to the

southeast and correlated with the Horse Butte thrust zone in the

Ringling Quadrangle (McGrew, 1977b). Because the correlation of

these thrusts is very apparent, the name Horse Butte thrust zone w ill

be used hereafter.

The Horse Butte thrust zone consists of five thrusts that

generally trend northwest, although the main thrust changes trend

from northwest to north-northwest further south. Total s tra ti graphic

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. throw based on cross section C-C' (Plate 2) is a minimum of 580 m for

the entire zone. The Horse Butte thrust fa u lt is the westernmost

thrust of the fa u lt zone, and where i t trends northwest i t places

Precambrian Spokane and Cambrian strata against the Meagher Limestone.

Further to the south (sec. 32, T.8N., R.7E.) the thrust changes trend

to north-northwest, cutting the western limb of a small syncline and

juxtaposing Cambrian Pilgrim Limestone against Upper Cambrian and

Devonian strata. Stratigraphic throw is approximately 365 m to 430 m.

Local topographic r e lie f is not great enough for an accurate deter

mination of dip by three-point problem, but the thrusts are estimated

to dip about 45°-50° to the southwest. Slip direction along the

thrust zone is predominantly dip slip as indicated by the parallel

trends and shallow plunge of minor fold axes and the orientation of

footwall anticlines and synclines.

Deformation within the Horse Butte thrust sheet is primarily

restricted to the Spokane Formation, with the exception of a small

dextral tear fa u lt in Spokane Shale and Cambrian strata in the

western half of sec. 32, T.8N., R.7E. Dips in the sparse outcrops

of Spokane Shale are very diverse, indicating intense folding and

possible shearing in the hanging w all.

The Horse Butte thrust zone is interpreted by McGrew (1977b) to

be Late Paleocene in age. A Middle to Late Paleocene age for this

thrust zone is reasonable as Upper Cretaceous rocks are involved in

deformation related to thrusting.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 45

Minor Faults. The four faults northeast of the main Horse Butte

thrust are shear zones in the western limb of a footwall syncline

(see section C-C‘ , Plate 2). Using cross section C-C', stratigraphic

throws of these minor imbricates range from less than 20 m to over

150 m. Field observations reveal the faults to be relatively steep,

dipping 45°-60° to the southwest with northwest trends.

Because the displacement on these thrusts is much less than the

main Horse Butte thrust, cross-section interpretation C-C' (Plate 2)

suggests that the faults are imbricate thrusts in the footwall.

These minor faults probably formed after and are structurally lower

than the main Horse Butte thrust.

Description of Folding

General statement: Numerous folds with wavelengths ranging from 4 m

to over 1 km are exposed within the map area. Major folds are repre

sented as footwall synclines and anticlines associated with the Moors

Mountain and Horse Butte thrust zone. Small wavelength parasitic

folds are generally present within the fold limbs of major anticlines

and synclines. Fold hinges are primarily parallel to the major

thrusts, indicating predominantly dip-slip movement of hanging walls

of adjacent thrusts. Stereographic analyses of folds within the

White Sulphur Springs area are in Appendix B.

Willow Creek Syncline

The northeast-to-east verging Willow Creek syncline is a broad

doubly plunging fold with smaller folds radiating from i t . I t is

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. associated with the footwall of the Moors Mountain thrust zone. The

overturned western limb of the syncline ranges in strike from due

north to N 70° W and dips roughly 50°-80° to the southwest. The

overturned limb is well exposed in the NE% of section 10, T.9N.,

R.7E. (Plate 1). The northwestern part of the fold hinge gently

plunges 10° to the southeast, and the southern fold hinge plunges 33°

to the north-northwest. The northv/estern hinge of the syncline is

well exposed a few feet west of Highway 89, revealing the Pennsylva

nian Tyler, Amsden, and Quadrant Formations (B-B', Plates 1 and 2).

The southern part of the hinge of the Willow Creek syncline is trun

cated roughly perpendicular to its axial trace by the Early-Middle

Eocene Castle Mountain stock.

Cottonwood Creek Syncline and Associated Folds

The broad footwall syncline associated with the Horse Butte

thrust zone was fir s t mapped by Weed and Pirsson (1896) who called i t

the Cottonwood trough. I t is herein referred to as the Cottonwood

Creek syncline. The northeast limb of the syncline is marked by the

concordant margin of the Castle Mountain stock that is in contact

with Precambrian Greyson Shale. The southwest limb is associated

with more tightly folded anticlines and synclines that are all

related to the Horse Butte thrust fau lt zone to the southwest. Fold

limbs on the Cottonwood syncline have gentle to moderate dips (10°

to 60°), with an interlimb angle of roughly 110°. The hinge o f the

syncline plunges 20° to the north-northeast (Appendix B, p. 100).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 47

An unbroken stratigraphic section from the Precambrian Greyson Shale

to the Upper Cretaceous Colorado Group is exposed in the syncline.

The southwest limb o f the Cottonwood Creek syncline becomes a

more tig h tly folded anticline to the southwest. Minor folding within

this anticline forms a minor anticlinal-syncline fold in section 23,

T.8N., R.7E. (see Plate 1 ). Outcrops of these minor folds are sparse,

hence, most of the contacts are inferred. The anticline exposes

strata from Mission Canyon Limestone to Kootenai Sandstone and has a

disharmonically folded hinge region which produces a W-shaped plung

ing anticline-syncline-anticline structure in the NW% of sec. 34,

T.8N., R.7E. The southern hinge of the folded anticlinal nose

plunges 30° to the southeast (Appendix B, p. 103) and is very well

exposed at the Pennsylvanian Amsden-Quadrant contact near the hinge

of the fold (Plate 1). The interlimb angle of the southern a n ti

clinal nose is roughly 10°, revealing the tig ht nature of the fold.

The southwestern flank of the anticline becomes a very tig h tly

folded syncline that is cut at its southwest limb by a thrust fault.

This thrust is part of the Horse Butte thrust fault zone that juxta

poses Mississippian Mission Canyon Limestone against synclinal rocks

that range from Mississippian to Late Cretaceous in age. The syncli

nal rocks are not exposed adjacent to the thrust to reveal i f the

syncline is overturned; however, sparse exposures of Kootenai Sand

stone and Big Snowy Group in the trough of the syncline (NE%, sec.

33, T.8N., R.7E.) reveal its tightly folded geometry (Plate 1).

Minor folds associated with the Horse Butte thrust zone are

common. Figure 12 is a sketch illu s tra tin g the relationship of folds

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 48

€w Fold C SW •€m NE -€w •Cm

p-Cs €m

approximate scale 2 5 0 5 0 0 feet p€s

Figure 12. Sketch showing the relationship of folding to thrusting along the Horse Butte thrust zone (fold C.is in the SW% of section 29, T.8N., R.7E., Plate 1).

to faulting along the Horse Butte thrust zone. Minor folds shown in

Figure 12 are within the Meagher Limestone located in the SW%, sec.

29, T.8N., R.7E. (Plate 1).

Post-Fold and Thrust Belt Deformation in the White Sulphur Springs Area

Regional Setting and History

A marked change from compressional thrust-belt tectonics to

extensional basin and range tectonics began in western Montana during

Late Eocene time (Kuenzi & Fields, 1971). Crustal arching accom

panied by regional extension produced basin and range features in

western Montana that are similar to that of the Great Basin region.

The tectonic style of such features in Montana have been interpreted

by many workers (for example, Chadwick, 1981; Reynolds, 1979) to be

a northern extension of the Great Basin region. Both areas have

similar heat flow and structural margins to the east, along with

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 49

similar Cenozoic histories and structural characteristics; however,

both areas are significantly different regarding their intensity of

heat flow, degree of extension, and style of normal faulting.

The faults that formed the margins of basins in western Montana

were established in Middle Miocene time (Reynolds, 1979); however,

Tertiary sedimentation began in intermontane basins in Late Eocene to

Early Oligocene time (Kuenzi & Fields, 1971; Pardee, 1950; Wolfe,

1964; and others). Many of these pre-Middle Miocene sediments can be

found on the flanks of ranges such as the Big Belt Mountains, indicat

ing their relative uplift in relation to downdropped valleys. Figure

3 shows the locations of basins and ranges in western Montana. Total

horizontal extension that produced such features across western

Montana is estimated to be a minimum of 10% to 15% (Reynolds, 1979).

Extensional tectonism may s t ill be active in the White Sulphur

Springs area. Evidence suggesting this includes the Montana earth

quake of 1925 which caused extensive damage in the White Sulphur

Springs region (Pardee, 1926). The focus of the earthquake was along

a post-Miocene fau lt that was located on the western margin of the

Big Belt Mountains near the town of Lombard (Pardee, 1926). The

earthquake ac tiv ity suggests that the Big Belts are s t ill being

uplifted in relation to the Townsend and Smith River Valleys.

During Middle and Late Cenozoic extension the Lewis and Clark

lin e exhibited a dextral component of movement that formed basins and

ranges south of the major lineament (Reynolds, 1979). Figure 13

shows the relationship between the Lewis and Clark line to basins and

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 50

Lewis and Q ar^-jine,

,SR

Figure 13. Generalized block diagrams illu s tra tin g the possible relationship between preexisting Laramide zones of weakness and Cenozoic basin-range extensional features at the eastern margin of the Lewis and Clark line. A - Undeformed block showing pre-extensional surface. B - Structures and extensional features of the Helena and White Sulphur Springs area. SR, Smith River Valley; SH, Spokane Hills; SG, Scratch-gravel Hills. Rock units: 1) Cenozoic sedimentary rocks; 2) Cretaceous intrusives; 3) Paleozoic rocks; 4) Precambrian Belt Supergroup strata. The probable complex structural culmination which forms the Big Belt Mountains is not illu strated . (Modified from Reynolds, 1979.)

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ranges south of the lineament. The Smith River Valley is the eastern

most basin formed by a dextral movement along this lin e .

The coincidence of the eastern margin of the Lewis and Clark

line with the eastern lim it of the fold and thrust belt suggests

possible recurrent movement along preexisting zones of weakness.

Basin-bounding faults may merge with thrust faults at depth, forming

listric normal faults. Figure 14 illustrates the development of a

listric normal fault in which thrust plates or portions of plates may

exhibit reverse drag movement during post-Laramide extension. Evi

dence supporting listric normal faulting in the Smith River Valley

includes the following: (a) Miocene sediments dip 4°-10° to the

southeast (Wolfe, 1964) and may increase in dip near the valley's

eastern basin-bounding fa u lt; (b) the close relationship--in map

view (Plate 1)—of normal faults and Tertiary sediments to the convex

eastward Pinchout Creek thrust that passes through the north edge of

town; (c) indications of recurrent downdropping of northwest-trending

thrusts in the area; and (d) gravity data (Gogas, 1984; this paper)

suggesting that the eastern basin margin is deeper and has a sim ilar

convex eastward geometry to that of thrusts in the area. Greater

downward rotation along the eastern margin of the basin may be

related to reverse drag of old thrust sheets.

The downwarping of Tertiary sediments is commonly associated

with rotations of the downdropped block accompanying lis tr ic normal

faulting (Anderson, Zoback, & Thompson, 1983). Figure 15 shows the

possible relationship between thrust faults and basin-bounding faults

in the Smith River Valley.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 52

Figure 14. Schematic diagram showing A) Laramide fa u lt geometry, B) extensional post-Laramide reverse drag forming a lis tr ic normal fa u lt, and C) deposition and downwarping of post-Middle Miocene sediments. Rock units: 1) Precambrian Belt Supergroup; 2) Paleozoic-Mesozoic rocks; 3) pre-Middle Miocene Cenozoic rocks; 4) post- Middle Miocene Cenozoic rocks. (Modified from Hamblin, 1965.)

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CJl to

Mz rocks Belt rocks Belt Belt rocks Rock units:Rock Ts - Tertiary rocks; Mz - Mesozoic rocks; Pz - Paleozoic rocks. thrust faulting and post-Laramide normal faulting in the Smith River Valley. Belt rocks Fiqure Fiqure 15. Generalized block the diagram showing possible relationship between Laramide

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Description of Faulting

Much of the post-Laramide structural character of the Smith

River Valley has been obscured by allu vial processes; consequently,

the existence of normal faulting in the area (Plate 1) has been

inferred primarily on the basis of well data, aerial photographs,

mapping Tertiary sediments, and gravity studies (Gogas, 1984; and

this paper).

Earlier work relating the Smith River Valley to normal faulting

has been minimal. Koerner (1939) was the first to recognize that

some normal faults in the area apparently follow previous zones of

displacement. Pardee (1950) and Wolfe (1964) studied the deposition

of Tertiary sediments in the Smith River Valley, but considered the

valley to be a downwarped basin that was not associated with normal

faulting. Birkholz (1967) mapped normal faults on the western margin

of the valley but did not relate these features to basin development.

Reynolds (1979) was the firs t to interpret the Smith River Valley as

a graben. He mapped normal faults and Tertiary strata in the valley,

and documented an offset of 1000 f t (305 m) for Lower Miocene lake

beds that are found on the flanks of the Big Belt Mountains in White

Sulphur Springs.

Normal faults in the area generally trend north, northwest, and

northeast. These different fa u lt trends combine to form a rhombic or

zigzag pattern of faulting along the eastern margin of the Smith

River Valley.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. White Sulphur Springs Basin-Bounding Fault System

Gravity data (Gogas, 1984; this paper) and well log data in di

cate that a north-trending normal fa u lt passes through the western

margin of White Sulphur Springs. This fa u lt is responsible for the

discharge of thermal waters in town and w ill therefore be referred

to as the White Sulphur Springs fa u lt. The presence of this fau lt

and its association with thermal a c tiv ity in town was fir s t recog

nized by Reynolds (1979). The fault trace is interpreted to merge

with that of the northwest-trending Moors Mountain thrust approxi

mately 2 miles (3.2 km) north of town (see Plate 1). The southern

extent of the fault is open to interpretation as it is covered by

Tertiary and alluvial sediments. Well log data are interpreted to

suggest the fau lt passes through section 30, T.9N., R.7E., and may

be continuous with the normal faults that cut the northwest hinge of

Cottonwood Creek syncline to the south. The well log data includes

the Bailey well (NW?s, sec. 29, T.9N., R.7E.) which penetrated Belt

shale at 125 f t (38 m), and the Hanson well (SE%, sec. 24, T.9N.,

R.6E.) one mile to the northwest which was completed in Tertiary

sediments at a depth of 300 f t .

Because the fault is not exposed, a determination of dip and

stratigraphic separation could not be made from fie ld evidence.

Gravity data (Plate 3) suggest the fa u lt dips steeply (65°-85°) to

the west. Minor synthetic faults may be associated with the major

basin-bounding fa u lt. Evidence supporting synthetic faults includes

the presence of moderately thick (>200 f t in places) Tertiary

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 56

sediments such as Clay Butte, and associated gravity lows that are

east of the main fau lt (see Plates 1 and 3). In the southern portion

of the map area, minor synthetic faults have been inferred on the

basis of aerial photograph interpretation, although the faults are

virtually indistinguishable in the field.

Northwest-trending normal faults in the White Sulphur Springs

area are apparently reactivated Laramide thrust faults that have

exhibited reverse drag movement. The Moors Mountain thrust fa u lt

displays recurrent normal movement northeast of section 36, T.9N.,

R.7E. East of section 36 normal movement appears to be along a foot-

wall splay associated with the Moors Mountain thrust system. The

fresh fa u lt scarps, marked change in topography, younger on older

relationship of minor fault splays, and the sharp outline of Tertiary

sediments associated with the faults is good evidence to support

recurrent normal movement along these thrusts.

An inferred north-northwest-trending normal fault in the

southern portion of the map area (Plate 1) has been interpreted to

be a reactivated portion of the Horse Butte thrust zone. This fault

is very apparent near Catlin Spring as one can clearly see that the

spring's source is associated with the normal fault. The reactivated

portion of this footwall splay changes trend to the northeast,

cutting the northwest limb of the Cottonwood Creek syncline to the

north, and truncating the Horse Butte thrust zone to the south. This

change in trend produces a rhombic pattern of normal faulting in the

southern portion of the map area. Gravity data (Gogas, 1984; this

paper, Plate 3) suggest that a similar pattern may exist with the

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 57

White Sulphur Springs fa u lt ju st south of town. A sharp deviation

in gravity contours (Plate 3) near the southern margin of town

suggests that the White Sulphur Springs fa u lt may change its trend

from north to northeast for a short distance. These different trends

may represent the interaction between regional east-west extension

and previously established compressional zones of weakness.

Various trends or patterns exhibited by normal faults in the

area appear to be related to reactivation along the following thrusts

or thrust-related features:

1. The northwest-trending normal fa u lt segments may be associ

ated with reactivation along the Moors Mountain and Horse Butte

thrusts, and along the rejoining splay segments of the Craig and

Moors Mountain thrusts.

2. Northeast-trending normal fault segments (i.e ., at Cat!in

Spring) may follow cross-strike or transverse features that

were transverse tear structures during thrusting and were later

reactivated by normal faulting.

3. North-northeast trending normal fa u lt segments, such as

the White Sulphur Springs fa u lt, may be following ramps in the thrust

sheets. The White Sulphur Springs normal fa u lt may follow the ramp

of the Pinchout Creek thrust (Figure 11, sequence (•).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER IV

RECONNAISSANCE GRAVITY SURVEY

Objective

The reconnaissance gravity survey was intended to provide a

balanced exploration strategy for thermal a c tiv ity in the White

Sulphur Springs region. The principal goal of the survey was to

identify structural features that may control hydrothermal circula

tion systems in the Smith River Valley, in particular, the geometry

of the valley and associated basin-bounding fau lts. This survey was

done without the knowledge of a more detailed gravity study of the

same area by Gogas (1984); therefore, an overview of this survey w ill

be done with frequent comparisons and references to the study by

Gogas (1984).

Data Acquisition and Processing

In August 1982, eighty-three gravity stations (stns. 42-124 in

Appendix C) were established by the author in the vicinity of White

Sulphur Springs, Montana (Plate 3). These stations complemented 41

gravity stations that were previously established (summer, 1981) by

Michael Stickney of the Montana Bureau of Mines and Geology (Appendix

C). Gravity readings at stations 1-41 were done with a Worden

Educator model gravimeter [dial constant .4017(8) m gals/div.], and

stations 42-124 were done with a Worden model 944 gravimeter [dial

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. constant .0970(6) mgals/div.]. Gravity data for stations 1-124 are

listed in Appendix C and will be referred to as the data.

Data reduction was performed by using program GRVRED, a reduction

program written by Dr. William Sauck of Western Michigan University to

calculate Bouguer anomaly values. The density used was 2.67 g/cm3 and

sea level was used as the datum. Base station readings were not tied

into a station of known gravity; therefore, an arbitrary observed

gravity of 980,484.00 mgals was chosen for base station 1 to achieve

positive Bouguer values with program GRVRED. The Bouguer anomaly con

tour map (Plate 3) shows relative changes in Bouguer gravity with

respect to the observed gravity chosen for base 1. All latitudes and

elevations were obtained from U.S. Geological Survey quadrangle maps

on a scale of 1:24,000. Terrain corrections were not applied because

the survey was primarily confined to the fla t-ly in g valley.

A contour map of residual gravity indicated that residual values

were biased because of an insufficient grid density; therefore, the

contour map was not included. Residual values were computed by using

program F0RFIT (Ghatge, 1984), a modified version of a double Fourier

fittin g program written by James (1966). The program uses the least-

squares method for calculating coefficients of the Fourier series.

Interpretation of the Bouguer Anomaly Map

Contours of relative Bouguer values (Plate 3) depicts the general

geometry of major structural features in the White Sulphur Springs

area. As expected, this map is very similar to the Bouguer gravity

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 60

map by Gogas (1984). The map suggests that the Smith River Valley

is a northwest-trending fault-bounded basin with its depositional

axis approximately .7 mi southwest of White Sulphur Springs. Modeling

of Bouguer profiles by Gogas (1984) suggests the maximum basin depth

is approximately 2000 f t (610 m) southwest of town; however, modeling

of Bouguer values may not yield accurate results. Also, the Hanson

well (NEJs, NE%, sec. 9, T.9N., R.6E.) d rille d near the basin's axis

reportedly hit bedrock at approximately 1100 ft (335 m) (Groff, 1965)

suggesting that the basin's depth may not be as great as 2000 f t .

The eastern margin of the basin is identified by a steep gradi

ent of over 8 mgals/mi near the town of White Sulphur Springs. The

sharp gradient indicates significant vertical displacement associated

with the steeply dipping White Sulphur Springs fa u lt. This fa u lt has

a northerly trend through the town but may change in trend to northeast

near the southern margin of town. This change in trend would account

for the pronounced northeast-trending gravity high ridge located in

town.

The western margin of the Smith River basin appears to be bounded

by a steeply dipping fa u lt that is antithetic to the White Sulphur

Springs fa u lt. This fa u lt changes trend from northwest to northeast

in the SW^s of section 23, T.9N., R.6E. where i t bounds a basin that

is a southern extension of the Smith River Valley. A northwest-

trending gravity high located near the White Sulphur Springs airport

may represent a horst that divides the Smith River Valley into what

Gogas (1984) calls the northern and southern basins. Gogas (1984)

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. interprets the maximum depth of the southern basin to be approxi

mately 2000 f t (610 m). The southern basin may owe its origin to

recurrent normal movement along the Horse Butte thrust whereas the

northern basin may be related to normal movement along the Pinchout

Creek and Moors Mountain thrusts (see Figure 11).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER V

HYDROGEOLOGY

General Statement

In order to delineate and define the geothermal potential of an

area, its hydrologic characteristics must be understood. Mixing o f

thermal waters with shallow cold ground water w ill dilute thermal

brines and transport the plume downgradient in shallow aquifers.

The plume w ill have a chemical composition and thermal expression

that generally ranges between that of warm thermal brines and cold

meteoric ground water. When using geothermal indicators and existing

shallow water wells to identify the thermal potential of an area, the

mixing and transport of thermal waters downgradient within shallow

aquifers may create an erroneous area of thermal potential; there

fore, a hydrologic study of the area should be made in conjunction

with well-water inventories and water-sampling programs designed for

geothermal exploration.

Drainage

Regional drainage of the White Sulphur Springs area is through

the northerly flowing Smith River and its major tribu taries. Local

drainage near White Sulphur Springs is controlled by the southwest

flowing North Fork of the Smith River which drains into the Smith

River 3.4 mi (5.5 km) west of town. The North Fork and the main

with permission of the copyright owner. Further reproduction prohibited without permission. 63

course of the Smith River are gently meandering and have gradients of

approximately 34 ft/mi and 13 ft/mi in the valley respectively. The

Smith River Valley is a "graben-like" feature that has a gentle slope

to the west, toward the Smith River. Many small drainage systems

near the margins of the valley are caused by spring-fed and inter

m ittent streams that have dissected Belt Supergroup and Tertiary

rocks.

Aquifers

Aquifers in the area exist mainly in Quaternary alluvium and

Tertiary sedimentary rocks, although many rock units (e .g ., Mission

Canyon Limestone) in the area are potential aquifers. Quaternary

sand and gravel is the main source of ground water in the Smith River

Valley as i t provides better quality water, and wells in these mate

rials have greater specific yields than most Tertiary and older rocks.

Quaternary gravel aquifers are generally present within 40 f t (12.1 m)

of the surface, although they are la te ra lly discontinuous and may be

interbedded with clays and s ilts (Appendix D). West of White Sulphur

Springs near the Smith River, Quaternary gravel aquifers may be

present at least 150 ft (45.4 m) below the surface; however, well

data indicate that below 40 f t (12.1 m), the valley f i l l consists of

Tertiary claystone and tuffaceous siltstone.

Tertiary stream channel deposits penetrated near the base of

many wells (Appendix D) may yield large quantities of water. Wells

with high yields in Tertiary stream bed deposits are generally deep,

such as the Hanson well (previously Shearer w ell) located in SE^ SE%

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 64

SE% sec. 24, T.9N., R.6E. which has a pumping rate of 1200 gpm and

is perforated at various intervals in Tertiary gravels to 220 ft

(67 m); and the Townsend well (SWls SE% sec. 26, T.9N., R.6E.) which

has a yield of 1850 gpm and is perforated to 250 ft (76 m) in

Tertiary conglomerate and claystone. In the Smith River Valley,

Tertiary channel deposits may be cemented by calcite and are la te r

a lly discontinuous in comparison to Quaternary gravels (Appendix D).

A Tertiary stream channel lith ic conglomerate interbedded with water-

laid tuffs is exposed in a roadcut 2 miles east of town. This

exposure exhibits calcite cementing in Tertiary gravels.

Bedrock aquifers are not widely used as a source of water in

the area, although many Castle Mountain Ranch Wells northeast of town

draw water from Paleozoic limestones. Paleozoic carbonates,

especially the Mississippian Mission Canyon Limestone, act as

recharge areas for springs such as T rin ity and Catlin Springs which

discharge from fau lt zones. Paleozoic rocks, especially the Mission

Canyon Limestone, are present in the footwalls of thrust zones north

and northeast of town, and may act as recharge areas that transmit

water to and along thrust faults that dip beneath the valley. A

good example of the Mission Canyon Limestone's a b ility to transmit

water is the Ringling petroleum test well 15 mi southeast of White

Sulphur Springs. The well is completed in the Mission Canyon and

discharges warm water (48° C) under artesian flow at a rate of

800 gpm.

Much of the valley floor is composed of Belt rocks that have low

hydraulic conductivities and, where unfractured, have extremely low

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 65

permeabilities. Belt shales and limestones may transmit and yield

significant volumes of water if highly fractured. Sandstones inter

bedded with the Greyson Shale and Newland Limestone may yield minor

amounts of water, but extensive fracturing must be present for them

to produce large volumes. A good example of a high yield well in

fractured sandstone and shale within the Greyson Shale is the thermal

bank well. A pump test of the bank well gave a calculated transmis-

s ib ility of 103,000 gallons per-day-per-foot and an estimated safe

yield of 50 gpm on a continuous basis (Sonderegger & Bergantino,

1981).

Ground Water Hydrology

The water table map of the White Sulphur Springs area (Plate 4)

indicates that the local ground-water-flow direction is to the west-

southwest. Minor variations in the flow direction and the hydraulic

gradient are mainly related to changes in topography; however, the

drawdown effects from pumping, lateral variations in permeability,

and the depth to bedrock may contribute to such variations. In the

vicinity of White Sulphur Springs, a sharp increase in hydraulic

gradient and deviation in ground-water-flow direction is related to

the following factors: (a) the sharp change in the depth to bedrock

which ranges from less than 75 f t (23 m) in the eastern half of town

to over 1200 ft (366 m) in the valley west of town; (b) the contrast

in permeability between clay rich Tertiary rocks in the eastern por

tion of town to Quaternary gravels west of town; and (c) the presence

of a topographic high in the eastern h alf of White Sulphur Springs.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 66

All of these factors are related to the north-trending normal fault

which transects the town of White Sulphur Springs (Plate 1).

An approximate value for the hydraulic gradient in the valley is

5.21 x 10"3 ft/ft. This value was calculated from the distance

between the 4900 foot and 5020 foot contour intervals in Plate 4 and

is considered to be an approximation of the mean gradient for the

area.

Ground-water flow velocities can be estimated with the use of

hydraulic gradients (Plate 4) and representative hydraulic conduc

tiv itie s and porosities of Quaternary and Tertiary sediments.

Because aquifers in the area exhibit an extremely wide range of

hydraulic conductivities, effective porosities and hydraulic gradi

ents, this thesis w ill not attempt to estimate ground-water flow

velocities considering the data available.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER VI

GEOCHEMICAL SURVEY

Objectives and Procedures

The water-chemistry program was undertaken to f u l f i l l two objec

tives: (1) to aid in the delineation and assessment of thermal

resources in the White Sulphur Springs area by the use of chemical

indicators, and (2) to estimate the reservoir temperature of the

geothermal system using geothermometers.

Twenty-six water samples were collected from wells in the area.

Two of the samples were from wells developed for hydrothermal use

(see Plate 4 ). Three 250 ml samples were collected at each well:

one untreated sample to be kept chilled, one filtered (.45y filte r)

sample kept ch illed, and one sample filte re d and acidified with

nitric acid. All plastic storage bottles, caps, and filtering

equipment were rinsed three times with sampled water (filte re d or

unfiltered) to help prevent cross-contamination. I f pressure tanks

were present, the pumping rate was measured and the well was pumped

for a sufficient period of time to insure a representative sample.

Field data collected at most stations included measurements of water

temperature, pH, specific conductance, and static water level. All

water samples were analyzed by the Montana Bureau of Mines and Geology

lab and the results are listed in Appendix E (pp. 111-141).

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 68

Isoconcentration maps (Plates 6 and 7) of specific conductance

and fluoride were constructed in hopes of delineating thermal waters

or possible areas of hydrothermal discharge. Because the concentra

tions of most parameters increased exponentially from shallow meteoric

to thermal flu id s , a logarithmic contour interval was used. The

contour interval was derived using the following formula:

1ogA = x(0,l,2,3,4,...,x) or A = log_1 x(0,l,2,3 x)

where x equals the intervals per decade.

Water Chemistry

Chemical analyses of thermal, meteoric, and meteoric-thermally

contaminated well waters are summarized in Table 1. The analyses

show that thermal waters have significantly higher concentrations

of Na+, K+, Cl", HC03“ , S042", F", B3+, Li+, Sr2+, and TDS than

shallow meteoric waters. The only parameters that generally have

lower concentrations in thermal waters are As3+ and Mg2+.

Evaluation of the bank thermal water analysis (Sonderegger, 1981)

indicates that the water is supersaturated with respect to c a lc ite ,

pyrite, flu o rite , chalcedony, and quartz [log (IAP/KT) values of 0.92,

9.53, 0.25, 0.17, and 0.57]. Analysis of the Spa Motel thermal spring

waters (Mariner et a l ., 1976) gave sim ilar results, with the excep

tion of calcite, which was undersaturated in the spring water [log

(IAP/KT) = -0.33]. An equivalent Eh of -0.302 volts and a sulfide

concentration of 2.5 mg/1 for the bank well suggest the thermal

waters are very reducing. Pyrite penetrated in fracture zones during

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. O') t o 1.5 0.16 0 0.001 0.12 0.15 3.2 0.15 2.5 0 9.2 STD 13.3 86.8 26.3 16.7 17.8 73.3 114.6 deviation

.30 .02 .39 7.75 <•002 9.7 3.4 4.2 0 14.7 15.7 32.3 15.3 38.3 56.7 Mean 476.5 404.3 225.1 6.7 6.7 - m 76.2 Range Shallow Meteoric Well Waters0 Well Meteoric Shallow .11 - .52 .11 5.2 - 40.2 5.2 - 0.8 8.9 15.9 - 60.9 15.9 252.6 - 650.3 252.6 229.6 - 541.0 229.6 .02 - .005 <.002 .95 - .76 .19 2.5 - 6.0 11.7 0.7 - 7.99 7.37 7.7 - 8.5 0.3 0.5 7.9 - 22.6 8.6 7.4

75.2 - 50.4 2.5 25.9 0 27 87 STD 101.5 - 120 10.7 522.7 deviation -.01 2.2 2.4 0 8.1 0.56 0.9 9.7 11.9 11.1 11.9 13.0 66.1 57.3 57.6 42.4 - 87.4 26.1 76.2 m 76.2 114.2 791.1 246.3 146.3 362.3 58.3 - 358 118 1042 33.5

Shallow Meteoric Well Water Well Meteoric Shallow 0 - 0 51.8 Range Mean With Thermal-Brine Contamination1* Thermal-Brine With 0.9 - 0.9 18.3 19.0 - 79.7 19.0 728.4 - 1824 728.4 Table 1 Table

.62 - 1.19 .017 8.63 - 9.20 7.67 2.5 - 101 1.7 25.2 - 5.62 0.39 44 Jordon® 026 WSS 7878 2533 - 445 317 53.4 m TD m 53.4

.24 2.02 - .043 <.002 7.23 7.07 7.7 - 2.28 0.14 9.5 3.4 - 0.5 18.5 47.5 15.3 - 9.0 15.0 17.4 19.0 47.9 41.7 186 827 - 9.5 177 806 Motel Shallow 2370.1 WSS 009 WSS flowing well flowing Thermal Well Thermal Partial Mixing Water Mixing Partial

Chemical Analyses of Ground Water From Uells in the White Sulphur Springs Area, Montana Area, Springs Sulphur White the in Uells From Water Ground of Analyses Chemical 1.84 1.97 7.9 8.2 6.3 0 0 86.4 43.7 791 Bank 1700.2 1817.8 6985.6 - 1157.5 630.9 2169 Screened WSS BANK WSS 27.4-103.4 m 27.4-103.4 ) 3 )

3 The four meteoric-thermally mixed domestic water wells were separated on the basis of isoconcentration maps (Plates 6-7) and chemical analysis chemical and 6-7) (Plates maps isoconcentration of basis the on separated were wells water domestic mixed meteoric-thermally four The data (Appendix E). The four wells include sample numbers WSS 010, 018, 022, and 025. and 022, 018, 010, WSS numbers sample include wells four E). The (Appendix data Field Water Temp. °C Temp. Water Field 43.3 c19 wells represented. wells c19 Lab pHLab 7.82 Lithium (Li) mg/1 (Li) Lithium 1.15 ?The Jordon well (WSS-026) was intended for domestic use. domestic for intended was (WSS-026) well Jordon ?The Strontium (Sr) mg/1 (Sr) Strontium - Lab mhos/cm TDS Cond. Spec. Lab Well Depths Well Fluoride (F) Fluoride mq/1 (B) Boron Parameter Sulfate (SOOSulfate 211 253 1332 - 264 39.1 Chloride (Cl)Chloride 147 Arsenic (As) ug/1 (As) Arsenic <■1 1.5 11.8 - 6.2 22.6 Potassium (K)Potassium (CO Carbonate 17.5 Bicarbonate (HCO Bicarbonate Anions - mo/1 Anions Silica (Si02) Silica (Ca) Calcium (Mg)Magnesium 41.0 9.5 Cations - mq/1 Cations (Na)Sodium 433 449 2130 - 250 51.3

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 70 d rillin g of the thermal bank well (Dunn, 1978) (TD-273 m) also

indicates reducing conditions and the supersaturation of pyrite in

these thermal waters.

The dominant cation present in the thermal waters is Na+, which

comprises more than 80% (in equivalents) of the total cations whereas

Ca2+ is the dominant cation in shallow meteoric waters. Sodium is

generally the second most abundant cation in shallow well waters

completed in Tertiary sediments, and Mg2+ is the second most abundant

cation in well water pumped from Quaternary gravel and sand. Other

elements that appear to have higher concentrations in Tertiary,

rather than Quaternary aquifers, include As3+, K+, F", and Sr2+.

Higher concentrations of these elements are expected in Tertiary

sediments because these sediments are mainly composed of volcanic

ash and water-laid tuffs.

The dominant anion species in both thermal and shallow water

wells is HC03“ which constitutes over 50% of the total anions (in

equivalents) for most well water sampled. The high concentrations of

HC03” and Mg2+ in'well waters suggest dissolution of carbonate rocks.

Therefore, meteoric and possibly thermal ground-water recharge areas

are in carbonate terranes, or carbonate dissolution occurs in

aquifers containing carbonate clasts or cement.

Water from the Jordan well (Appendix E, p. 137) has an extremely

high Na+ content (2130 mg/1) which constitutes over 99% of the total

cations (in equivalents). The anomalously high observed temperature

(15.3° C), brine-rich composition, and low Mg2+ content (3.5 mg/1)

suggest that the Jordon well water represents a cooled thermal water

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 71

with minor dilution. If the Jordon well water is chemically repre

sentative of the thermal reservoir, the bank and Spa Motel well

waters comprise approximately 20%-25%> thermal water, with the

remaining component being cold meteoric water.

Some mixing of thermal and meteoric waters obviously occurs in

shallow aquifers. Evidence that supports shallow mixing includes the

increase in discharge temperature of the White Sulphur spring (~21° F)

when a cement culvert (shallow dug well) was installed for the Spa

Motel. Mixing at some intermediate depth is likely for the Spa Motel

and bank well waters because they are nearly identical in chemical

composition even though the bank well was completed in Greyson Shale

(screened 27-104 m) and the Spa Motel well is in the top few feet of

alluvium. These thermal waters are relativ ely dilute in comparison

to the Jordon w ell, indicating a large mixing factor. This mixing

may be caused by cold meteoric water moving through fractures related

to the thrust zone north of town intersecting and mixing with thermal

waters that ascend along the north-trending normal fa u lt.

Progressive leaching of Tertiary sediments by thermal fluids

could explain the brine-rich composition of the Jordon w ell; however,

water analyses of cold meteoric waters indicate that the chemical

difference between waters from Tertiary sediments and those from

Quaternary alluvium is small; therefore, the differences in thermal

water chemistry may be attributed to various degrees of mixing. The

possibility of the Jordon thermal waters being derived from a sepa

rate, intermediate brine-rich reservoir within Tertiary sediments

may be another explanation.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Isoconcentration maps (Plate 6 and 7) indicate that thermal

waters discharge along a north-south-trending zone associated with

the White Sulphur Springs fa u lt. The length of the discharge area is

less than a kilometer as thermal fluids move la te ra lly down-gradient

and are diluted by cold meteoric ground water. This meteoric-thermal

brine mixture produces a plume of water that has a chemical composi

tion between that of background meteoric and thermal water (Plates 6

and 7), with the exception of As and Mg, which generally have higher

concentrations in the plume consisting of a meteoric ground water-

thermal brine mixture (see Table 1). A re s is tiv ity low caused by the

brine-rich contaminant plume can be identified as fa r west as the

King Wilson sportman's lodge (Poor Farm) in the NW% of section 13,

T.9N., R.6E. (Sonderegger, personal communication, 1983). Analysis

of the Wilson well (sample #WSS018, p. 129) shows high concentrations

of Na+, B3+, and As3+, which confirms the mixing of thermal waters in

the area. The areal extent of the plume caused by the ground-water

transport of thermal brine to the west-southwest is identified by

chemical isoconcentration maps (Plates 6 and 7). The westerly direc

tion of contaminant movement shown by the maps correlates well with

the west-southwest flow direction derived from the potentiometric

surface map (Plate 4). I t is important to note that some thermal

fluids may move through lower confined aquifers in the T ertiary, and

may not effectively mix with the shallow unconfined Quaternary gravel

aquifer from which many wells were sampled.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Geochemical Thermometers

Dissolved s ilic a and Na-K-Ca geothermometers are useful tools

for determining the reservoir or base temperature of low to inter

mediate temperature hydrothermal systems. Calculated reservoir

temperatures and related analytical data for thermal waters in the

White Sulphur Springs area are listed in Table 2. Temperatures were

calculated using the following chemical thermometers and equations

(Fournier, 1981):

Temperature Geothermometer Restriction

Quartz no steam loss

t = 0 - 250° C

Na-K-Ca

1647 t °C = t< 100° C, B = | 1 og (Na/K) + g[log(/Ca/Na) + 2.06] + 2.47 t>100°C, B = j - 273.15

where C is concentration in mg/kg.

These geothermometers are accurate only when certain conditions

are met. Factors that must be considered when using the s ilic a geo

thermometer were discussed in detail by Fournier (1981) and include

the following: (a) Temperature restrictions must be met; (b) chemi

cal equilibrium must be established i f mixing has occurred, otherwise

calculated quartz temperatures w ill be low; (c) possible

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Mg 9.5 Ca Ca K Na concentrations mg/l 43.7 433 41.0 17.5 Silica Si02 R Dissolved 23.8 Na-K-Ca Mg-Corr. Table 2 (B=l/3) Na-K-Ca 99.8 143.4 73.4 23.6 47.9 449 41.7 17.4 9.5 95.6 144.9 72.0 Temperature Quartz Quartz no no loss steam in White Sulphur Springs (W.S.S.), Montana 15.3 95.9 122.5 53.5 31.5 44.0 2130 2.5 19.0 3.4 47.5 43.3 Observed Name Owner or Owner Ralph Jordon Sulphur Sulphur Springs - Motel Spa National Bank-W.S.S. White White No. Sample Where = R Mg/(K + + Where Ca Mg) * 100, with concentrations in equivalents (see Figure 16 for correction).Mg WSS-026 WSS-009 WSS-Bank F irst < < Calculated Reservoir and Temperatures Analytical Data for Thermal Well Waters

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. polymerization or precipitation of silica may occur before sample

collection; (d) polymerization of silica may occur after sample

collection due to improper sample preservation; (e) the effects of

steam separation must be considered—not a factor for low temperature

systems; (f) the effect of pH on quartz so lu b ility must be con

sidered; (g) the control of aqueous silica by solids other than

quartz must be considered; and (h) water-rock reactions of thermal

and mixing fluids with s ilic a -ric h fine-grained rocks causing s ilic a

enrichment must also be considered.

The following factors should be considered when using the

Na-K-Ca geothermometer (Fournier, 1981): (a) The loss of aqueous

Ca2+ may occur as a result of boiling—not a factor for low tempera

ture systems, although calcite can precipitate i f there is a rapid

loss in C02 associated with a reduction in hydrostatic head (i.e .,

near a ground-water discharge point); (b) erroneous results may occur

when the equation is applied to Mg2+-rich waters; (c) low calculated

values may result when Mg corrections are applied to thermal waters

that gained Mg2+ during ascension; and (d) mixing or dilution

corrections should be applied for waters with a thermal component

less than 20%-30%.

Calculated s ilic a reservoir temperatures (Table 2) for the three

thermal wells in the area range from 95.6° C to 99.8° C. These cal

culated temperatures are probably high as thermal waters are super

saturated with respect to quartz, and the mixing of s ilic a-ric h

meteoric waters may cause s ilic a enrichment. The mean s ilic a concen

tration for water from 19 wells producing cold meteoric water is

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 38.3 mg/1 (Table 1). This concentration yields a quartz reservoir

temperature of 89.8° C even though the 19 wells had a mean observed

temperature of 9.7° C. The supersaturation of silica in cold

meteoric and possibly thermal waters may be attributed to the disso

lution of fine grained silica-rich Tertiary ash deposits.

The Na-K-Ca geothermometers gave a temperature range of 122.5° C

for the Jordon well and 144.9° C for the bank well (Table 2). These

temperatures are higher than the actual reservoir temperature because

Mg2+ concentrations are elevated due to the mixing of thermal and

cold meteoric water. When Mg2+ corrections are applied (Figure 16),

the calculated reservoir temperatures are significantly lowered and

range from 53.5° C for the Jordon well to 73.4° C for the Spa Motel

w ell. The 72.0° C and 73.4° C Na-K-Ca-Mg temperatures for the bank

and Spa Motel wells correlate well with the 73° C chalcedony tempera

ture derived for the bank well (Sonderegger, personal communication,

1984); however, the thermal waters are slig h tly supersaturated with

respect to chalcedony, suggesting that the calculated temperature

may be high. The 53.5° C Na-K-Ca-Mg temperature calculated for the

Jordon well is very sim ilar to the 52° C A 180(S0i+ - H2O) temperature

(Sonderegger, personal communication, 1984) derived fo r the bank

w ell. Both of these temperatures appear to be lower than the actual

reservoir temperature. The 52° C A180(S0i* - H20) temperature is

obviously low as the maximum observed discharge temperature for the

spring was 58° C (Sonderegger & Schmidt, 1981). The Mg2+ corrected

temperature (53.5° C) for the Jordon well may be adjusted too far

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 77

>00

too

100

100 too 3 0 0 No-K-Co CALCULATED TEMPERATURE (°C)

Figure 16. Graph for estimating magnesium correction temperature (AtMg) to be subtracted from the Na-K-Ca calculated reservoir temperature. R = 100 Mg/(Mg + Ca + K) in equivalents. (From Fournier & Potter, 1979.)

downward as the low Mg2+ concentration (3.4 mg/1) and high TDS value

(6986 mg/1) suggest mixing may be minor.

The wide range of calculated reservoir temperatures [A^OfSOq. -

H20 ), 52° C; Na-K-Ca-Mg, 53.5°, 72.0°, and 73.4° C; Chalcedony, 73° C;

Quartz, 95.6-99.8° C], indicate that the thermal waters do not reach

equilibrium at depth, and that variable degrees of mixing do occur.

Considering the calculated reservoir temperatures and the chemical

characteristics of the thermal waters, an estimated reservoir tempera

ture of 72° C ± 10° C seems reasonable. Previously estimated base

temperatures of 150° C (Renner et a !., 1975) and 125° C (Sonderegger

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 78

& Bergantino, 1981; Sonderegger & Schmidt, 1981) appear to be

optim istically high. The reservoir temperature estimate of Renner

et a l. (1975) was based on chemical thermometer temperatures of

103° G and 148° C for quartz and Na-K-Ca. The 150° C reservoir

temperature was based on the assumption that most geochemical ther

mometers provide minimal estimates of subsurface temperatures. No

magnesium corrections were applied fo r the 148° C Na-K-Ca

temperature.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER VII

WHITE SULPHUR SPRINGS HYDROTHERMAL SYSTEM

General Statement

To determine the geothermal potential of an area, the character

istics that govern the hydrothermal system must be understood. These

characteristics include the reservoir temperature, heat sources, and

the structural and lithologic controls of the circulation system.

The characteristics of the White Sulphur Springs hydrothermal system

w ill be discussed in hopes of determining potential areas fo r future

geothermal development.

Thermal Gradient and Heat Source

According to Chadwick and Kaczmarek (1975), the normal geo

thermal gradient for western Montana is 1° C/100 f t (32.8° C/km).

The AAPG geothermal gradient map of Montana (Kehle, 1972) indicates

that the White Sulphur Springs region has a thermal gradient of

1.56° C/100 f t (51.2° C/km); however, the r e lia b ility of this value

is low as the data control for this area was poor. The Ringling well

(TD 2320 f t ) , 15 mi southeast of White Sulphur Springs, produces warm

water at a flow rate of 800 gpm at a temperature of 48° C. Assuming

a mean annual ambient temperature of 8° C, a thermal gradient of

1.7° C/100 f t (56.6° C/km) can be calculated for the area. This is a

conservative estimate as the w ell's discharge temperature may not be

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 80

representative of the well's base temperature, and therefore, should

be considered the minimum reservoir temperature. The Ringling well

penetrated mainly Paleozoic carbonates and Mesozoic sandstones which

had a thin (<3Q m) Tertiary cover. The presence of a thicker (~610 m)

thermally nonconductive (estimated K = 2 meal/cm s °C) Tertiary

blanket overlying the thick (~1220 m) Precambrian Greyson Shale

(estimated K = 4 meal/cm s °C) in the Smith River basin suggests that

the thermal gradient in the valley is much greater than that calcu

lated for the Ringling w ell, perhaps ranging from 2.0°-2.4° C/100 f t

(66°-79° C/km). Anomalous gradients within this range are commonly

present in basins of western Montana (Kehle, 1972).

Regional heat flow in the White Sulphur Springs area is approxi

mately 65-71 m illiwatts/m 2 or 1.1-1.2 HFU (Grim, Berry, Ikelman,

Jackson, & Smith, 1979) although low conductivity Tertiary clays and

Precambrian shales should create anomalous heat flow in the Smith

River Valley. The temperature difference caused by low conductivity

strata in the valley can be illustrated by calculating the change in

temperature ( a T) between the low conductivity blanket and a higher

background conductivity by using the formula (Diment et a l., 1975):

AT = q[(K! - K2)/(K x x K2)]Z

where q is heat flow, estimated to be approximately 1.4 HFU in the

Smith River Valley, Ki and K2 are the conductivities of each blanket

or layer, and Z is the thickness of the low conductivity blanket

(estimated to be -1.83 km). A conductivity of 3.3 mcal/cm s °C was

derived for the low conductivity blanket (K2) by taking the weighted

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. mean of the previously mentioned estimated conductivities and thick

nesses of the Tertiary sediments and the Greyson Shale. A conduc

tiv it y of 6 mcal/cm s °C (Ki) was used for comparison because i t is

typical of igneous basement rocks (Diment et a l., 1975). When

inserting the estimated conductivities, heat flow, and thickness

values into the previous formula, a temperature difference of 35° C

is calculated when q = 1 .4 HFU (see Appendix A for conversion units)

and Z = 1.83 km. This temperature would be considerably higher i f

the high conductivity value represented thick Paleozoic carbonates

which bound the northern margin of the valley. Even though the

temperature derivation is somewhat arbitrary, it illustrates that the

thermal effect caused by low conductivity strata in the Smith River

Valley is significant.

The heat source of the White Sulphur Springs hydrothermal system

is not related to recent plutonic activity. The small size and Early

Eocene age of the Castle Mountain stock suggest remnant heat from the

intrusive is negligible. Basaltic volcanism in the area is Late

Oligocene in age (Chadwick, 1978) and is not a significant heat

source. High regional heat flow in the area is attributed to exten-

sional tectonism which may s t ill be locally active. Local anomalous

heat flow in the Smith River Valley is primarily related to thermally

nonconductive Tertiary clay and thick Precambrian Belt Supergroup

shale.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 82

Circulation System

Thermal a c tiv ity in the vic in ity of White Sulphur Springs is a

surface expression of a hot-water dominated hydrothermal convective

system. Considering an estimated thermal gradient fo r the area

(~65°-75° C/km), the shallow (~.6 km max.) basin depth (Gogas, 1984;

this paper), and the 72° C estimated reservoir temperature, the

circulation of thermal waters should be deeper than the bottom of the

basin (-1400-1600 f t ) . The generalized model of the White Sulphur

Springs convective hydrothermal system (Figure 17) indicates that

cold meteoric water descends along thrusts and fractures zones where

i t is heated by the anomalously high thermal gradient at depth. The

heated water ascends along the north-trending White Sulphur Springs

basin-bounding fa u lt. During ascension mixing occurs at intermediate

depths and also in near surface unconsolidated aquifers. Mixing of

thermal-meteoric waters at depth may be controlled by fracture zones

associated with the White Sulphur Springs fa u lt and the Pinchout

Creek thrust just north of town.

Some thermal water discharges as thermal springs (Spa Motel

flowing well) while much of the water appears to flow laterally

along permeable fracture zones and sandstones within the Greyson

Shale (Dunn, 1978). In some areas, thermal water may be prevented

from reaching near surface aquifers by Tertiary clay. This suggests

that intermediate thermal reservoirs may be present in Tertiary

bedded gravel deposits at depth. These reservoirs should have

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 00 CO

a £ hc I I I 111 U . w 1000 4 0 0 0 3000 -2000 •5000

Qal-, Qal-, NE indicates indicates water flow shows shows relative fault movement ^White Sulphur thermal spring 5 .9 — - - - _ _ p€g p€g - Shale; Greyson Precambrian p€s - Shale; Precambrian Spokane circulation system. units: Rock p€n - Limestone; Precambrian Newland Cf - Flathead Cambrian Sandstone; Ts - Tertiary sediments. Figure 17. Generalized diagrammatic sketch of the White Sulphur Springs hydrothermal - ~

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. different base temperatures and chemical compositions than water

that is controlled by faults.

Rapid ascension of thermal water is lik e ly because the discharge

rate of the Spa Motel well (in alluvium) is 350 gpm. Pressure that

drives the thermal system may be caused by the combination of head

produced by the thermal expansion of rising hot water, and the

hydraulic head caused by deep circulation of waters along a confined

aquifer (e.g., fault zone).

Controls on Recharge-Discharge

Relatively impermeable Belt Supergroup shale that encompasses

the area of thermal a c tiv ity in town suggests that recharge-discharge

patterns for the hydrothermal circulation system are structurally

controlled. Recharge for the hypothesized circulation system may be

predominantly controlled by thrust faulting in the area, although

water may be directed toward faults by permeable Paleozoic carbonates

which comprise footwall strata north and east of town. The carbonate

unit with the best aquifer characteristics is the Mission Canyon

Limestone. The Mission Canyon has paleokarst solution-breccia beds

(Figure 18) near its upper surface and forms footwall rocks along the

Moors Mountain thrust. The majority of water that is recharged

through Paleozoic carbonates appears to circulate down the Moors

Mountain thrust zone as the only major spring discharging from the

thrust zone is Trinity spring. The majority of the thrust zone is

topographically higher than streams in the area, indicating that

recharge dominates along this zone.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 85

Figure 18. Photograph of solution breccia in the upper member of the Mission Canyon Limestone. Northeast limb of the Willow Creek syncline, SW^, sec. 35, T.10N., R.7E.

The area of greatest recharge w ill occur where thrust faults are

covered by water saturated alluvium. Such an area is present north

and northeast of town where the Moors Mountain thrust zone and the

Pinchout Creek thrust are covered by allu vial sediments associated

with the North Fork of the Smith River; however, geologic cross

sections (Figure 11; Plate 2) suggest that a circulation system con

trolled by the Moors Mountain thrust zone should produce a reservoir

base temperature that is greater than those calculated for thermal

waters in town (Table 2). Therefore, the Pinchout Creek thrust and

an associated splay fa u lt may significantly control recharge for the

hydrothermal system (Figure 17). Solution development in the Newland

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Limestone may direct water toward the Pinchout Creek thrust north of

town; however, extensive solutioning in the Nev/land Limestone has not

been observed in the area. Other areas of possible recharge include

fractures associated with the White Sulphur Springs normal fa u lt and

joints that are in rocks of the Belt Supergroup. Lateral movement

of thermal water perpendicular to the White Sulphur Springs fa u lt

(i.e ., thermal bank well) indicates that fracture zones associated

with the fa u lt are extensive. This also suggests that recharge may

occur at higher elevations, north and south of White Sulphur Springs,

along the fa u lt zone. Recharge along jo in t sets in the Precambrian

Greyson Shale should be insignificant as jointing is extensive only

near the margin of the Castle stock.

As previously mentioned, the discharge of thermal waters is

along the north-trending White Sulphur Springs normal fa u lt. These

thermal waters mix with cool meteoric water to form a plume that is

transported downgradient to the west, along more permeable Quaternary

and Tertiary sands and gravels. The geologic controls that restrict

the discharge area to the immediate v ic in ity of town are open to

interpretation.

Gravity data by Gogas (1984) and this paper (Plate 3) suggest

that the White Sulphur Springs fa u lt may change its trend from north

to northeast near the southern margin of town. The fa u lt trends

northeast for a short distance (~1 mi) south of town and then returns

to a northerly trend. This change in trend could be a controlling

factor for the southern margin of thermal discharge, whereas the

Pinchout Creek thrust may control the northern margin of discharge.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. A water well that was reported to have encountered hot water in the

western half of section 12, T.9N., R.7E. (Ronald Jackson, personal

communication, 1981) suggests that thermal waters may discharge along

the Pinchout Creek thrust west of town. Unfortunately, the well was

not cased and was allowed to collapse.

The restriction of thermal waters to the v ic in ity of White

Sulphur Springs is apparently related to the variation in the depth

to bedrock caused by normal faulting. On the basis of well log data,

the depth to bedrock is generally less than 75 f t (23 m) under the

eastern h alf of town whereas bedrock is as deep as 2000 f t (610 m)

in the downdropped valley just west of town. Data from wells south

of town suggest that Tertiary sediments are more than 120 f t thick.

The presence of thicker Tertiary clay south of town may prevent

further ascension of thermal waters in this area.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER V III

THERMAL DEVELOPMENT

Present Development

Current geothermal use in the town of White Sulphur Springs

consists of the First National Bank and Spa Motel thermal wells. The

bank well supplies approximately 80% of the space heating required by

the bank (Sonderegger & Bergantino, 1981). The well is drilled in

Greyson Shale to a total depth of 273 m and is perforated from 27 m

to 103.7 m (Dunn, 1978). Pump test data suggest the well can produce

48° C water with an estimated safe yield of 50 gpm (Sonderegger &

Schmidt, 1981). Discharged warm water used by the bank is piped

across the street and is used in conjunction with the Spa Motel well

to heat a swimming pool and hot bath.

The Spa Motel well is a good example of a developed thermal

spring (White Sulphur spring). Development of the spring consisted of

the installation of a cement culvert (similar to a dug well) to

decrease shallow ground water mixing. After the well's installation,

the discharge temperature increased from approximately 46.1° C to

48° C with a flow rate of 350 gpm (Sonderegger & Schmidt, 1981).

Potential for Development

Development of hydrothermal resources in the White Sulphur

Springs area w ill be limited to space heating and recreational uses

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. due to the low temperature of thermal fluids (reservoir temperature

72° C±10° C). Plate 5 depicts an area where shallow ground water

temperatures may be suitable for heat pump use. A standard water

temperature of 10° C (Sonderegger & Schmidt, 1981) was used for the

cutoff for heat pump use. I t is important to note that Plate 5

shows water temperatures that were primarily measured from shallow

wells; therefore, the isothermal map cannot be d irectly related to

thermal potential at depth. Much of the area shown as suitable for

heat use (Plate 5) is highly suspect because of the following

factors: (a) Many wells measured were domestic wells with pressure

tanks, (b) water temperatures were primarily measured in July, and

sufficient quantities of ground water for development. Much of the

area east and southeast of town may not yield adequate volumes

because of the shallow depth to bedrock (Greyson Shale) and overlying

Tertiary clays. The low conductivity (hydraulically and thermally)

of strata east of town is the primary reason for s lig h tly above

normal water temperatures (10° - 12° C).

The area suitable for heat pump use just west and within the

town of White Sulphur Springs is related to the discharge of thermal

waters and their transport downgradient. Isoconcentration maps

(Plates 6 and 7) indicate that the area of thermal discharge is

restricted to the vicinity of town.

Potential for shallow thermal development—sim ilar in temper

ature (48° - 58° C) to the bank and Spa Motel wells—occurs in a

narrow north-trending zone that is controlled by the White Sulphur

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 90

Springs fa u lt. This zone extends approximately 1.5 km to the south

and less than a kilometer northwest of the bank well (see Plate 5).

Evidence supporting the southern extension of this zone includes high

water temperatures and concentrations of geothermal indicators found

in shallow water wells (see Plates 6 and 7). This zone may extend

further to the south as thicker Tertiary sediments overlying the White

Sulphur Springs fau lt may re s tric t the ascension of thermal waters.

Evidence of thermal a c tiv ity northwest of town is sparse. Wells

sampled in this area do not have anomalous chemical concentrations;

however, these wells are completed in shallow allu vial gravels near

Fox Creek and the North Fork of the Smith River suggesting chemical

indicators may not be useful. An unconfirmed report (Ronald Jackson,

personal communication, 1981) of a 200 f t water well which produced

warm water in the NW^, SW%, section 12, T.9N., R.6E. suggests

thermal potential may exist a short distance northwest o f town.

This well was supposedly abandoned and allowed to collapse because

i t was not suitable for domestic or stock use.

Intermediate thermal aquifers may exist in permeable Tertiary

stream bed gravels near the downdropped side of the White Sulphur

Springs fa u lt. Because Tertiary gravels are discontinuous in nature,

such reservoirs would be limited in extent. Thermal reservoirs

within Tertiary gravels may exist west and southwest of White Sulphur

Springs, but such reservoirs would probably be low in temperature

(15° C - 30° C) because of heat loss from dilution with cold ground

water. Also, Tertiary gravels are often confined aquifers that may

not have sufficient sustained yields.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. In summary, the potential for thermal development in the White

Sulphur Springs area is very limited in extent. The most promising

area for future development is along the White Sulphur Springs fa u lt

south of the bank and Spa Motel thermal wells. Deeper wells

(>200 f t ) d rille d near the downdropped margin of the fa u lt may

produce thermal waters in this area. The warm temperature (15.3° C)

and brine rich composition of the Jordon well suggest the area ju st

west of the high school is a potential zone for development; however,

utilization of corrosive waters similar in composition to the Jordon

well (TDS 6986 mg/1) may create operational problems.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. CHAPTER IX

SUMMARY AND SYNTHESIS

Tectonic History

Structural relationships in the White Sulphur Springs area are

related to various features that date back to Precambrian (Protero-

zoic) time. The following is a summary of the tectonic history of

the White Sulphur Springs region:

1. The Phanerozoic Belt basin developed. This basin was

possibly an aulocogen, failed arm of a triple junction (Burchfiel &

Davis, 1975; Schmidt & Garihan, 1984), or a continental block-faulted

region (Winston, 1987). The major transgressive-regressive sequence

of Belt sediment deposition (-1500-850 Ma) was accompanied by

regional arching and erosion along the basin margins (Winston, 1987).

This thickest accumulation of young Belt deposits occurred in the

Helena embayment, an eastward-trending arm of the Belt basin.

2. The Lewis and Clark line was established during Precambrian

(probably Windermere) time (Harrison et a l., 1974). This regional

structural lineament is located near the northern margin of the

Helena embayment.

3. Deposition of the transgressive sequence of Cambrian strata

began during Middle Cambrian time. Renewed tectonic a c tiv ity ,

perhaps related to the Antler orogeny, prevented deposition in the

area from Ordovician through Lower Devonian time. Tectonic s ta b ility

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. returned with the deposition of the Late Devonian Maywood and Jeffer

son formations.

4. Deposition of stable shelf sediments with renewed periods

of tectonic a c tivity was perhaps related to the Sonoma orogeny (Late

Paleozoic-Early Mesozoic) and the Nevadan orogeny (Middle to Late

Mesozoic). Such a c tiv ity resulted in nonmarine (Jurassic Morrison)

and clastic (Cretaceous Kootenai) synorogenic deposits.

5. In itia l development of Sevier east-west compressional fea

tures in the area began during Late Cretaceous to Paleocene time.

Thrusting in the area was associated with le ft-la te ra l movement

along the Lewis and Clark line (Reynolds, 1979). The convex eastward

geometry of thrusting is related to the margin of Belt deposition

(Helena embayment) and the buttressing effect of the stable foreland.

6. Fold and thrust features were truncated by the Early Eocene

Castle Mountain stock.

7. Regional extension and associated u p lift began in Late

Eocene time (Kuenzi & Fields, 1971). Extension continued during

Middle Miocene time, with associated rig h t-la tera l movement along

the Lewis and Clark lin e . South of the Lewis and Clark lin e , basin

and range extensional features such as the Smith River Valley were

formed (Reynolds, 1979). Extensional features truncated many

Sevier structures although some may have followed preexisting

Sevier zones of weakness.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Hydrothermal

Hydrothermal a c tiv ity in the White Sulphur Springs area is a

surface expression of a structurally controlled circulation system.

Meteoric water descends along fracture zones associated with faulting

and is heated within a high thermal gradient regime that is related

to low conductivity rocks (Belt shale and Tertiary clays) in the

Smith River Valley and high regional heat flow. Recharge may predom

inate where water saturated alluvium provides a constant source of

water to fault zones north of White Sulphur Springs.

The wide range of calculated reservoir temperatures [ a ^OCSO^-

H20 ), 52° C; Na-K-Ca-Mg, 53.5°, 72°, and 73.4° C; Chalcedony, 73° C;

Quartz, 95.6°-99.8° C] fo r thermal waters indicates that variable

degrees of mixing occur, and that thermal waters do not reach chemi

cal equilibrium at depth. Mixing at intermediate depths may be

related to recharge along faults that are at different structural

levels.

Discharge of thermal water is along the north-trending White

Sulphur Springs normal fa u lt. The area of discharge is lim ited to

a short linear zone (~2 km) which greatly constrains the potential

fo r shallow thermal development in the area. The 72°C ± 10°C

estimated reservoir temperature indicates that future thermal

development in the area is limited to space heating and recreational

use.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. APPENDICES

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix A

Conversion Factors for Units Used in This Paper

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 97

CONVERSION FACTORS FOR UNITS USED IN THIS PAPER

Length: 1 meter (m) = 3.281 f t 1 kilometer (km) = .6214 mi = 3,281 f t

Area: 1 km2 = 106 m2 = 0.3861 mi2

Volume: 1 lit e r (1) = 0.2642 gal 1 1/sec = 86.4 m3/day = 15.85 gal/min (gpm)

Temperature: °C = | (°F - 32); °F = | (°C) + 32

Temperature gradient: 1° C/100 f t = 32.8° C/km = 10"30 C/m rate of temperature increase with depth

Pressure: 1 bar = 0.9869 atm = 14.50 psi = 1.020 kg/cm2 = 106 dynes/cm2

Heat flow: 1 x 10“6 cal/cm2 sec = 4.19 x 10"2 W/m2 (Watts per square meter) 1 heat flow unit (HFU) = 1 x 106 cal/cm2 sec

Thermal conductivity (K) 1 x 10"3 cal/cm sec °C = .418 W/m °K

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix B

Stereographic Analyses of Folds

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. • poles to bedding + poles to . (pressure solution \ cleavage

3 6° S49W

A. Station WSS-81-38. S-pole diagram for fold in the Newland Limestone. Located in the NE% sec. 5, T.9N., R.7E B. Station WSS-81-GSA. S-pole diagram for a minor fold and pressure solution features in the Newland Limestone. Located in the NE% sec. 5, T.9N., R.7E.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. .20° S I4E

A. Station WSS-82-77. S-pole diagram for a minor fold in th Jefferson Formation. Located in the Wh sec. 8, T.8N., R. B. Station WSS-82-78. S-pole diagram for the Cottonwood Creek syncline. Located in sec. 7 & 8, T.8N., R.7E.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. N

27° S76%

B 18° sie'W

A. Station WSS-82-97. S-pole diagram for a minor fold in the Meagher Limestone. Located in the SW^ sec. 29, T.8N., R.7I B. Station WSS-82-108. S-pole diagram for a minor fold in the Pilgrim Limestone.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 7 ° S8E

A. Station WSS-82-100-107. S-pole diagram for the Willow Creek syncline. Located in sec. 23 & 24, T.9N., R.7E. B. Station WSS-82-91. S-pole diagram for a minor fold in the Pilgrim Limestone. Located in the NE^s sec. 30, T.8N., R.7E.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 3 0 ° S 4 7 °E

A. Station WSS-82-177. S-pole diagram for a fold in the Amsden Formation. Located in sec. 33, T.9N., R.7E. B. Station WSS-82-176. S-pole diagram for a fold in the Amsden Formation. Located in sec. 34, T.8N., R.7E.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix C

Gravity Data

104

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 105 WHITE SULPHUR SPRINGS, MONTANA GRAVITY SURVEY

Area - Meagher Co., MT Observer - Michael Stickney (MBMG) Instrument - Worden Meter Educ. Model Density used in Bouguer correction factor - 2.670 Datum - Base 1 - 980484.00 Date 7-27-81 STA, LATITUDE LONGITUDE ELEV SIMPLE NO, DEC MIN DEG MIN b . anom , » t » __ «»»»»»»» _* juhhm »jh »«»♦ BAS El 46 32,90 10 56,76 4960.0 12,313 WS001 46 32,88 11 01,45 4911.0 26,187 HS002. -44- 32 >.90 A . 1 X 2.3...414 WS003 46 32,90 110 59,38 4903,0 16,302 ;wS004 46 32,90 111 0 0 , 00 4880,0 20.457 J1SS05- 46 S2-,-ga 440-5-a.iJ-_ 4 i4 i..-0 - i a JA a WS006 46 32,90 110 58,12 4927.0 14,203 WS007 46 J_2,90 110 57.48 4945,0 12,942 WS008 46“ 32,90 110- 56.18 4977.0 fl,"9 2 2 WS009 46 32,90 110 55,57 4993.0 12,194 M50X0. _4_6__12^_90 110-5.4. 9J __5 406 ,0 12,609 WS011 46 33,15 110 54,93 5013.0 14,217 WS012 46 32,81 110 54,63 5020.0 17,835 WS4i3_ ..46... 32^95 110 53*60__538_0.*0 l 9_*0“jL 0S014 46 33.13 110 53.12 5060.0 19,421 WS015 46 33,14 110 54.15 5035.0 20,271 wsai6_ 110—5.5 -57__5 B 1 A —2L -1 ^ 6 7 7 WS017 46 34,02 110 56,28 5038.0 l¥ |'9 T T WS018 46 34,10 110 56.83 5034.0 17,908 WS019 A6_3A*65 410-5.8., 1 2 4997 a L3_^54. WS020 46 35,52 110 59,38 4987 ^0 l3 tT 5 0 WS021 46 34,40 110 59.40 5053.0 20,883 WS0?o _46_37_ai 110 _59j _28 5035.0 — L?xp.3. WS023 46 35,52 111 00,67 4912.0 I3,5y2 WS024 46 33,78 110 56.83 4978,0 17.377 WSa25. j46__13_U 110 56.83 4964 x 0 13.053 WS026 46 32,83 110 56.83 4956,0 13,533 MS02-7- _ 4 6 _ 3 l*4 0 110 *i , fl 3 4 9 4 ^,0 lj)7_ WS028 46 31,47 110 57.13 4930.0 18,191 WS029 46 30,18 110 58,27 4914.0 21,255 MS 03.0. -A6 31 ,4-5 20. 568 WS031 46 30,69 110 57.50 4940,0 16,733 WS032 46 30,72 110 57,43 4973.0 18,502 M S filli 46 30.73 -L? . 2 2 4_ WS034 46 30,73 110 55.50 4980.0 16,922 WS035 46 30.73 110 54.30 5032.0 12,802 MS01S —46—3-1 rla ■14.0 54.^30— 5 0 4 4 ,0 - _ L 5 ^ li7 _ WS037 46 32,35 110 54.30 5034,0 12,900 W&038 46 32,05 110 55,57 4975,0 11.929 MMISL Utt- 5.6,20-._49s.i..a_ WS040 -46“ 34765 10 56,83 5116.0 T 2 7 4 ¥ T Wf04l 46 31,38 10 56,50 4937,0 19,335

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 106 WHITE SULPHUR SPRINGS, MONTANA GRAVITY SURVEY

Area - Meagher Co., MT Observer - William Gierke (WMU) Instrument - Worden Meter No. 944 Density used in Bouguer correction factor 2.670 Datum - Base 1 - 980484.00 Date 7-19-82 •STA, LATITUDE LONGITUDE ELEV SIMPLE NO, DEG MIN DEG MIN B.ANOM , • »»» »»»»»»»» «*»**»•» »»*» »»»» BASE1 46 32,90 110 56,76 4960,0 12,313 WS042 46 32,87 111 03.70 5106,0 22,469 WS2L4-J- 4ft 32,87 11J1__0-3^.U— S0 78-^2- „_ 2,2^211 WS044 46 32.87 111 01.90 5032.0 29,624 WS045 46 29,83 110 00,02 4903,0 21,052 WS046 46 29,83 111 00.67 4890.0 20,528 WS047 46 29,83 110 54.93 5028,0 16,425 WS048 46 29,83 110 55.62 4994,0 15,666 HS043- 46 29*42- 15.3J6 WS050 46 28,53 110 57,40 5024,0 15,839 WS051 46 28,53 110 59.60 5137.0 15,559 WSgSo -46 28*53- 1.4,941 WS053 46 28,10 110 57.05 ~5023,0 11,993 WS054 46 27,66 110 57.05 5043,0 11,380 -W.sa5.S- 110 57 70 *07? 0 -12,9?7. WS0S6 46 27,65 110 58^35 5094Ja 14.3 WS058 46 30,93 110 51,75' 5258 'm 0 15^901 Date 7-20-82 WS059 46 33,00 110 52.33 5114.0 17,918* WS060 46 33,38 110 51.82 5138,0 18,6b9 wsa6i _-46_14_3x 110 51 Jj 2_-5-1.00.0. _21_J}06_ WS062 46 33,92 110 51.37 5122.0 19,257 WS063 46 35,63 110 50.48 5233,0 23,166 WS064 _A6-_3&U-5 U 0 50.42 5306^2 _12A46l WS065 46 36,89 110 50.62 5371,0 25,7 29“ 46 35,05 110 50.57 5158.0 21,727 uS067 - 46 34,2.1 110 51.15 5118 r 0 17.519 WS068 46 34,18 110 48,32 5455,0 21,424 WS0fr9 -46_34-^S 110 50.57 517a,0 18.781 WS070 46 33,29 110 50.08 5234,0 20,765 w saJi 46 33.06 110 49.22 5490.0 18,792 WS072 46 32,89 110 54.32 5015.0 15,086 1WS073 46 32,89 110 54.45 5021.0 17,529 :WS07a -4.6—32j-5.1 110 54.15 .5069.0 16,065 IW5075 46 32,53 110 53.85 5096.0 “15,7 59 WS076 46 32,70 110 53,85 5116.0 15,875 ;WSfl77 110 54.15 5064,0 17,685 WS078 46 32,85 110 54,15 5031.0 19,539 WS079 46 32,89 110 53,67 5088.0 19,002 IwSflia 110 _5J_05 _ 5130 0 19.779

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 107 WHITE SULPHUR SPRINGS, MONTANA GRAVITY SURVEY Area - Meagher Co., MT Observer - William Gierke (WMU) Instrument - Worden Mete No. 944 Density used in Bouguer correction factor - 2.670 Datum - Base 1 - 980484. 00 Date 8-09-82 STA, LATITUDE jONGITUDE ELEV SIMPLE 1 NO, DEG MIN DEG MIN B.ANOM , »«*• _*«*# #.*.#.*_____« « * #— ***_• ;WS081 46 29.43 ,10 54,22 5082.0 18,398 !WS08? 46—28,60 10 54.22 5094.0. 16.249 WS083 46 28.67 10 53,67 5149.0 18,093 WS094 46 28,80 10 52.62 5265.0 14,536 WS0B5 46 27,96 10.5.3.4.2. 5142 r 0 — l l 7 2 ! WS086 46 26.82 10 53,30 5202.0 13,900 WS087 46 26,42 10 52.45 5312.0 15,195 : WS088 _4l_25^9.a 10 51,82 5424.0 - l ! * 286. 1 WS089 46 25.65 10 50,63 5605.0 15,510 WS090 46 27.82 10 54,22 5070.0 16.317 Date 8-10-82 WS091 45 26,80 10 54.22 5139.0 12.172 WS0*2 46 26,80 10 55.23 5069.0 12,078 WS093 46 26.87 10 56.28 5082.0 10,266 WS094 46 26, 82 ) 10 57 ,05_ 5125.0 13.355 BASE2 46 32,93 10 52.43 5112.0 18,482 Date 7-14-82 WS095 46 32,95- 10 48.45 5533.0 20,149 WS0-9& 46 32, 95 10-4 8^5 2 —5-445U-0- -2 9 j 6_42. WS097 46 32,94 10 48,80 5452.0 21,267 WS098 46 32,94 10 48.97 5365,0 19,065 -WS099- 46 32,94 10_4aU-2__511-7.2- _ 2 !. 8.0.7_. WS100 46 32,94 10 49,28 5408.0 23,628 WS101 46 32,95 10 49,58 5344.0 23.389 M S 1 & & 46- 3 2 *3 5 1.10—49.9-2 524&JJ- _2-U 2^-7_ WS103 46 32,95 10 50,22 5215,0 20,504 WS104 46 32.95 10 5u.53 5210.0 18,979 WS105 46 32,93 10 52,10 5140.0 18,362 WS106 46 32,93 10 51,82 5198,0 18.721 WSL01 —46_32t 93 110 .5-1.48 __5206.0- 18.789 WS108 46 32,93 10 51.17 5224.0 17,806 WS109 46 32.94 10 50,85 5211.0 17,239 BASE3 46 30,30 10 54,08 5058.0 16,037 Date 7-17-82 WS110 46 30,29 10 50,52 5920.0 10,393

MSlLt- -4-6 3&t-2-9 . U .2 tf0 WS112 46 30,29 10 51,12 5447,0 10,344 WS113 46 30,29 10 51,90 5424.0 12.311 tf&LL4- -46 30,3^ 10 -5-1. B2__S35-4-.0- -14.-567 .WS115 46 30,30 10 5.2,05 5357.0 17,277 WS116 46 30,30 10 52,40 5279.0 14,596 iW SllX 46 30.1-0 10 52r68 -5.22-8—0- X 2,112 WS118 46 30,30 10 53.95 5072.0 15,663 WS119 46 30,30 10 53.62 5107.0 13.312 WS120 _4 6-3 0^3.0 1.1.0 -5-3L.J.3— -51-47.. a. 11,478 WS121 46 30,30 10 53,05 5184.0 11,153 WS122 46 30,30 10 54.30 5053.0 15,855' WS123 46 30,30 10 54,87 5018.0 18,731 _WSJL2 4 _ 46-30.30 110 54.55 ..52.3X.J2_ . l i j 3 3 _ . .

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix D

Stratigraphic Profiles

108

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.

day sandy day colluvium approximate approximate location of of White Sulphur Springs Springs fault & rock clay broken gravel A, clay clay sand gravel gravel

A gravel clay A clay sand clay sand sand static static level water 0*0 0*0 372-* JT JT '

APPENDIX D. APPENDIX Stratigraphic profile A-A' (Plate 4). Vertical scale exaggerated A gravel A gravel clay sand gravel sand sand 4980 5100 5060 4900 4860 5020 z

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.

o i B

clay day gravel gravel A approximate approximate location of White Sulphur Springs fault Springs clay rock brokan clay gravel cemented bend bend profile in = = static water level clay soil gravel i B APPENDIX D (Cont'd). APPENDIX Stratigraphic profile B-B1 (Plate 4). Vertical scale exaggerated. ' 5 0 2 0 • • 4 9 8 0 • • 4 9 4 0 ' 4 9 0 0 r 5 0 6 0 L L 4860 < iti -I lil >

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Appendix E

Chemical Analyses of Well Waters

111

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 112

Sample Number WSS001 - Cemetery Well

HONTANA BUREAU OF MINER AND GEOLOGY UATER DUALITY ANALYSIS BUTTE,MONTANA 39701 < 4 0 0 ) <*90- 0101 LAD NO. 0101112 STAUf MONTANA MEAGHER LATITUDE-LONGITUDE 46D32'03*N 111D01'32*W SITE LOCATION 9N 6E 10 CCDD UTM COORDINAH:S 71? N5153150 F498045 MDMG S IT E WSSOOl ■ TOPOGRAPHIC MAP HANSON RESERVOIR 7 1 / 2 ' 463203111013201 GEOLOGIC SOURCE WELL DRAINAGE DASIN BC LAND SURFACE ALTITUDE 5 0 4 2 . FT < 10 AGENCY + G AMPI.HR MBMGXMGG SUSTAINED YIELD BOTTLE NUMBER USS001 YIELD MEAS METHOD DATE SAMPLED JO-JIJI. - 01 TOTAL DEPTH OF HELL ?S 0. n (R> TING SAMPLED 12 540 HOURS SUL A B O V E (-) OR DELOW GS 7 . FT (M ) LAB + ANALYST MUMGXFNA ft DATE ANALYSED OG-AUG-81 CA!5IS8s?A8M?^ STt?EL SAMPLE HANDLING 31? COMPLETION TYPE * METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER IJSE IRRIGATION SAMPLINO SITE CEMETARY Hell GEOLOGIC SOURCr MG/L MEO/L MG/L MEO/L CALCIUM (CA) 39.9 1.99 BICARBONATE (HC03) 162.7 2 .4 7 MAGNESIUM (MG) 9 . 9 0 .8 1 CARBONATE (C 0 3 ) 0 . SODIUM (NA) 1 7 .6 0 .7 7 CHLORIDE(CL) 1 6 .3 0 .4 7 POTASSIUM (K> 6.? 0.16 SULFATE ( S04 > 3 1 .? 0 .6 5 IRON (F E ) .0 0 2 0 .0 0 NITRATE (AS N) 1 .0 6 0 .0 8 MANGANESE (MN) < .0 0 1 FLUORIDE ( F ) .3 0 0 .0 2 SILICA (SI02) 3 9 .2 PHOSPHATE TOT (AS P> TOTAL CATIONS 3 .7 3 TOTAL ANIONS 3 . 8 7

STANDARD DEVIATKIN OF ANION-CATION BALANCE (SIGMA) 0 .0 8 LABORATORY PH 7 .6 7 TOTAL HARDNESS AS CAC03 1 4 0 .3 0 FIE L D WATER TEMPERATURE S 3 . F TOTAL A LK A LIN ITY AS CAC03 1.33.44 CALCULATED DISSOLVED SOLIDS ?6?.01 SODIUM ADSORPTION RATIO 0 .6 3 SUM OF DIGS. CONSTITUENT 344.56 RY7NAR STABILITY INDEX 7.R 8 LAB SPEC.COND. <•02 STRONTIUM.DISS (MG/L-8R) .21 C ADMIUM.DIGS(M G/L AS CD) < •00? TITANIUM DISCMO/l. AS TI) .003 CHROMIUM. D IS S (H G /L -C R ) <.002 VANADIUM.DISSCMG/L AG V> <.001 COPPER.DISS (HG/L AS CIJ) <.00? ZINC.DISS (MG/L AS ZN) .004 LITHIUM,DISS(MG/l. AS L.I) <.002 ZIRCONIUM DIS(HG/I. ZR) <.004 MOLYBDENUM. D IS S (MG/I. - MO > .5 ARSENIC. DISSCUG/l. AS AS) 7.2

REMARKS: HATER LEVEL TAKEN DURING PUMPING * 7 ' BMP * NO TASTE OR ODOR X 14 SPRINKLERS PUHPINO DURINO THIS TINE *

EXPLANATION: MO/L - MILLIGRAMS PER L IT E R . IJG/L - MICROGRAMS PER L IT E R . H E n/l. MILLIEQUIVF.LENTS PER LITER. FT - FEET, MT « METERS. (M) - MEASURED. (E) - ESTIMATED, (R> - REPORTED. TR » TOTAL RECOVERABLE. TOT - TOTAL.

QU UA S2 UI OU PW AT o t h e r OTHER AVAILABLE DATA Y OTHER F i i . r n u m b e r s :

p r o j e c t : cost : LAST EDIT DATE: 16 -S E P -8 1 b y : TP XM.JT PROCESSING p r o g r a m : F1730P V2 ( 8 / 9 / 0 0 ) p r in t e d : 16-S E P -B 1 PERCENT MEQ/L (FOR PIPER PLOT) CA MO NA K CL S04 HC03 33 21 20 4 12 16 68 NOTEI IN CORRESPONDENCE, PLEASE REFER TO LAB NUMBER.' 8 1 0 1 1 1 2

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 113

Sample Number WSS002 - Edwin Bodell

MONTANA BUREAU OF MINER AMU GEOLOGY HATER QUALITY ANALYSIS BUTTE,MONTANA 59701 (106 ) 496-4 101 LAB HU. H101113 STATE MONTANA COUNTY MEAGHER LATITUDF-LONft.TTUDE AAPSA'tA'N llODSAMO'W SITE LOCATION 9H 6E 2 ACCC UTM COORDINATES 712 NS1S72S0 CS04R95 HBHO SITE WSS002 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 465414110561001 GEOLOGIC SOURCE * * a SAMPLE SOURCE Uri l DRAINAGE BASIN DC LAND SURFACE ALTITUDE 5 0 9 0 . FT < 10 AGENCY + SAMPLER MBM03UGG SUSTAINED YIELD 1 0 . OPM BOTTLE NUMBER WSS002 YIELD MEAS METHOD BUCKET/STOPWATCH DATE SAMPLED 20—JUL-81 TOTAL DEPTH OF WELL 1 9 0 . FT OR BELOW GO (M > LAB + ANALYST n d m «* f n a oasinosdiameter B IN (R> DATE ANALYZED STEEL SAMPLE HANDLINO 3 1 2 0 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL HATER USE DOMESTIC SAMPLING S IT E BODF.LL. EDWIN*2 MI NU WHITE SULPHUR SPRINGS GEOLOGIC SOURCE MG/L NFO/L MG/LMEO/L CALCIUM (CA) 4 3 .7 2.10 BICARBONATE (IIC03) 236.7 3 .8 8 MAGHESIUM (MG) 1 6 .1 1 .3 2 CARBONATE (C 03 ) 0 . SODIUM (NA) 1 6 .8 0 . 7 3 CHLORIDE (Cl.) 5 . 8 0 .1 6 POTASSIUM (K> 7 .7 0 .1 7 SULFATE (S 0 4 ) 2 0 . 0 0 .4 3 IRON (FE) <.002 NITRATE (AS N) .7 7 0 .0 7 MANGANESE (MM) <.001 FLUORIDE (F) .4 5 0 .0 2 SILICA ( S I0 2 ) 5 6 .6 PHOSPHATE TOT (AS P) TOTAL CATIONS 4 .4 2 TOTAL ANIONS 4 .5 7 STANDARD D EVIA TIO N OF ANION-CATIONCON DAl.ANOEBALANCE (SIGMA) 0.86 LABORATORY PH 7 . OH TOTAL HARDNESS AS CAC03 .17 5.39 FIE LD UATER TEMPERATURE 5 0 . 0 F TOTAL A LK A LIN ITY AS CAC03 1 9 4 .1 3 CALCULATED DISSOLVED SOLIDS 7 5 5 .0 7 SODIUM ADSORPTION RATIO 0 . 5 3 SUM OF DISS. CONSTITUENT 4 0 5 .1 2 RYZNAR S TA B ILITY INDEX 7 .2 6 LAD SPEC.COND. (MICROHHOS/CM) 4 3 4 .7 I.ANGI.IEK SATURATION INDEX 0 .3 1 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 82. CNDUCTVY,FIELD MICROMHOS 4 0 2 . FIELD PH 6.50 ALUMINUM. DISS (NO/L-AL) < . 0 3 NICKEL.DISS (MG/L AS NI) <.01 SILVER, DISS (HR/I. AS Aft) <.002 LEAD.DISS (MO/L AS PB) <.04 BORON .DISS (MO/L AS B) <.02 STRONTIUM. DIGS (MO/I.-SR) .52 CADMIUM,DISS(MG/L AS CD) <.002 TITANIUM DIS(MO/L AS TI> .017 CHROHKJM» DISS (MC/L-CR) <.002 VANADIUM.DISS(HG/I. AS V) .001 COPPER.DIES (MG/L AS CU> <•002 ZINC.DISS (MO/L AO 7N) .022 LITHIUM,DISO(MO/L AS LI) <.002 ZIRCONIUM DIS(MG/L ZR> <.004 MOLYBDENUM. DISS (M G /L-H O ) <.1 ARSENIC,DI5S(UG/L AS AS) 5.9

r e m a r k s : w a t e r h a s no o dor or t a s t e * SEND COPY TO EDWIN BODELL. WHITE SULPHUR SPRINGS *

EXPLANATIONS MG/L - MILLIGRAMS PER L IT E R . UG/I. " MICROGRAMS PER L IT E R , MEO/L MILLIGQUIVELENTS PGR LITER. FT « FEET, MT - METERS. (M> - MEASURED, (E) - ESTIMATED, (R) - REPORTED. TR - TOTAL RECOVERABLE. TOT «■ TOTAL. QW VA !12 WI OW PW AT OTHER OTHER AVAILABLE DATA Y Y OTHER f i l e n u m b e r s :

p r o j e c t : c o s t : LAST EDIT DATE! 1 6 -S E P -0 1 b y : TP SMJT p r o c e s s in g p r o g r a m : F1730P V2 (G /7 /G 0 ) p r i n t e d : 16 -fiE P -O l PERCENT NEO/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 49 27 16 4 3 7 84 NOTES IN CORRESPONDENCE. PLEASE REFER TO I.AB NUMBER: 0101113

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Sample Number WSS003 - Edwin Bodell

MONTANA BUREAU OF MINES AND OCOt.OOY UATER QUAl.I TY ANALYSIS BUTTE.MONTANA 59701 (406)496 -4101 LAB NO. 01Q1114 STATE MONTANA COUNTY MEAGHER LATITUDE-I.ONRITUUE 4 6 D 3 3 '0 6 ‘ N 11 0D57'26•W CITE LOCATION 9W 6E 10 DCDB UTN COORDINATES 712 N5155130 E503305 MDNO SITE USS003 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463306110572601 GEOLOGIC SOURCE 110ALVM* X S SAMPLE SOURCE WELL DRAINAGE DASIN DC LAND SURFACE ALTITUDE 4960. FT < 10 AGENCY + RAHPLER MDMG3UGG SUSTAINED YIELD BO TTlE NUMBER USS003 Y IE LD MEAS METHOD DATE SAMPLED 20-JU L--81 TOTAL DEPTH OF WELL 36» FT (R) TIME SAMPLED 17 545 HOURS SUL A B O V E (-) OR BELOW OS 1 4 . FT (R ) LAB fr ANALYST MDHOSFNA CASINO DIAMETER 7 IN DATL* ANALYZED CASINO TYPE STEEL SAMPLE HANDLING 3 1 20 COMPLETION TYPE 01* METHOD SAMPLED PIJHPED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING SITE BODELL' EDWIN S GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) MG/L MEO/L MG/L MEP/L CALCIUM (CA) 0 7 .44.36 4 . 3 6 BICARBONATE (H C 03) 3 5 8 . 5 .3 7 MAGNESIUM (MG) 1 7 .5 1 .4 4 (C 03) 0 . SODIUM (NA) 7 .2 0 .3 1 (CL) 4 . 0 0 .1 1 POTASSIUM (K) 1.0 0 . 0 5 (5 0 4 ) 1 3 .3 0 .7 8 IRON (F E ) < .0 0 2 NITRATE (AS N) .2 6 0 .0 2 MANGANESE (MN) < .0 0 1 FLUORIDE (F) .2 4 0 .0 1 SILICA (SI02) 2 0 .1 (AS P ) TOTAL CATIONS 6 . 1 6 ANIONS 6 .2 9 STANDARD D EVIATIO N OF ANIO N-CATIO N BALANCE (S IG M A ) 0 .6 5 LABORATORY PH 7 .0 4 TOTAL HARDNESS AS CAC03 2 9 0 .2 7 F IE L D UATER TEMPERATURE 4 0 . 5 F TOTAL A LK A LIN ITY AS CAC03 2 9 3 .6 2 CALCULATED DISSOLVED SOLIDS 320.15 SODIUM ADSORPTION RATIO 0.18 SUM OF DISS. CONSTITUENT 509.80 RYZNAR S T A B IL IT Y INDEX 6 .3 4 LAD SPEC.CONK.(MICROMIIOS/CM) 577.6 LANGLIER SATURATION INDEX 0.75

PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C> 7 9 .0 CNDUCTVY.FIELD MICROMHOS 5 2 6 . FIELD PH 6.55 ALUMINUM. DISS (MG/l.-AL) <.03 NICKEL.DISS (MG/L AS NI> < .0 1 SILVERrlllSS (HG/L AG AG) <.002 LEAD.DISS (MO/L AS PB) < .0 4 BORON .DISS (MG/L AS B) <.02 STRONTIUM.DIGS (MG/L-GR) .2 9 CADMIUM' D IS S ( MG/L AS CD) < .0 0 2 TITANIUM DIS(H()/L AS TI) .0 1 1 CHROMIUM.-DISS (MO/L-CR) <.002 VANADIUM. DISS(MO/l. AG V) .0 0 1 COPPER. BISS (MG/L AS GtJ) <.002 ZINC.DISS (MO/L AS 7N) .0 0 5 LITHIUM.DISS(MO/L AS LI) <.002 ZIRCONIUM DIS(MG/L ZR) < .0 0 4 MOLYDDENUH.DIGS(HG/L-HO) <.1 ARSENIC.DISS(UG/L AS AS) 1 .2

REMARKS) UATER HAS NO ODOR OR PECULIAR TASTE * OUNER COMPLAINS OF HINERAI. DEPOSITS IN HOT UATER HEATER TANK (CAC03) * MAIL COPY TO EDUIN DOOELL WHITE SULPHUR SPRINGS. MT. *

EXPLANATIONS MG/L ■ MILLIGRAMS PER LITER. U G /L <• MICROGRAMS PER L IT E R . MEP/L MTL1.IEQUIVELENTS PER LITER. FT ■ FEET. MT METERS. (M> - MEASURED. (E ) ■ ESTIMATED' (R) - REPORTED. TR ' TOTAL RECOVERABLE. TOT - TOTAL. QU UA S2 UI OU PU AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS) PROJECTS COSTS LAST EDIT DATES 16-SEP--81 BY' TP SMJT PROCESSING PROGRAMS F1730P V7 (0/9/00) PRINTED) 16-GEP-G 1 PERCENT MEQ/L (FOR P(PER PLOT) CA MG NA K CL 004 HC03 70 23 3 0 1 4 93 NOTES IN CORRESPONDENCE. PLEASE REFER TO LAD NUMBERS 81 0 1 1 1 4

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Sample Number WSS004

MONTANA BUREAU OF MINES AND GEOLOGY UATER QUALITY ANALYSTS BUTTE*MONTANA 59701 <406)476-4101 l a d n o . m a i n s STATE MONTANA COUNTY MEAGHER LATITUDE-LONOITUBE 46D32' 43*N 110D59/:I7,H SITE LOCATION 9N 6E 17 AACC UTM COORDINATES Zl? N51S4420 E500520 MBMfi S IT E USS004 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463243110593701 GE0I.00TC SOURCE 110AI.VM4 * * SAMPLE SOURCE UEI.L DRAINAGE DASIN DC LAND SURFACE ALTITUDE 4 0 0 0 . FT < 10 AGENCY I SAMPLER HDHG*UGG SUSTAINED YIELD 6 . GPM BOTTLE NUMBER USS004 YIELD MEAS METHOD BUCKET/STOPWATCH DATE SAMPLED 2 1 -J U L -0 1 TOTAL DEPTH Or WELL 2 2 . FT OR DEL.OW GS 7 .0 FT (M ) LAD > ANALYST MBMGtFNA CASING DIAMETER 24 IN (M> DATE ANALYZED 00-A U G -81 CASING TYPE G-STEEL SAMPLE HANDLING 312 COMPLETION TYPE O lt O l METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE DOHESTIC SAMPLING SITE GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) MG/L MEO/L MG/LMEO/L CALCIUM (CA) B3.9 4.19 BICARBONATE (H C 03) 3 4 4 . 3 .6 4 MAGHESIUM (MG) 1 7 .0 1 .4 0 CARBONATE (C 0 3 ) 0 . SODIUM (NA) 19.7 0.06 CHLORIDE (CL) 1 9 .4 0 .5 5 POTASSIUM (K) 2.0 0.07 SULFATE (S 0 4 ) 2 2 .4 0 .4 7 IRON (F E ) <.002 NITRATE (AS N) .9 5 0 .0 7 MANGANESE (MN) <.001 FLUORIDE (F) .4 3 0 .0 2 SILICA (SZ02) 10.8 PHOSPHATE TOT (AS P ) TOTAL CATIONS 6 .5 1 TOTAL ANIONS 6 .7 4 STANDARD DEVIATIO N OF ANION-GATION BALANCE (S IS M A ) 1. 1: LABORATORY PH 7 .6 4 TOTAL HARDNESS AS CAC03 2 7 9 .4 7 F IE L D UATER TEMPERATURE 4 9 .0 F TOTAL A LK A LINITY AS CAC03 2 0 2 .1 4 CALCULATED DISSOLVED SOLIDS 354.04 SODIUM ADSORPTION RATIO 0 .5 1 SUM OF DISS. CONSTITUENT 529.3B RYZNAR S T A B IL IT Y INDEX 6 .6 1 LAD SPEC.COND.(MICROMHOS/CM) 6 2 6 .5 LANGLIER SATURATION INDEX 0 .5 1 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 70. CNDIJCTVY.FIEI.il HICROMHOS 5 5 9 . ALUMINUM. DISS (MG/L-AL) <.03 NICKEL.DIGS (MO/L AS NT) <.01 SILVFR*DISS (MG/L AS AG) <.002 LEAD.DISS (MG/L AS PD) < .0 4 BORON .DISS (NG/L AS B) <.02 STRONTIUM.DISS (MO/L-SR) .2 6 CADMIUM.DISS(MG/L AS CD) <.002 TITANIUM D1S(MG/L AS TI> .0 0 3 CHROMIUM. BISS (M O /L -C R ) < .0 0 2 VANADIUM.DISS(MO/L AS V) <.001 COPPER.DISS (MG/L AS CU) <.002 ZINC.DISS * (MG/L AG ZN> .3 8 LITHIUM.DISS(MG/L AS LI) <.002 ZIRCONIUM DIO(HG/L ZR) < .0 0 4 MOLYBDENUM * D IS S ( N G /L -H O ) < .1 ARSENIC.DISSOJG/L AS AS) .8

REMARKS! UATER HAS NO ODOR OR TASTE * LADf FU CA OF 116.7 M G /L. MG OF 1 7 .7 HG/L. NU OF 20.4 MG/L AND K OF 5.1 LAD: GIVES -.03 SIGMA * EXPLANATION: MG/L - MILLIGRAMS PER L IT E R . U G /L » MICROGRAMS PER L IT E R . MEO/L ■ M ILLIEQ U IVELEN TS PER L IT E R . FT FEET. MT - METERS.

p r o j e c t : c o s t : LAST EDIT DATE! 16 -S E P -8 1 d y : TP SMJT p r o c e s s in g p r o g r a h : F1730P V2 ( 8 / 9 / 0 0 ) p r i n t e d : 16-G EP-B 1 PERCENT MEO/L (FOR PIPER PLOT) CA MG NA K CL 004 NCOS 64 21 13 1 0 6 83

n o t e : i n correspondence , p l e a s e r e f e r TO LAB n u m b e r : 0 1 R l 115

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Sample Number WSS005 - R. E. Saunders, J r.

MONTANA BUREAU O f MINCH AND OEOLOGY HATER QUALITY ANALYSIS BUTTE.MONTANA 59701 (406)496-4101 LAD HO. 0101116 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 46D33'20,N 11 4 9 M 6 U0D SITE LOCATION 9N 7G 10 ACCA UTM COORDINATES 712 HS155013 E S I3050 MDMO S IT E USS005 TOPOBRAPHIC MAP UTLLOH CREEK RESERVOIR 7 STATION ID 463520110494601 GEOLOGIC SOURCE 110ALVM* * t SAMPLE SOURCE HELL DRAINABE DASIN DC LAND SURFACE ALTITUDE 5 5 6 0 . FT < 10 AGENCY + SAMPLER MDMOAUSG SUSTAINED YIELD BOTTI. E NUMBER USS005 YIELD MEAS METHOD DATE SAMPLED 21 -J U L -8 1 TOTAL DEPTH OF NELL 0 5 . FT (R> TIM E SAMPLED 11:30 HOURS SUL ABOVE( - ) OR BELOU OS 3 . FT LAD I- ANALYST MBH03FNA CASINO DIAMETER 6 IN (R ) DATE ANALYZED 0 8 -A U G -81 CASING fYPE STEEL SAMPLE HANDLINO 312 COMPLETION TYPE 02t METHOD SAMPLED PUMPED PERFORATION INTERVAL 55 TO 75 FT UATER USE DOMESTIC SAMPLING SITE SAUNDERS» R. E. JR. * UNITE SULFUR SPRINGS GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) HG/L MEO/L MG/L MEO/l. CALCIUM (CA) 44.9 2.24 BICARBONATE (NCOS) 1 9 4 .2 3 .1 8 MAGNESIUM (MG) 1 3 .9 1 .1 4 CARBONATE (C 0 5 ) 0. SODIUM (NA) 5 .2 0 .2 3 CHLORIDE (CL) O.S 0 .2 4 POTASSIUM (K> .8 0.02 SULFATE (3 0 4 ) 1 5 .2 0 .3 2 IRON(FE) .0 3 0 0 .0 0 NITRATE (AS N) .02 0.00 MANGANESE (MN) .0 4 6 0.00 FLUORIDE (F) .21 0.01 SILICA (:SI02) 16.6 PHOSPHATE TOT (AS P) TOTAL CATIONS 3 .6 3 TOTAL ANIONS 3 . 7 ! STANDARD DEVIATIO N OF AHIO N-CATIO N BALANCE (OIOMA) 0 . 7 3 LABORATORY PH 7 .9 1 TOTAL HARDNESS AS CAC03 1 6 9 .3 3 FIELD HATER TEMPERATURE 4 9 . F TOTAL A LK A LIN ITY AS CAC03 1 5 9 .2 8 CALCULATED DISSOLVED SOLIDS 201.00 SODIUM ADSORPTION RATIO 0 . 1 7 SUM OF DISS. CONSTITUENT 299.61 RY7NAR S TA B ILITY INDEX 7 . 3 8 LAB SPEC.COND.(MICROHHOS/CM) 350.0 LANGLIER SATURATION INDEX 0 .2 6 PARAMETER VALUE PARAMETER VALUE TEMPERATURE, AIR (C) 80.0 CNDUCTVY,FIELD MICROMHOS 106. ALUMINUM, DISS (MO/l.-AL) <.03 NICKEL,DISS (MG/L AS NI) <.01 SILVER,DISS (MG/L AS AG) <.00? LEAD,DISS (MG/L AS PB> < .0 4 BORON , DISS (H G /L AS B) < .0 2 STRONTIUM,DISS (MO/L-SR) .1 7 CADMIUM,DISG(MG/L AS CD) <.002 TITANIUM DIS(MG/L AS TI) .002 CHROMIUH, DISS (HO/l.-CR) <.002 VANADIUM,DISS(MO/L AS V) <.001 COPPER,DISS (MG/L A3 CU) .013 ZINC,DISS - (MG/L AS 7N) .0 1 5 LITHIUM, DIS3(M0/l. AS LI) <.002 ZIRCONIUM DIG(MO/L ZR) < .0 0 4 MOLYBDENUM, D IS S ( M G/L-M O ) < .1 ARSENIC, D1SS(UG/I. AS AS) .3

REMARKS: MATER HAG NO ODOR OR TASTE 40HNER SAYS HELL RIJNS DRY IN A SHORT PERIOD OF TIHC - ABOUT 5 HRS * UEI.I. TEST DATA FROM DRILL I.OG t PUMPING LEVEL BELCH LSD -• 00 FT AFTER 2 HRS PUMPING AT 2 OPM * SEND COPY TO OUNER

EXPLANATION: MG/L - MILLIGRAMS PER L IT E R , UG/L - MICROGRAMS PER L IT E R , MEO/L - MILl.IEOUIVEL.EHTS PER LITER. FT - FEET, MT - METERS.(M) « MEASURED, (E) ■ ESTIMATED, (R) ' REPORTED. TR - TOTAL RECOVERABLE. TOT * TOTAL. QW HA S2 UI OU PU AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E n u m b e r s :

p r o j e c t : c o s t : LAST EDIT DATE! 16-S E P -Q 1 b y : TP iM JT PROCESSING p r o g r a m : F1730P V2 (0/9/80) p r i n t e d : 1 6 -S E P -O l PERCENT HEG/t. (FOR PIPER PLOT) ’ CA MG NA K CL S04 HC03 61 31 6 0 6 0 84 NOTE: IN CORRESPONDENCE, PLEASE REFER TO LAD NUMBER) 0 1 0 1 1 1 6

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Sample Number WSS006 - Dave E llington

MONTANA BUREAU 111* MINER AND GEOLOGY HATER QUALITY ANALYSIS BUTTE.MONTANA 59701 < 406)496-4101 LAB NO. 0101117 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 46D3?'44,N 1 1 0 D S 1 '5 9 *U RITE LOCATION 9N 7E 17 AACD UTM COORDINATES 713 H5154473 E51027S M3M0 S IT E USS006 TOPOGRAPHIC MAP WILLOW CREEK RESERVOIR 7 STATION ID 4 LAD + ANALYST NDMOSFNA CASINO DIAMETER 6 IN (R) DATE ANALYZED 08-AIJG-Q1 CASING TYPE STEEL SAMPLE HANDLING 312 COMPLETION TYPE 01* METHOD SAMPLED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING SITE ELLINGTON. DAVF. * GEOLOGIC SOURCE MG/L MEO/L MG/L MEO/L CALCIUM (CA) 2 6 . 1 1.30 BICARDONATE (HC03) 1 3 1 .8 2 . 1 6 MAGNESIUM (MG) 10.1 0 .S 3 CARBONATE (C 0 3 ) 0. SODIUM (NA) 6.2 0.27 CHLORIDE (CL) 2 . 7 0 . 0 8 POTASSIUM (K) 1.0 0.05 SULFATE (S04) 1 0 .7 0.22 IRON (FE) < .0 02 NITRATE (AO N) .6 0 0 . 0 4 MANGANESE (HN) .00? 0.00 FLUORIDE (F) .4 4 0.02 SILICA (SI02) 3 9 . 2 PHOSPHATE TOT (AS P) TOTAL CATIONS 2.45 TOTAL ANIONS .52 STANDARD DEVIATION OF ANION-CATIO N BALANCE (SIGM A) 0 . 5 3 LABORATORY PH 7 .6 8 TOTAL HARDNESS AG CAC03 1 0 6 .7 4 FIELD UATER TEMPERATURE 50.0 F TOTAL A LK A LIN ITY AS CAC03 100.10 CALCULATED DISSOLVED SOLIDS 162.77 SODIUM ADSORPTION RATIO 0 .2 6 SUM OF DISS. CONSTITUENT 229.44 RYZNAR S T A B IL IT Y INDEX 0 .4 2 LAB SPEC.COND.(MICROHHOS/CM) 252.6 LANGLIER SATURATION INDEX - 0 . 3 7 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. A IR (C> 8 0 . CNDUCTVY.FIELD MICROMHOS 2 1 9 . ALUMINUM. DISS (HO/L-AL) <,03 NICKEL.DISS (MO/L AS NI> <.01 SILVER.DISS (MG/L AS AG) < .0 0 7 LEAD.DISS (MO/L AS PD) < •0 4 BORON .DIGS (HO/L AS B) <.02 STRONTIUM.DIGS (MG/L-SR) .11 CADMIUM. DISS(MG/I. AS CD) < .0 0 2 TITANIUM DIG(MG/L AG T I> .001 CHROMIUM. DISS (MO/L-CR) < .0 0 2 VANADIUM.DISS(MO/l. AS V) <.001 COPPER.DISS (MG/L AS CIJ) <.002 ZINC.DISS . (MG/L AG 7N) < .0 0 4 LITHIUM.DIGS(MO/L AO LI) <.002 ZIRCONIUM DIG(MO/L ZR) < .0 0 4 MOLYBDENUM.DISS(MG/L-MO) < .1 ARSENIC.DISGdJG/L AG AS) 5 .2

REMARKS! WATER HAS NO ODOR GR SMELL * PH METER OUT OF ORDER * UNABLE TO MEASURE STATIC WATER LEVEL * 100' ESE OF THE SOUTH SIDE CANAL * SEND COPY TO P.O. DX 471, WHITE SULFUR SPRINGS. MT. *

EXPLANATION: MG/L - MILLIGRAMS PER LITER. UG/L MICROGRAMS PER L IT E R . MEO/L M IL L IE O U IV E L E N rS PER L IT E R . FT - FEET. MT - METERS. (H > MEASURED. (E) ESTIM ATED. (R ) ■ REPORTED TR ■ TOTAL RECOVERABLE. TOT ■ TOTAL. QU UA S2 UI GU PW AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATES 1 6 -S E P -8 1 b y : TP *MJT PROCESSING p r o g r a m : T1730P V2 ( 8 / 9 / 8 0 ) p r i n t e d : 1 6 -S E P -n i PERCENT MEO/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 53 33 11 1 3 0 35 note: in correspondence, please refer to lab number: 0101117

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Sample Number WSS007 - Herb Townsend

MONTANA BUREAU Ilf HINES AND GEOLOGY WATER OUAl.ITY ANALYSIS BUTTE,MONTANA 37701 (404)494-4101 LAB NO. 0101110 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 44D30'20,N UODSA'OS1 CITE LOCATION 9N 4E 24 DCC UTM COORDINATES 712 NS150015 ESOSOtO MDHO S IT E USS007 TOPOGRAPHIC HAP WHITE SULPHUR SPRINGS 7 1 STATION ID 443020110340301 GEOLOGIC SOURCE U0ALVMS120SDMS* 3 SAMPLE SOURCE HELL ' DRAINAGE DASIN DC LAND 5URFACF ALTITUDE 4947. FT < 10 AGENCY + SAMPLER HDMOaUGG SUSTAINED YIEL.fi 1000.0 BOTTLE NUMBER HSS007 Y IE LD MICAS METHOD REPORTED DATE SAMPLED 21-.JUL-G 1 TOTAL DEPTH OF HELL 250. FT (R> TIME SAMPLED 1 4 t4 3 HOURS SUL ABOVE (* ) OR DEI.OU GS 1 5 . FT .7 9 0 . 0 4 MANGANESE (MN) <.001 FLUORIDE ( F> .4 3 0.02 SILICA (SI02) 1 5 .9 PHOSPHATE TOT (AS P ) TOTAL CATIONS 4 .1 4 TOTAL ANIONS 4 .2 9 STANDARD DEVIATION OF ANION-CATION BALANCE (SIOM A) 0 .7 7 LABORATORY PH 7 .S 9 TOTAL HARDNESS AS CAC03 1 0 2 .0 1 FIE LD HATER TEMPERATURE 4 0 .3 TOTAL ALK A LINITY AS CAC03 1 3 7 .8 8 CALCULATED DISSOLVED SOLIDS 237.23 SODIUM ADSORPTION RATIO 0.33 SUM OF DISS. CONSTITUENT 334.93 RYZNAR STABILITY INDEX 7.33 LAB SPEC.COND.(MICROHHOS/CM) 409.7 LANGLIER SATURATION INDEX 0.27 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 77. CNDUCTVY.FIELD HICROHHOS 317. ALUMINUM. DISS (MO/L-AL) <.03 NICKEL.DISS (MG/L AS NI) <.01 SILVER.DISS (MG/L AS AG) <.002 LICAD.DISS (MO/L AS PD) <.04 BORON .D IS S (M O /L AS B> < .0 2 STROHTIUM.DISC (MC/L-BR) .37 CAD M IU M .D ISS(M G /L AS Cn> < .0 0 2 TITANIUM DI3(MG/L AS T1) .001 CHROMIUM. DISS (H O /L -C R ) < .0 0 2 VANADIUM.DI3S(MG/L AS V) <.001 COPPER,DIBS (MG/L AS CU) <.002 ZINC.DISS (MG/L AS ZN) <.004 LITHIUM.DISS(MG/I. AS LI) <.002 ZIRCONIUM BIS(HB/L 7R) <.004 MOLYBDENUM.DISS(MG/L-MO) <.1 ARSENIC.DISS(UG/L AG AS) 1.4

REMARKS: WATER HAS NO ODOR OR SHELL * FILTE R WAS VERY D IR T Y , S IL T 3 SAMPLE UAS COLLECTED IN A DUCKET FROM THE PUMP * SEND COPY TO P. 0 . BX, WHITE SULPHUR SPRINGS * OTHERS PERF5 ON INVENTORY FORM *

EXPLANATION: MG/L " MILLIGRAMS PER L IT E R , U G /L » MICROGRAMG PER L IT E R , MEO/L ■ HTLLIEOUIVELENTS PER L IT E R . FT ■ FEET, MT « METERS, (M> ■ MEASURED. (E ) ■ ESTIMATED, (R ) " REPORTED. TR - TOTAL RECOVERABLE. TOT «■ TOTAL. QU WA S2 H I OW PU AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 14 -S E P -8 1 b y : TP 3MJT PROCESSING p r o g r a m : F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 16-S EP -G 1 PERCENT MEQ/l. (FOR PIPER PLOT) CA MG NA CL S04 HC03 57 29 11 2 21 73

n o t e : i n correspondence , p l e a s e r e f e r t o la b n u m b e r : g i b i i i b

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 119

Sample Number WSS008 - Howard Zehntner

MONTANA ntlRljTAU OF MINES! AND GEOLOGY HATE!? QUALITY ANAl.Y!!IS BUTTIf .MONTANA 59701 < 4 0 6 ) 4 9 6 -4 1 0 1 I.AB NO. 0101119 STATE MONTANA COUNTY MEAOHER LATITUDE-LONGITUDE 46D34' 22' N 1 l o n s i ' s o U SITE LOCATION 9H 7E 5 ADAD UTM COORDINATE!) 713 N5157II00 E 510 415 MDMO S IT E USS008 TOPOGRAPHIC MAP WILLOW CREEK RESERVOIR 7 STATION ID 463422110515001 GEOLOGIC SOURCE 1 1 OALVM* * a SAMPLE SOURCE WELL DRAINAGE BASIN DC LAND SURFACE ALTITUDE AGENCY + SAMPLER MOMOSHSS SUSTAINED YIELD 5 . GPM BOTTLE NLINKER USSOOO YIELD MEAS METHOD BUCKET/STOPWATCH DATE SAMPLED 2 i- . ju i.~ a i TOTAL DEPTH OF HELL 42.3 FT TTHli SAMPLED 17130 HOURS GUI. ABOVE< - ) OR BELOW GS 26.0 FT LAD + ANALYST MBMQXFNA CASINO DIAMETER 6 IN (M ) DATE ANALYZED Ofl-AUG-Gl CASING TYPE STEEL SAHPLE HANDLING 31 2 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING SITE ZEHNTNER. HOWARD * SOURCE ALLUVIUM (QUATERNARY)GEOLOGIC MG/L ME 07 1. MG/L MEO/l. CALCIUM (CA) 5 4 .9 2 .7 4 BICARBONATE (H C 03) 2 4 0 .3 3 .9 4 MAGNESIUM (HG) 1 3 .6 1 .1 2 CARBONATE (C 05 ) 0. SODIUM (N A ) 6 .3 0.27 CHLORIDE (CL) 2 . 5 0 .0 7 POTASSIUM (K) 1.9 0.03 SULFATE ( S 0 4 ) 1 1 .3 0 .2 4 IRON (FE) <.002 NITRATE (AG N) .1 6 0,01 MANGANESE < .0 0 1 FLUORIDE 7 3 . 0 CNDUCTVY.FIELD MICROMHOS 1 0 0 0 . ALUMINUM, DISS (MO/l.-AL) <.03 NICKEL,DISS (MO/L AS NI> <.01 SILVER.DISS (MG/L AS AG) <.002 LEAD.DISS (MG/L AS PD) <.04 . BORON /DISS (MG/L AS B) <.02 STRONTIUM.DISS (MO/L-SR) ,24 CADMIUM.DISS(MG/I. AS CD) <.002 TITANIUM DIS(MG/L AS TJ> .023 CHROMIUH/ DIGS (HO/L-CR) <.002 VANADIUM.BISS(MO/L AS V) <.001 COPPER.DISS (MG/L AS Oil) <.002 ZINC,DISS (MG/L AS ZN) .024 LITHIUM.DISS(MG/L AS LI) <.002 ZIRCONIUM DIS(MG/L ZR) <.004 MOLYBDENUM.DIGS( MG/L-MO > <.1 ARSENIC,DISS(UG/I. AS AS) 1.6

REMARKS: HATER HAS NO ODOR OR SMELL 2 PH METER IS INOPERATIONAL X SEND COPY TO P . 0 . BOX 5 3 4 , UNITE SULPHUR SPRINGS, MT. *

EXPLANATION: MO/L « MILLIGRAMS PER L IT E R . IJO/L " MICROORAMS PER L IT E R , MEQ/l. M II.LIEQ UIVELENTS PER L IT E R . FT ' FEET, MT - METERS. >» MEASURED. « ESTIMATED, ■» REPORTED. TR * TOTAL RECOVERABLE. TOT - TOTAL. QU HA 02 HI OU PH AT OTHER OTHER AVAILABLE DATA Y OTHER FILE NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: I6 - 3 E P - 0 1 b y : TP *MJT PROCESSING p r o g r a m : F1730P V2 (8/9/80) p r i n t e d : 1 6-G E P -81 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 65 2 6 6 1 1 3 92

n o t e : INCORRESPONDENCE, PLEASE r e f e r TO LAB n u m b e r : 81S 1119 ANALYSIS NOT IN FILE:

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 120

Sample Number WSS009 - Spa Motel

MONTANA BUREAU OP MINES AND GEOLOGY UATER DUALITY ANALYSIS BUTTE,MONTANA 59701 (406)496-4101 I.AD NO. 0101120 ST ATI' MON'I ANA COUNTY MEAGHER LATITUDE-LONOITUBE 0 ' •) D ' ’U SITE LOCATION UTM COORDINATES Z N E MBMG SITE WSS009 TOPOGRAPHIC MAP WHITE SULPHUR OPRINOG 7 1 STATION ID GEOLOGIC SOURCC . * * * SAMPLE SOURCE WELL DRAINAGE BASIN LAND SURFACE ALTITUDE AGENCY + SAMPLER MDMG*.JLS SUSTAINED YIELD BOTTLE NUMBER WSSQO? YIELD MEAS METHOD DATE SAMPLED 2 2 - JU L -01 TOTAL DEPTH OF HELL TIME SAMPLED 0 0 ! 15 HOURS SUL A D O V E(-) OR BELOW GS .. „ LAB + ANALYST MBMGtFNA CASINO DIAMETER ™ (R> DATE ANALYZED OO-AUOt-OI CASING TYPE CONCRETE SAMPLE HANDLING 312 COMPLETION TYPE 0 1 * METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE RECREATIONAL SAMPLINO SITE SPA MOTEL * WHITE SULPHUR GPRINOS * GEOLOGIC SOURCE MG/L MEO/L MO/L MEO/l. CAl.CIUH (CA) 4 1 .7 2.0G BICARBONATE (HC03 > 0 0 4 . 1 3 .2 1 MAGNESIUM (MG) 9 . 3 0 .7 0 CARBONATE < C03 > 0. SODIUM (NA) 4 4 9 . 1 9 .5 3 CHLORIDE (CL ) 1 0 4 . 5 .2 5 POTASSIUM ( K > 1 7 .4 0 .4 3 SULFATE (S 0 4 ) 2 5 3 . S. 27 IRON (FE) .0 9 6 0.01 NITRATE (AS N ) .02 0.00 MANGANESE ( MN) .1 4 0.01 FLUORIDE (F) 7 .0 7 0 .3 7 S IL IC A (S 1 0 2 ) 4 7 .9 PHOSPHATE TOT (AO P ) TOTAL CATIONS 2 2 .0 5 TOTAL ANIONS 2 4 .1 0

STANDARD DEVIATION OF ANIO N-CATIO N BALANCE (SIOMA) 2 .7 9 LABORATORY PH 7 .2 3 TOTAL HARDNESS AS CAC03 1 4 3 .2 3 F IE L D WATER TEMPERATURE 4 7 . 3 C TOTAL ALKALINITY AS CAC03 6 6 1 .0 4 CALCULATED DISSOLVED SOLIDS 1400.07 SODIUM ADSORPTION RATIO 1 6 .3 3 SUM OF D IS S . CONSTITUENT 1 0 1 7 .8 3 RYZNAR S T A B IL IT Y INDEX 6 .8 9 LAB SPEC. COND. ( NICROHHOG/CM) 2370.1 LANGLIER SATURATION INDEX 0 .1 7 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. A IR (C) 4 5 . CNDUCTVY.FIELD MICROHHOS 2 3 7 0 . FIELD PH 6.05 ALUMINUM. DISC (MO/L -AL) < . 03 NICKEL.DISS (MO/L AS HI) .0 1 SILVER.DIOS (MG/L AS AG) < .0 0 2 LEAD.DISS (MO/L AS P»> <.04 BORON .DISS (MO/L AS B) 0 .20 STROHTIUM. DISS (M G /I.-S R ) 1 .9 7 CADMIUM.DISG(HG/I. AS r:n> < .0 0 2 TITANIUM DI0(H0/L AS TI) < .0 0 1 CHROMIUM.. D IS S (M O/L -CR) < .0 0 2 VANADIUM.DISS(MG/I. AS V) <.001 COPPER.DISS (MG/L AS CU) < .0 0 2 ZINC.DISS (HO/L AO ZN> < .0 0 4 LITHIUM.DISS(MG/L AS LI) .2 4 ZIRCONIUM BIS(MG/L ZR> < .0 0 4 MOLYBDENUM. D IO S ( MO/L' •MO) < .1 ARSENIC.DIS8(U0/L AS AS) 1.5

REMARKS! UATER IS CLEAR t H2S ODOR * SAMPLED AT POOL DURING FILLINO * 2S0 GPM MAX. SUSTAINED YIELD * LADJ FU CA OF 4 3 .1 M O /L. MO OF 1 0 . 1 . NA OF 469 AND K OF 1 7 .4 GIVES .4 0 5 LABI SIOMA * EXPLANATION: MG/L ■ MILLIGRAMS PER L IT E R . UG/L <» MICROGRAMO PER L IT E R . MEO/l. MILLIEOUIVELENTS PER LITER. FT <* FEET. MT • METERS. (M) MEASURED. (E) ESTIMATED. (R> - REPORTED. TR - TOTAL RECOVERABLE. TOT ■ TOTAL. OU UA 02 UI OU PU AT OTHER OTHER AVAILABLE DATA OTHER riLE NUMBERS!

PROJECT! c o s t : LAST EDIT BATE! 1 6 -8 E P -9 1 BY * TP *M JT PROCESSING PROGRAM! F1730P V2 (0/9/00) p r i n t e d : 1A -S E P -01 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL 004 HC03 9 3 05 1 21 21 34 note: in correspondence, please refer to lad number: 0101120

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 121

Sample Number WSS010 - Cow Palace

MONTANA BUREAU OF MINES AND GEOLOGY HATER QUALIVY ANALYSIS BUTTE,MONTANA 59701 (406)496-4t01 LAB NO. U 1 0 U 2 J STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE AAD3?'?7’N 110DS4'20'U SITE LOCATION 9N 6E 13 DAAA UTM COORDINATES 7.1?. N5153950 ES07250 MBMG S ITE USS01 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463227110542001 GEOLOGIC SOURCE 110ALVHS120SBMS* 3 SANPLE SOURCE HELL DRAINAGE BASIN BG LAND SURFACE ALTITUDE 5041. FT < 10 AGENCY + SAMPLER MBMG3USS SUSTAINED YIELD BOTTLE NUMBER H55010 YIELD MEAS METHOD DATE SAMPLED 2 2 - JU L -81 TOTAL DEPTH OF HELL 110. FT (R) TIME SAMPLED 11 1 0 0 HOURS SWI. A B O V E (-) OR BELOW GS 53.75 FT (M) LAB + ANALYST MBH03FNA CASINO DIAMETER 6 IN (R ) DATE ANALYZED OO-AUG-Ol CASING TYPE IRON SAMPLE HANDLING 312 COMPLETION TYPE 02* METHOD SAMPLED PUMPED PERFORATION INTERVAL GO TO 110 FT UATER USE DOMESTIC SAMPLING SITE COW PALACE 3 GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) MG/L MEO/L MG/L MEO/L CALCIUM (CA) 101. 5.04 DICARDONATE (H C 03) 4 4 5 . 7 .2 9 MAGNESIUM (MG) 1 8 .5 1 .5 2 CARBONATE (COE) O. SODIUM (NA) 2 5 0 . 10.00 CHLORIDE (CL) 1 7 7 . 4 .9 9 POTASSIUM (K> ia .3 0.47 SULFATE ( S04 > 2 6 4 . 5 .5 0 IRON (FE) .011 0.00 NITRATE (AS N ) 3 .0 9 0 . 2 8 MANGANESE (MN > <•001 FLUORIDE (F) .1 4 0.01 SILICA (SI02) 7 9 .7 PHOSPHATE TOT (AS P) TOTAL CATIONS 1 7 .9 1 TOTAL ANIONS 1 8 .0 7 STANDARD DEVIATION OF ANION-CATIO N BALANCE (SIOMA) 0 . 4 3 LABORATORY PH 7 .6 7 TOTAL HARDNESS AS CAC03 3 2 0 .3 4 FIE L D WATER TEMPERATURE 5 9 . F TOTAL ALKALINITY AS CAC03 3 6 4 .9 8 CALCULATED DISSOLVED SOLIDS 1 1 3 1 .7 5 SODIUM ABSORPTION RATIO 6.00 SUM OF DISC. CONSTITUENT 1 3 5 7 .5 4 RYZNAR S TA B ILITY INDEX 6.20 LAB SPEC.COND.(MICROHHOS/CM) 1 0 2 4 . LANGLIER SATURATION INDEX 0 .7 4 PARAMETER VALUE PARAMETS VALUE TEMPERATURE» AIR (C) 7 3 . CNDUCTVY.FIELD MICROMHOS 1 6 0 3 . ALUMINUM> BISS (MO/L-AL) < .0 3 NICKEL.DISS (MG/L AS NT) <.01 SILVER.BISS (MG/L AS AG) <.002 LEAD,DISS (MG/L AS PD) < .0 4 BORON .D IS S (M O /L AS B> 5 .6 2 STRONTIUM.DISS (M0/1.-SR) 1 .1 9 CADMIUM.DISS(MG/I. AS CD) <.002 TITANIUM D1S(HG/I. AS TI) .0 1 3 CHROMIUM. DIGS (MG/L-CR) <.002 VANADIUM.DISS(MG/L AS V) <.001 COPPER.DISS (MG/L AS CU> .1 3 7INC.DIS3 (MO/l. AG 7.N> .0 1 9 LITHIUM.DISS(MG/L AS LI) <.002 ZIRCONIUM DIG(MG/L ZR) < .0 0 4 MOLYBDENUM.DIGS(MG/L-MO) <.1 ARSENIC.DIGSdJG/l. AS AS) 0.1

REMARKS: UATER LEVEL MEASURED WHILE PUMPING * TEMPERATURE READING IS NOT ACCURATE * + OR - 2 F * SEND COPY TO! BOX 660. WHITE SULPHUR SPRINGS. MT. *

EXPLANATION: MG/L - MILLIGRAMS PER LITER. UG/L » M1CR0GRAMS PER LITER. MEO/L MILLIEOUIVELENTS PER LITER. FT - FEET, HT - METERS. (M) • MEASURED, (E) » ESTIMATED. - REPORTED. TR - TOTAL RECOVERABLE. TOT - TOTAL. OM UA HI OU PW AT OTHER OTHER AVAILABLE DATA Y Y OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 16-G E P -81 b y : TP 3MJT p r o c e s s in g p r o g r a m : F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 16 -S E P -0 1 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA CL S04 HC03 20 0 60 27 30 40 NOTE: IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER.* 0101121

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Sample Number WSS011 - James Lind

MONTANA BUREAU OF MINE!? AND OEOLOGY HATER QUALITY ANAI.YOIS BUTTEf MONTANA 5970.1 <406)496-4101 I. A ft NO. 0101122 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 46D73'09,N 110D57' 02*U SITE LOCATION 9N 7lf 0 cn cc UTM COORDINATES 712 NH155250 E500910 MSMO S ITE WSS011 TOPOGRAPHIC HAP WHITE SULPHUR SPRINGS 7 1 STATION ID 467709110570201 GEOLOGIC SOURCE UOALVM* • * * SAMPLE SOURCE WELL DRAINAGE BASIN DC LAND SIJRrACE ALTITUDE 5 0 6 5 . FT < 10 AGENCY I- SAMPLER MDHOSWGG SUSTAINED YIELD BOTTLE NUMBER WSS011 YIELD MEAS METHOD BATE SAMPLED 2 2 -J U L -8 1 TOTAL DEPTH OF HELL 6 0 . FT < R > TIME SAMPLED 09 1 4 5 HOURS SUI. ABOVE (••> OR BELOW GS 10. FT DATE ANALYZED OO-AUG-Ol CASING TYPE STEEL SAMPLE HANDLING .1 1 2 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING S ITE L IN D . JAMES * GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) HG/LMEQ/L MG/L MEO/L CALCIUM (CA) 6 1 . 7 3 .0 0 BICARBONATE (HC0.1) 2 7 0 .4 4 .4 3 MAGNESIUM (MO) 1 5 .7 1 .2 9 CARBONATE (COS) 0. SODIUM (NA) 1 9 .7 0 .0 6 CHLORIDE (CL) 14.0 0.39 POTASSIUM (K) 5.0 0.17 SULFATE (S04) 27.0 0.56 IRON (F E ) < . 0 0 2 NITRATE (AS N) .57 0 .0 4 MANGANESE (MN> < .0 0 1 FLUORIDE (F ) .2 9 0 . 0 2 SILICA (SI02) 4 6 . 7 PHOSPHATE TOT (AS P) TOTAL CATIONS 3 .3 6 TOTAL ANIONS 5 .4 4 STANDARD DEVIATION OF ANION-CATION BALANCE (SIOM A) 0 . 4 8 LABORATORY PH 7 .6 6 TOTAL HARDNESS AS CAC07 2 1 0 .6 9 FIELD WATER TEMPERATURE 46. F TOTAL ALKALINITY AS CAC03 2 2 1 .7 7 CALCULATED DISSOLVED SOLIDS .727.06 SODIUM ADSORPTION RATIO 0 .5 B SUM OF DISS. CONSTITUENT 461.06 RYZNAR S TA B ILITY INDEX 7 . 0 7 LAB SPEC.CONK.(MICROMHOS/CM) 509.0 LANGLIER SATURATION INDEX 0 .3 0 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 70. CNDUCTVY.FIELD MICROMIIOS 4 7 2 . ALUMINUM. DISS (HO/L-AL) <.03 NICKEL.DISS (MO/L AS NT) <.01 SILVER.DISS (MG/L AS AG) <.00? LEAD.DISS (HG/L AS PD) < .0 4 BORON . DISS (MO/L AGB) < . 0 2 STRONTIUM.DISS (MC/L-SR) .2 5 C ADM I UN f DISS (MG/I. AS CD) <.00? TITANIUM DIG(MG/L AS TI) .0 0 2 CHROMIUM. DISS (MO/I.-CR) <.002 VANADIUM.DISS(HG/L AS V) < .0 0 4 COPPER fDISS (MG/L AS CI1) .004 ZINC.DIGS . (HG/L AS ZN) .0 1 5 LITHIUH f DISS(MG/L AS LI) <.002 ZIRCONIUM DIS(HG/L ZR> < .0 0 4 MOL YDDENUM.DIGS(MG/L-MO) <.1 ARSENIC.DISS(UG/L AS AS) 7 .2

REMARKS! WATER HAS. NO COLOR OR ODOR * CAC03 DEPOSITS IN UASHINO MACHINE AND HOT UATER HEATER * SEND COPY TOSP.O.DX 5 6 7 . WHITE SULPHUR SPRINGS. M T. t

explanation : mg/ l - m i l l ig r a m s PER L IT E R . UO/l. - MICROORAMS PER L IT E R . MEQ/L MILLIEOUIVELENTS PER LITER. FT - FEFT. MT - METERS. (M> - MEASURED. (G> ■ ESTIMATED. (R) » REPORTED. TR « TOTAL RECOVERABLE. TOT » TOTAL.

QW WA S2 WI OW PU AT o th e r OTHER AVAILABLE DATA Y Y OTHER F IL E NUHBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 1 6 -S E P -fll BY • TP *MJT PROCESSING p r o g r a m : F1770P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 16-SF.P-G1 PERCENT MEQ/l. (FOR PIPER PLOT) CA MG NA K CL 0 0 4 HC03 57 24 13 2 7 10 31 note: in correspondence, please refer to lad number: 0101122

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Sample Number WSS013 - B ill Skelton

MONTANA BUREAU OF HINES AND GEOLOGY UATl'R QUALITY ANALYSIS BUTTF.MONTANA 59701 (406>496-4101 LAB NO. 0101123 STA TE MONTANA COUNTY MEAGHER LATITUDE- LONGITUDE 46D30'24•N 11 0DS7'23'U SITE LOCATION 9N AE 27 DCBC UTM COORDINATES 712 N5150170 E503330 MBMO SITE USS013 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 4 43024110572301 GEOLOGIC SOURCE * * * SAMPLE SOURCE UELL DRAINAGE BASIN DC LAND SURFACE ALTITUDE 4 9 5 3 • FT < 10 AOENCY + SAMPLER M0MGSJLS SUSTAINED YIELD BOTTLE NUMBER WSS0.13 YIELD MEAS METHOD DATE SAMPLED. 2 0 -J U L -8 1 TOTAL DEPTH OF UELL 22. FT (R ) TIME SAMPLED 14100 HOUR SUL ABOVE( - ) OR BELOH OS LAD I- ANALYST MDMG3FNA CASINO DIAMETER 36 $N DATE ANALYZED Ofl-AUG-81 CASING TYPE CONCRETE SAMPLE HANDLIHO 312 COMPLETION TYPE 01* MFTHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE SAMPLING SITE SKELTON. D IL L * RANCH 4 MI SM OF TOWN GEOLOGIC SOURCE

MG/L MEO/L MG/L MEO/L CALCIUM (CA) 5 2 ,8 2 . 6 3 BICARBONATE (H C 03) 1 6 3 .0 2 . 6 7 MAGNESIUM (MG) 1 4 .1 1 .1 6 CARBONATE (C 0 3 ) 0. SODIUM (NA) 1 6 .2 0 .7 0 CHLORIDE (CL) 2 9 .3 0 . 3 3 POTASSIUM (K) 7.1 0.05 SULFATE (S04) 4 3 .6 0 .9 1 IRON (F E ) .0 1 3 0.00 NITRATE (AS N) 3 .3 7 0 . 2 3 MANGANESE (MN) < .0 0 1 FLUORIDE(F) .1 9 0.01 SILICA (SI02) 2 1 . 0 PHOSPHATE TOT (AS P) TOTAI. CATIONS 4 .3 3 TOTALANIONS 4 .6 7 STANDARD DEVIATION OF ANION-CATIO N DALANCE (SIOMA) 0.67 LABORATORY PH 7 . 3 7 TOTAL HARDNESS AS CAC03 1 0 9 . GO FIE L D HATER TEMPERATURE 9 . 0 TOTAL A LK A LIN ITY AS CAC03 1 3 3 .6 9 CALCULATED DISSOLVED SOLIDS 263.17 SODIUM ADSORPTION RATIO 0 .5 1 SUM OF DISS. CONSTITUENT 345.38 RYZNAR S T A B IL IT Y INDEX 7 .9 3 LAB SPEC.COND.(MICROMHOS/CM) 4 7 0 .5 LANGLIER SATURATION INDEX -0.70 PARAMETER VALUE PARAMETER VALUE CNDUCTVY.FIELD MICROMHOS 465. FIELD PH 7.54 ALUMINUM. DISS (MO/L-AL) <.03 NICKEL.DISS (MO/L AS NI) <.01 SILVER.DISS (MG/L AS AG) <.007 LEAD.DISS (MG/L AO PD) <.04 BORON .D IS S (M G /L AS B> <.02 STRONTIUM.DISS (MO/L-SR) ,33 CADMIUM.DISS(MG/I. AS CD) <.007 TITANIUM DI5(MG/I. AO TI) .005 CHROMIUM. DISS (MO/L-CR) <.002 VANADIUM.DISS(MO/l. AS V) <.001 COPPER.DISS (M G/L AS CU) .021 ZINC.DISS' (MG/L AS ZN> .12 LITHIUM.DISS(MG/L AS LI) <.002 ZIRCONIUM DIG(MG/I. ZR) <.04 MOLYBDENUM.DISS(MG/L-MO) <.1 ARSENIC,DISS(UG/I. AS AO) .8

REMARKS! UATER IS CLEAR * NO COLOR OR TASTE NOTED * OUNER DOES NOT WANT M .L . MEASURED * SAMPLED AT OUTSIDE HYDRANT THROUGH HOSE * UL H IT H IN 6 FT OF LAND SURFACE IN SPRINO *

explanation : mg/ l - MILLIGRAMS pe r L IT E R . UO/L - MICROGRAMS p e r l i t e r , m c o / i. MILLIEOUIVELENTS PER LITER. FT » FEET. MT - METERS. (M) - MEASURED, (E) - ESTIMATED..(R) « REPORTED. TR • TOTAL RECOVERABLE. TOT - TOTAL. QU UA S2 HI OU PU AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS:

PROJECT! c o s t : LAST EDIT DATE: 16-SEP-81 b y : TP *MJT PROCESSING PROGRAM: F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 16“SEP-01 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 57 25 15 1 17 19 57 NOTE: IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER.* 0 1 0 1 1 2 3

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 124

Sample Number WSS014A - B ill C o rk ill - T ra ile r Well

MONTANA BUREAU ill- HtNI.il AMI) OLOLOOY WATER OUALITY ANALYSIS BUTTE,MONTANA 59701 ( 406)496 •-UO.t LAB NO. (1101133 STrt n.- MONTANA COUNTY MEAGHER LATITUDE LONG.IT UDE 4/.D30'lft'N tlOOAA'SS’W SITE LOCATION 9N 7E ?5 DOCD UTM COORDINATES 212 MSI 49995 E5I/.740 ...... ITMflMO SITE L USS014A TOPOGRAPHIC NAP WILLOW CREEK RESERVOIR TATION Hi 4/,::o i b i i o 4/,5.,; o i g e o l o g ic s o u r c e 11OAl. VMS 1 20TRRC* LE SOURCE DRAINAGE BASIN DC LAND ALT ITUDE 50.10. PT < 10 AGENCY I SAMPLER HDMG3JL.S NEO Y tE I.I B O TH IT NUMBER WGS014A YI AO METHOD DATE SAMPLED 30 -,JUL --31 TOTA -pr H OF UELL 9/>...... i FT < R > TIM E SAMPLED I? .*00 HOURS 3UL A BO VI: OR: BELOW SO 3 0 .1 7 PT LAD L ANALYST HBM03ENA IHOi DIAMETER /, IN DATE ANALYZED 0 0 - OCT-0 1 CA SINO TYPE STEEL SAMPLE HAMBLINO .1131 COMPLEITION TYPE METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE INDUSTRIAL SAMPLING SITE CORKILL. DILL « GEOLOGIC SOURCE ALLUVIUM (lit)A TERNARY) MG/L MEO/L MG/L MEO/L CALCIUM (CA) S/,.7 2.03 BICARBONATE (HC03) 303.7 3 .3 4 MAGNESIUM (MG) n./» 0 .7 1 CARBONATE (0 0 3 ) 0 . SODIUM (NA) 7.7 0.33CHLORIDE (Cl.) 0.5 0 . 2 4 POTASSIUM (K) 2.3 0.06 SULFATE (0 04 ) 1 7 .5 0 .3 /, IRON (F E ) < .0 0 3 NITRATE (AS H) .0 9 0 . 0 a MANGANESE (MN) < .0 0 1 FLUORIDE ( F ) .24 0 .0 1 SILICA (SI02) 3 5 .4 PHOSPHATE TOT (AS P) TOTAL CATIONS 3 .9 3 TOTAL ANIONS 4 . 0 2 STANDARD DEVIATION OF ANION-CATIO N BALANCE (STOMA) 0 .5 3 LABORATORY PH 7 .7 4 TOTAL HARDNESS AS CAC03 1 7 0 .9 0 FIE L D UATER TEMPERATURE 9 . 0 C TOTAL A LK A LINITY AS CAC03 1 A 7 .0 7 CALCULATED DISSOLVED SOLIDS 330.37 SODIUM ADSORPTION RATIO 0.23 SUM OF DISS. CONSTITUENT 341.73 RYZNAR S T A B IL IT Y INDEX 7 .3 1 LAB SPEC. COND. < .0 2 STRONTIUM,DISS (MO/L-SR) .17 CADMIUM,DI5S(MG/L AS CD) <.00? TITANIUM DIO(MG/L AS TI) <.001 CHROMIUM, DISS (M O /L -C R ) < .0 0 3 VANADIUM,DISG(MO/L AS V) .001 COPPER,DIOS (M G/L AO GU) .0 0 3 7 I N C , D l 00 (MG/L AS 2N) .00 7 LITHIUM,DIOS(MG/L AS 1.1) <.002 ZIRCONIUM DIG(HG/L ZR) <.004 MOL YDIIENUM. DIOS ( MG/L • HO) < . 1 AROfHTC, DIO G (UG /l. AS AO) 3 ./,

REMARKS: WATER IS OASSY X NO ODOR OR TASTE CHARACTERISTICS S 1ST TRAILER BY WtLL

EXPLANATION! MG/I. * MILLIGRAMS PER LITER, UG/L ” MICROGRAMS PER L IT E R , MEP/L MILLIEOUIVELENTS PER LITER. FT ■» FEET, NT » METERS. (M) " MEASURED, (E> ESTIMATED. (R) REPORTED. TR TOTAL RECOVERABLE. TOT «■ TOTAL. OU UA S3 NT OU PU AT OTHER OTHER AVA ILAOI.E DATA Y OTHER F IL E NUMBERS:

PROJECT I c o s t : LAST EDIT DATE! 09 ••OCT-fll TP 3MJT PROCESSING PROGRAH! F1730P V? ( 0 / 9 / 0 0 ) PRINTED! 31 • OCT-01 PERCENT MEO/L (FOR PIPER PLOT) CA MG HA K CL S04 HC03 71 17 0 1 5 9 03 NOTE: IN CORRESPONDENCE, PLEASE REFER TO LAD NUMBER! O l O l i :

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 125

Sample Number WSS014B - B ill C o rk ill - Welding School

MONTANA BUREAU o r NINES AND GEOLOGY WATER QUALITY ANALYSIS BUTTE,MONTANA 09/01 (406)496-4101 LAB HO. 01 0115 4 STATE MONTANA COUNTY MEAGHER l a t i t u d e - i .o n o it u b e 46050'10'N 11 ODSA'ZB'W RITE LOCATION 9N 6E 2 5 DDCD UTM COORDINATES ? N C MBMG S IT r topographic hap WHITE SULPHUR SPRINGS 7 1 STATION ID 40.1010110542001 g e o l o g ic s o u r c e UOTKRCX « X SAMPLE SOURCE HELL DRAINAGE DAS IN DC LAND SURFACE ALTITUDE 5 0 5 0 . FT < 10 AGENCY + SAMPLER NDMGXJLS SUSTAINED YIELD BOTTLE NUMBER USS014B YIELD HEAR METHOD DATE1 SAMPLED 2 0 —JU L -01 TOTAL DEPTH 01- HELL 9 6 . FT (R) TIME SAMPLED 1 9 S00 HOURS RUL ADOBE (-•> OR DELOU OR 5 5 .1 7 FT LAB + ANALYST HBMGXFNA CASINO DIAMETER 6 IN (E ) DATE ANALYZED O lI-A U O -G l CASINO TYPE STEEL SAMPLE NANDI. ING 212 COMPLETION TYPE METHOD SAMPLED PUMPED PERFORATION INTERVAL WATER USE INDUSTRIAL SAMPLING RITE CORRILL, DILL X WELDING SCHOOL GEOLOGIC SOURCE TERRACE DEPOSITS (QUATERNARY) HG/L MEQ/L MG/l. MEQ/L CALCIUM (CA) 57.2 2.05 BICARBONATE (H C 03) MAGNESIUM (MG) 0 .6 0 .7 1 CARBONATE (C05) SODIUM (HA) 7.9 0.34 CHLORIDE (Cl.) POTASSIUM (K) 2 .4 0 . 0 6 SULFATE < R04 > IRON (FE) < .0 0 ? NITRATE (AS N) MANGANESE (MN> . < .0 0 1 FLUORIDE (F) S IL IC A (fl1102) 3 5 . a THOSPHATE TOT (AS P) TOTAL CATIONS 5 . 9 7 TOTAL ANIONS STANDARD DEVIATIO N OF ANION-CATION BALANCE (S10MA) LABORATORY PH TOTAL HARDNESS AR CAC05 1 7 0 .2 3 FIELD WATER TEMPERATURE 9 . 0 C TOTAL A LK A LIN ITY AS CAC03 CALCULATED DISSOLVED SOLIDS SODIUM ADSORPTION RATIO 0 . 2 6 SUM OF ni3S. CONSTITUENT RYZNAR S TA B ILITY INDEX LAD GPEC.COND,(MICROHHOR/CM) LANOLIER SATURATION INDEX PARAMETER VALUE PARAMETER VALUE CNDUCTVY, FIE LD MICROMHOS 595. FIELD PH 7 .6 7 ALUMINUM. BISS (HG/I.-AL) <.03 NICKEL.DIRS (HG/L AS NI) <.01 SILVER/DISS (HO/L AS AS) <.002 LEAD.DIRS (MO/L AS PD> < .0 4 BCIROH > DIBS (H O /L AS B> <.02 STRONTIUM .DIRS (MG/I.-SR) .1 7 CADMIUM.DIRS(HO/L AS CD) <,002 TITANIUM D(S(MO/l. AS TI) <.001 CHROMIUM. DISS (H R /I.-C R ) < .0 0 2 VAN AD1UM. DISS (MG/I. AS V) .004 COPPER, DIRS (HO/L AS GU) .00/. ZINC, DISS (MO/L AS ZN) .040 LITHIUM.DIRR(HO/L AS L I) <.00? ZIRCONIUM .DIR (HO/I. ZR) < .00 4 MOLYBDENUM.DISS(MO/L-MO) < .1 ARSENIC, D.fSf>( IJO/L AR AS) 5 . 7

r e m a r k s : w a ter i s g a s s y x no odor or t a s t e characteristics X COLLECTED FROM BATHROOM AT WELDINO SCHOOL X PUMP WAS RUNNINO X

EXPLANATION: H R /I. » MILLIGRAMS PER L IT E R . IJG/L * MICROGRAMS PER L IT E R . HER/L MI'LLIEOUIVGLEMTS PER L IT E R . FT » FEET, MT •• METERS. (M> ■« MEASURED, (E ) - ESTIMATED. (R) " REPORT Ell. TR • TOTAL RECOVERABLE. TOT ~ TOTAL. QW WA 32 UI OW PU AT OTHER OTHER AVAILABLE DATA Y OTHER FILE n u m b e r s :

p r o j e c t : c o s t : LAST EDIT DATE! 16-SEP-31 b y : rp XMJT PROCESSING PROGRAM! F1730P V? (G /9 /S 0 ) p r i n t e d : 16' SEP-OJ PERCENT MEO/I. (FOR PIPER P L O D CA MG NA K CL S04 HC03 71 17 0 1 0 0 0 NOTE I IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER: 01R1134

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Sample Number WSS015 - Deters House

MONTANA BUREAU OF MINES AND GEOLOGY HATER QUALITY ANALYSIS BUTTE.MONTANA 39701 (406)496-4101 LAB NO. 0101124 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 46D31 ' 45' N 110D54 ' 32•W SITE LOCATION 9N 6F 24 ABB UTM COORDINATES 712 NS152630 E306995 MONO S ITE WSS015 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463145110543201 GEOLOGIC SOURCE U0ALVM3120TRRC* * SAMPLE SOURCE HELL DRAINAGE DASIN DC LAND SURFACE ALTITUDE 3033. FT < 10 AGENCY + SAMPt.ER MBM03.JLS SUSTAINED YIELD 5 0 . CFS BOTTLE NIJHPER WSS015 YIELD MEAS METHOD REPORTED DATE SAMPLED 2 1 - JU L -8 1 TOTAL DEPTH OF HELL GO. FT < R) TIME SAMPLED 09 1 0 5 HOURS OWL ABOVE(-> OR BELOW GO 3 2 . FT (R> LAD + ANALYST HDH03FNA CASINO DIAMETER 6 IN DATE ANALYZED OO-AUG-fll CASIHG TYPE STEEL SAMPLE HANDLING 312 COMPLETION TYPE 0 4 * METHOD SAMPLED PUMPED PERFORATION INTERVAL 79 TO SO FT UATER USE DOHESTIC SAMPLING SITE DETERS MOLISE*.5 M S WHITE SULPHUR SPRINGS GEOLOGIC SOURCE ALLUVIUM HG/L MEG/I. MG/L MEO/L CALCIUM(CA) 7 4 .8 3 . 7 3 BICARBONATE (H C 03) 2 9 1 .8 4 .7 8 MAGNESIUM (MG) 2 2 .6 1 .0 6 CARBONATE ( C 0 3 ) 0. SODIUM (NA) 2 3 .4 1.10 CHLORIDE ( Cl.) 3 0 .7 0 . 8 7 POTASSIUM (K ) 3 . 7 0.13 SULFATE (S 0 4 ) 4 3 .6 0 .9 1 IRON (FE> .0 1 6 0.00 NITRATE (AS N) 2 .2 3 0 . 1 6 MANGANESE (MN) .0 0 1 0.00 FLUORIDE (F) .1 9 0.01 SILICA (SI02) 44.0 PHOSPHATE TOT (AS P) TOTAL CATIONS 6.84 TOTAL ANIONS 6 . 7 3 STANDARD DEVIATION OF ANION-CATION DAL.ANCE (SIGMA) - 0 . 3 8 LABORATORY PH 7 .7 9 TOTAL HARDNESS AS CAC03 2 7 9 .0 0 FIELD WATER TEMPERATURE 9.7 C TOTAL ALKALINITY AO CAC03 2 3 9 .3 3 CALCULATED DISSOLVED SOLIDS 392.90 SODIUM ADSORPTION RATIO 0.66 SUM OF DISS. CONSTITUENT 541.04 RYZNAR O TAD ILITY INDEX 6 .7 0 LAD SPEC.COND.(MICROHHOS/CM) 650.3 LANGLIER SATURATION INDEX 0 .3 4 PARAMETER VALUE PARAMETER VALUE CNDUCTVY.FIELD MICROMHOS 667. FIELD PH 7 .6 4 ALUMINUM. DISS (MG/L-AL) <.03 NICKEL.DISS (MO/L AS NI) <.01 SILVER.DISS (MG/L AS AG) <.002 STRONTIUM.DISS (MG/L-BR) .5 2 BORON .DISS (MG/L AS B) <.02 TITANIUM DIS(MO/L AiS TI) .010 CADMIUM.DIGS(MG/I. AS CD) <.002 VANADIUM.DIGS(MG/L AS V) .0 0 4 CHROMIUH. DISS (HG/L-CR) <.002 ZINC.DISS (MO/L AS ZN) < •0 0 4 COPPER.DIOS (MG/L AO CM) .000 ZIRCONIUM. DIS(MG/L ZR) < .0 0 4 LITHIUM.DISS(MO/L AS LI) <.002 ARSENIC.DISO(UO/L AS AS) 2 .3 MOLYBDENUM. DISS(MG/L-MO) <.1 LFAD.DISS (MG/L AS PB>

r e m a r k s : w a ter i s c l e a r - HAS a t r a c e o f s a n d * NO ONE HOME * NO WL t SAMPLED THROUGH HOSE

EXPLANATION! MO/L ■ MILLIGRAMS PER L IT E R . UG/L ■ MICROGRAMS PER L IT E R . MEQ/L MILLIEQUIVELENTS PER LITER. FT * FEET. MT - METERS. (M) - MEASURED. (E) - ESTIMATED. (R) ■ REPORTED. TR ■ TOTAL RECOVERABLE. TOT - TOTAL. QW WA HI OW PW AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 1 6 -5 E P -8 1 b y : TP *MJT p r o c e s s in g p r o g r a m : F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 1 6 -S E P -01 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL 504 HC03 54 27 16 2 12 13 71 NOTE! IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER: 01R 1124

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Sample Number WSS016 - Ronald Jackson - T ra ile r Well

MONTANA BUREAU OF MINES AND GEOLOGY WATER OUALITY ANALYS5IS BUTTE*MONTANA 59701 ( 404)494-'I-t01 L AD NO. 0 1 0 1 1 2 3 STATE MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 44 n 3 2 '3 4 ’ N 11 ODSA'GP'U SITE LOCATION 9N 4E 11 CCDD UTM COORDINATES 7.1?. N 3 I5 4 0 5 0 E504433 MBHG SITE WSS014 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 443254110543201 GEOLOGIC SOURCE UOALVM* * S SAMPLE SOURCE WELL DRAINAGE BASIN DC LAND SURFACE ALTITUDE 4 9 4 3 . FT < 10 AGENCY + SAMPLER MDHO*JLS SUSTAINED YIELD BOTTLE NUMBER USS1 6 Y IE LD MIIAG METHOD DATE SAMPLED 2 1 —JUL—81 TOTAL DEPTH OF WELL 43. FT (R ) TIME SAMPLED o n :ift hour SWI. ABOVE!-> OR BELOW OS 7. FT (R ) LAD + ANALYST MBMOtFNA CASINO DIAMETER 6 IN (H ) DATE ANALYZED CASING TYPE STEEL SAMPLE HANDLINR .1120 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING SITE JACKSON.RONALD * TRAILER WEL1 GEOLOGIC SOURCE ALLUVIUM (QUATERNARY) MG/L MEO/I. MG/L MEO/l CALCIUM (CA) 4 9 .1 3 .4 3 DICARDONATE (HC03) 2 0 3 .5 4 .4 8 MAGNESIUM (MG) 1 5 .0 1 .2 3 CARBONATE (C 0 3 ) 0 . SODIUM (NA) 7 .8 0 .3 4 CHLORIDE (C l.) 4 .2 0 . 1 2 POTASSIUM (K> 1.7 0.04 SULFATE (S04 ) 13. fi 0 .2 9 IRON (F E ) .0 0 4 0 .0 0 NITRATE (AG N) .3 4 0 . 0 2 MANGANESE (MN) .0 0 2 0.00 FLUORIDE .4 5 0 .0 2 SILICA (SI02) 1 0 .7 PHOSPHATE TOT (AS P> TOTAL CATIONS 5 .0 7 TOTAL ANIONS 5 . 1 3 STANDARD DEVIATION OF ANION-CATION BALANCE (SIGM A) 0 . 3 7 LABORATORY PH 7 .7 2 TOTAL HARDNESS AS CAC03 2 3 4 .7 9 FIE L D WATER TEMPERATURE 9. TOTAL ALKALINITY AS CAC03 2 3 4 .1 4 CALCULATED DISSOLVED SOLIDS 271.74 SODIUM ADSORPTION RATIO 0.22 SUM OF DISS. CONSTITUENT 414.40 RYZNAR STABILITY INDEX 4 .8 4 LAD SPEC.COND. <.002 ZINC,DISS' (MG/L AS ZN> .0 0 4 LITHIUM, niSS(HG/l. AS I..I) <.002 ZIRCONIUM DIS

r e m a r k s : w a ter i s c l e a r , h a s no o d g r s d e g a s s e d s l i g h t l y * P ITL E S S ADAPTER * NO HI. MEASUREMENT t NEW WELL(SANDY) * SAMPLED THROUGH HOSE * 1 .3 H I NW WHITE SULPHUR SPRINGS, MT.

explanation : MG/L - MILLIGRAMS p e r l i t e r , U G /L - MICROGRAMS PER L IT E R . MfiO/l. MILLIEOUIVELENTS PER LITER. FT » FEET, MT METERS. (M > ■ MEASURED. (E ) - ESTIMATED, " REPORTED. TR - TOTAL RECOVERABLE. TOT - TOTAL. QU WA S2 UI OW PW AT OTHER OTHER AVAILABLE DATA OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 1A-5EP- 81 b y : TP *MJT PROCESSTNG PROGRAM: F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 1A -8EP -G 1 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL S04 HCG3 40 24 4 0 2 5 91 NOTES IN CORRESPONDENCE, PLEASE REFER TO LAD NUMBER: 0 1 0 U 2 S

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Sample Number WSS017 - Wallace Bailey - House Well

MONTANA BUREAU OF MINER AND OEIH.OCY WATER QUAL. IT T ANALYRIS BUTTE,MONTANA 59701 (406)496-4101 LAB NO. 0101126 STATE MONTANA COUNTY MEAGHER LATITUDE-I.ONGITUDE 4 6 D 3 1 ' 16 * N 11 0D S 3' 1 9 • W R ITE LOCATION 9M 71; 19 DDC3 UTM COORDINATES 712 H5X51650 E 5 0 0 1 2 1 0 MBMO R IT E WGR017 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463116110531901 GEOLOGIC SOURCE * * 3 SAMPLE SOURCE WELL DRAINAGE BASIN DC LAND SURFACE ALTITUDE 5 1 0 0 . FT < 10 AGENCY + SAMPLER HDMOSJLS SUSTAINED YIELD BOTTLE NUMBER WGS017 Y IE LD MEAG METHOD DATE SAMPLED 2 1 -J U L -8 1 TOTAL DEPTH OF WELL 1 0 4 . FT TIME SAMPLED 10 * 30 HOURS OWL ABOVE!-> OR DELON GS LAB + ANALYST MDMOSFNA CASINO DIAMETER 6 IN DATE ANALYZED 0 0 -A U G -81 CARING TYPE STEEL SAMPLE HANDLING 31 2 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL 130 TO 104 FT (R> WATER USE DOMESTIC AND STOCK SAMPLING S IT E B A ILE Y . WALLACE L . t HOUSE WELL * GEOLOGIC SOURCE MG/L MFQ/L MG/L MKR/L CALCIUM (CA) 5 2 .2 2.60 BICARBONATE (HC03) 110.1 1 .9 4 MAGHESIUH (MG) 1 6 .7 1 . 3 7 CARBONATE (C 03 ) 0. SODIUM (NA) 4 0 .2 1.75 CHLORIDE (CL) 5 0 .4 1 .4 2 POTASSIUM (K) 5 .7 0.15 SULFATE ( S 0 4 ) 120.0 2 .5 0 IRON (FE> .0 1 6 0.00 NITRATE (AS N) 1 .4 2 0.10 MANGANESE (MN) .001 0.00 FLUORIDE (F) .37 0.02 SILICA (SI02) 5 9 .3 PHOSPHATE TOT (AS P) TOTAL CATIONS 5 .8 7 TOTAL ANIONS 5 .9 8 STANDARD D EVIA TIO N OF ANION-CATION BALANCE (SIG M A) 0 .5 3 LABORATORY PH 7 . 6 0 TOTAL HARDNESS AS CAC03 1 9 9 .0 8 FIELD WATER TEMPERATURE 1 1 . C TOTAL A LK A LIN ITY AS GAC03 9 6 .8 6 CALCULATED DISSOLVED SOLIDS 404.40 SODIUM ADSORPTION RATIO 1 .2 4 SUM OF DIRS. CONSTITUENT 464.41 RY7NAR STABILITY INDEX 7 .9 9 LAB SPEC.COND.(HICROMIIOS/CM) 624.5 LANGLIER SATURATION INDEX - 0.20 PARAMETER VALUE PARAMETER VALUE CNDUCTVY.FIELD MICROMHOS 6 3 1 . F IE L D PH 7 . 9 6 ALUMINUM. DISS (HO/L-AL) <.03 N IC K E L .D IS S (M G /L AS NI> <.01 SILVER.DISS (MO/L AS AG) <.002 STRONTIUM.DIOS (MG/L-SR) .3 5 BORON .D IR S (H G /L AS B> < .0 2 TITANIUM DIG(MO/L AG TI> .0 0 7 CADMIUM.OISS(MG/l. AS CD) <.002 VANADIUM.-DISS (MG/l. AS V) .0 0 6 CHROMIUM. DIRS (M G /L -C R ) < .0 0 2 ZINC.DISS (MO/L AS 7N) .0 8 9 COPPER.DIRS (HG/L AS CU> <.002 ZIRCONIUM DIG(MG/L ZR) < .0 0 4 LITHIUM.DIS0(MG/L AO l.t) <.002 ARSENIC.DISS(UO/L AS AS) 2.2 MOLYBDENUM.DIRS(MG/L-MO) <.1 LEAD.DISS (MU/I. AS PD)

REMARKS.* WATER IS CLEAR * SAMPLED FROM HYDRANT BY CORRAL (WESTS ID E ) * STEEL CAGING TO 1 2 7 ' * PVC 127 TO 104 * PROBABLY PERFORATED WITH D RILL IN THE PVC * PVC DIAMETER UNKNOUN <

EXPLANATION! MG/l. - MILLIGRAMS PER L IT E R . UG/L - MICROGRAMS PER L IT E R . MEQ/L MTLLIEQUIVELENTS PER L IT E R . FT - FEET, MT « METERS. (M> » MEASURED. (E) - ESTIMATFD. (R) « REPORTED. TR > TOTAL RECOVERABLE. TOT - TOTAL. OW WA S2 UI OW PW AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS: PROJECT! COST! LAST EDIT DATE! 16-R E P -B 1 BY! TP *MJT PROCESSING p r o g r a m : F1730P V2 (0/9/00) PRINTED: 16-SEP-01 PERCENT MEG/l. (FOR PIPER PLOT) CA MG NA K Cl. S04 HC03 44 23 29 2 23 41 32 note: in correspondence, please refer to lad number: 0101126

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 129

Sample Number WSS018 - King Wilson - Poor Farm - Sportsmans Lodge

MONTANA BUREAU OF MINES AND GEOLOGY WATER QUALITY ANALYSIS BUTTE.HONTANA 59701 (404>494-4101 I.AB NO. 0 1 0 1 1 2 7 STATE MONTANA COUNTY MEAOHER LATITUDE-LONGITUBE 4 4 D 3 2 '3 3 'N 11 0n53'lA*W SITE LOCATION 9M 6E 13 BCDA UTM COORDINATES Z12 NS134110 E504045 NBHO SITE USS01S TOPOGRAPHIC HAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463233110531401 GEOLQOIC SOURCE X * * SAMPLE SOURCE WELL DRAINAGE BASIN DC LAND SURFACE ALTITUDE 4993. FT < 10 AGENCY + SAMPLER MDMOX.JLS SUSTAINED YIELD BOTTLE NUMBER WSS01G YIELD MEAS METHOD DATE SAMPLED 2 1 -J U L -8 1 TOTAL DEPTH OF WELL 1 2 3 . FT TIM E SAMPLED 11 M S HOURS SUL ABOVE( - > OR BELOM GS 4 0 . FT ( R ) LAD + ANALYST MDMOXFNA CASINO DIAMETER DATE ANALYZED OB-AIJG-Ol CASING TYPE SAMPLE HANDLING 312 COMPLETION TYPE METHOD SAMPLED PUMPED PERFORATION INTERVAL WATER USE PUBLIC SUPPLY SAMPLING SITE WILSON# KING * POOR FARM XSPORTSHANS LODGE GEOLOOIC SOURCE MG/L MER/L MG/L MER/L CALCIUM (CA) 1 .7 0 . 0 0 BICARBONATE ( H C 03) 3 2 4 . 5 .3 4 MAGNESIUM (MG) .5 0 .0 4 CARBONATE (C 0 3 ) 5 1 .0 1 .7 3 SODIUM (NA) 100. 7.03 CHLORIDE (CL) 9 . 5 0 . 2 7 POTASSIUM (K > .9 0.02 SULFATE (S 0 4 ) 3 9 .1 0.G1 IRON (F E ) <•002 NITRATE (AS N> .1 4 0.01 HANGANESE (HN) <.001 FLUORIDE (F) 2 .2 S 0.12 SILICA (SI02) 1 9 .0 PHOSPHATE TOT (AS P) TOTAL CATIONS 7.90 TOTAL ANIONS S .2 S STANDARD D EVIATIO N OF ANIO N-CATIO N BALANCE (SIONA) 1 .3 5 LABORATORY PH 9 .2 0 TOTAL HARDNESS AS CAC03 4 .3 0 FIELD WATER TEMPERATURE 11.4 C TOTAL A LK A LIN ITY AS CAC03 3 3 3 .7 7 CALCULATED DISSOLVED SOLIDS 443.51 SODIUM ADSORPTION RATIO 3 1 .2 0 SUM OF DISS. CONSTITUENT 030.92 RYZNAR S T A B IL IT Y INDEX 0 .2 4 LAB SPEC. COND. ( HICRfJMHOS/CM) 8 0 0 .2 LANGLIER SATURATION INDEX 0 .4 8 PARAMETER VALUE PARAMETER VALUE CNDUCTVY.FIELD MICROMHOS 8 2 0 . FIELD PH 9 .3 0 ALUMINUM. DISS (HO/l.-AL) <.02 NICKEL/DIGS (MO/L AS NI) <.01 SILVER.DISS (MG/L AS AG) <.002 STRONTIUM.DISS (MB/I.-SR) .0 1 7 BORON . D CSS (M O /L AS B) 2 .1 4 TITANIUM DIS(MO/L AS TI) <.001 CADM IUM .DIG S(M G /L AS CI1) <.00? VANADIUM.DISS(HR/L AS V) .0 0 5 CHROMIUM. DISS (HG/I.-CR) <.002 ZINC.DIGS - (MG/L AG 7N) < .0 0 3 COPPER.DISS (MG/L AS CU> <.002 ZIRCONIUM DIS(MG/L ZR> < .0 0 4 LITHIUM.BISS(MG/L AS 1.1) <.002 ARSENIC. DIGS(UG/I. AS AS) 22.6 MOLYBDENUM. D IS S (M G /I.-M O ) < .1 LEAD.DISS (HG/L AS PD)

REMARKS! WATER IS VERY OASSY X HIGH C02 ? * MAIL COPY TO! P .O . DX 4 5 2 . WHITE SULPHUR SPRING S. MT. * NEW(1 9 7 6 ) WELL IN OLD WELL HOUSE ? LAD! FU CA OF 1.2 MG/L. MG OF .4. NA OFF 184. K OF 1.3 GIVES .58SIGMA X EXPLANATION! MO/L -'M IL L IG R A M S PER L IT E R . UO/t. - MICROORAMG PER L IT E R .MEQ/L MILLIEGUIVELENTS PER LITER. FT FEET. MT - METERS (M) MEASURED. (E> ESTIMATED. (R) - REPORTED. TR TOTAL RECOVERABLE• TOT > TO TAL. QW WA S? WI OH PW AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS! PROJECT! COST! LAST EDIT DATE! 1A-GEP-B1 D r! TP XMJT PROCESSING PROGRAM! F1730P V2 (8/9/BO) PRINTED! 14 -S F P -B 1 PERCENT MEO/L (FOR PIPER PLOT) CA MG NA K CL 504 HC03 1 0 90 0 3 9 44 NOTE! IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER! 0 1 0 1 1 2 7

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 130

Sample Number WSS019 - Gordon Doig - House Well

MONTANA BUREAU OF MINER AND GEOLOGY UATER QUALITY ANAl.YRIS BUTTE,MONTANA 59701 (40A>44'6-4101 LAB NO. S1R1128 STATE MONTANA COUNTY MEAGHER LATITUnE-l.ONOITUI.lli AAD32'?I*N 11 0DS3'53*U SITE LOCATION 9N 7E 1SXCACA UTM COORDINATES 712 N51S3720 E507G23 MSMG SITE WSS019 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 463221110535301 GEOLOGIC SOURCE X * * SAMPLE SOURCE WELL DRAINAGE BASIN BC LAND SIIRFACF ALTITUDE 5 0 9 5 . FT < 1 0 AGENCY + SAMPLER MBMOiJLS SUSTAINED YIELD BOTTLE NUMBER WSS019 YIELD MEAS METHOD DATE SAMPLED 2 1 -J U L -G 1 TOTAL DEPTH OF WELL 1 6 0 . FT LAB + ANALYST MBHOfFNA CASINO DIAMETER A IN DATE ANALYZED OO-AUG-Ol CASING TYPE STEEL SAMPLE HANDLING .1120 COMPLETION TYPE 01* METHOD SAMPLED PUMPED PERFORATION INTERVAL 9A TO 160 FT UATER USE DOMESTIC SAMPLING S IT E DOIG. GORDON * HOUSE GEOLOGIC SOURCE MG/L : n /i. MG/LMEG/L CALCIUM (CA) 4 0 .2 2 .4 1 BICARBONATE (HC03) 192.8 3.16 MAGNESIUM (MG) 1 2 .9 1 .0 4 CARBONATE (C 0 3 ) 0 . SODIUM (NA) 3 0 .5 * 1 .3 3 CHLORIDE(CL) 2 9 .6 0 . 8 3 POTASSIUM (K) fl.fl 0 .2 3 SULFATE (S04) 46.1 0.96 IRON (FE) <.002 NITRATE (AS N) 1 .3 4 0 .1 0 MANGANESE (MN) <.001 FLUORIDE (F) .3 0 0 .0 3 SILICA (SI02) (40.9 PHOSPHATE TOT (AS P)

TOTAL CATIONS 5 .0 2 TOTAL ANIONS til o CD l-CATIO N BALANCE (SIOMA) 0.32 LABORATORY PH 7 .9 9 TOTAL HARDNESS AS CAC03 1 7 3 .4 3 FIELD UATER TEMPERATURE 1 3 .0 C TOTAL A LK A LIN ITY AO CAC03 1 5 0 .1 3 CALCULATED DISSOLVED SOLIDS 333.02 SODIUM ADSORPTION RATIO 1.01 SUM OF D IS S . CONSTITUENT 431.44 RYZNAR STABILITY INDEX 7 .2 3 LAB SPEC.COND• ( MICROMHOS/CM) 309.2 I.ANGLTER SATURATION INDEX 0 .3 7 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C> 2 7 . CNDUCTVY.FIELD MICROMHOS 5 0 4 . FIELD PH 7.34 ALUMINUM. DIGS (MO/L-AL) < .0 3 NICKEL .DISS (MG/L AS N I) <.01 SILVER.DIGS (MG/L AS AG) <.002 LEAD. OIS!) (MO/L AS PB) <.04 DORON .DISS (MO/L AS B) <.02 STRONTIUM.DISS (NG/I.-SR) .3 9 C A D M IUM .DIG S(M G/L AS CD) <.002 TITANIUM DIS(MO/L AS TI) <.001 CHROMIUM. DISS (MC/L-CR) <.002 VANADIUM.DISS(MG/L AS V) .0 0 7 COPPER.DISS (M G /L AS OU) <.002 ZINC.DISS (MG/L AS ZN> <.004 LITHIUM.DISS(MG/L AS LI) .0 0 3 ZIRCONIUM DIS(MG/I. ZR) <.004 MOLYBDENUM.DISS(MG/L~MO> <.002 ARSENIC.DISS(IJG/L AS AS) 0.5

REMARKS: UATER IS CLEAR t HAS MINOR GAS BUBBLES * 6 IN. STEEL CASING 0-9<4 FEET * 4 IN. PVC 80-160 FEET * DRILLED HOLES 1/2 X 1/2 INCH IN PVC *

EXPLANATION: MG/L ■ MILLIGRAMS PGR LITER, UG/L HICROGRAMS PER LITER, MEG/I. MTLI.IEQUIVELENTS PER LITER. FT - FEET, MT - METERS. (M) - MEASURED. (E) ■ ESTIMATED. (f<> » REPORTED. TR ■ TOTAL RECOVERABLE. TOT - TOTAL.

QU UA U I OU PW AT o t h e r OTHER AVAILABLE DATA OTHER F IL E n u m b e r s :

p r o j e c t : c o s t : LAST E D IT d a t e : 1.4-SEP-G1 d y : TP 4MJT p r o c e s s in g p r o g r a m : F1730P V2 (0/9/00) p r i n t e d : 16-S E P -G 1 PERCENT MEQ/L (FOR P IPER PLOT) CA MG NA K CL S04 HC03 47 21 26 4 14 10 42

n o t e : in correspondence > p l e a s e r e f e r t o la b n u m b e r : o i o i i d s

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 131

Sample Number WSS020 - Fox - Stock Well

MONTANA BUREAU OF MINES AND GEOLOGY HATER DUALITY ANALYSIS BU TTE * MONTANA 59701 ( 4 0 0 )4 9 6 - 4 1 0 1 LAO NO. 0101179 STATIC MONTANA COUNTY MEAGHER LATITUDE-LONGITUDE 4.4D:n'in'N h o d 5'01‘W SITE LOCATION 9N AG 12 CAA UTM COORDINATES 712 N!I.t5S505 G~ 0A400 MBMG SITE W5S020 TOPOGRAPHIC MAP WHITE SULPHUR PRINOS 7 1 STATION ID 443310110550101 GEOLOGIC SOURCE tlO Al.VM * * * SAMPLE SOURCE win.i DRAINAGE BASIN PC LAND SURFACE ALTITUDE 50 00. FT < 10 ACENCY (• SAMPLER MBMGSJI.G SUSTAINED YIELD BOTTLE NUMBER USS020 YIELD MEAS METHOD DATE 3AMPLED 2 1 -J U L -ftl TOTAL DEPTH OP WELL 4 5 . FT ( R ) TIM E SAMPLED l A i l ! HOURS ;ui. ABOVE( - ) OR BELOW OS LAD + ANALYST MBMGSF NA CASING DIAMETER DATE ANALYZED 19 AUO-81 CASING TYPE SAMPLE HANDLING 3 1 2 COMPLETION TYPE METHOD SAMPLED PUMPED PERFORATION INTERVAL HATER USE STOCK SAMPLING S ITE STOCK HELL AT F O X * .5 MI N WHITE SULPHUR 3P GEOLOGIC SOURCE ALLUVIUM 2 6 . CNDUCTVY.FIELD MICROMHOS 5 9 2 . FIELD PH 7 .4 ALUMINUM. DISS (HO/L-AL) <.02 NICKEL,DISS (MG/L AS NI> <.01 S IL V E R .D IS S (M O /L AS AG) < .0 0 ? LEAD,BISS (MO/L AS PB) < .0 4 DORON .DISS (HO/L AS B) <.02 STRONTIUM,DISS (MG/I.-SR) .31 CADMIUM. D IS S (M G /L AG CD) < .0 0 ? TITANIUM DIS(MG/L AG TI) .0 0 5 CHROMIUM. DISS (MG/L-CR) <.002 VANADIUM.DISS(MG/L AS V) < .0 0 1 COPPER.DISS (M O /L AS CU) < .0 0 2 ZINC.DISS (MG/L AS ZN> .0 4 2 LITHIUM.DISS(MO/L AS LI) <.002 ZIRCONIUM DIG(MG/L ZR> < .0 0 4 MOLYBDENUM. D IS S(M G /l.*M O ) < .1 ARSENIC,DISSdJG/l. AS AS) 2 .8

r e m a r k s : w a te r i s CLEAR * IRON s t a i n on f i l t e r *

EXPLANATION: MG/L ™ MILLIGRAMS PER LITER. UG/L KICROGRAMS PER LITER. MER/L MILLIEQUIVELENTS PER LITER. FT ■ FEET, MT « METERS. (M) ■» MEASURED, - REPORTED. TR •• TOTAL RECOVERABLE. TOT * TOTAL. QW UA 52 H I OW PW AT OTHER OTHER AVAILABLE DATA OTHER F IL E NUMBERS:

p r o j e c t : c o s t : LAST EDIT DATE: 1 6 -S E P -B l b y : TP *MJT PROCESSING p r o g r a m : T1730P. V2 ( 0 / 9 / 0 0 ) PRINTED: 1A-GGP-01 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 66 23 5 1 . 3 5 90 NOTE! IN CORRESPONDENCE, PLEASE REFER TO LAP NUMPGR: 01Q 1129

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Sample Number WSS021 - Ivan Bodell - Ranch House

MONTANA BUREAU OP MINES ANB OEOl.OOY WATER QUALITY ANALYSIS BUTT fir MONTANA 59701 (4 0 4 )4 9 4 - 4 1 0 1 I.AB NO. 0101150 STATE MONTANA COUNTY MEAOHER L A T H UBE-I.ONBI TUBE 44D35 '24 *N HOBSO'H?^ SITE LOCATION ION 4E 20 ODD UTM COORDINATES ZIP. N5141340 E5047t5 MONO S IT E U88021 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 STATION ID 443524110505201 GEOLOGIC SOURCE S SAMPLE SOURCE WELL BRAINAGE BASIN BC LAND SURFACE ALTITUDE 5035. FT < 10 AGENCY + SANPLER MBM04JLS SUSTAINED YIELD BOTTLE NUMBER WS502.1 YIELD MHAB METHOD DATE SAMPLEB 2 1 -J IJL -01 TOTAL DEPTH OF WELL TIM E SAMPLED i n : 30 ho u r s >WL ABOVE (■*) OR BELOW GS LAD + ANALYST MDMOSFNA CASING DIAMETER DATE ANALYZED 00-A U G -81 CASING TYPE SAMPLE MANDLINO 312 COMPLETION TYPE METHOD SAMPLEB PUMPED PERFORATION INTERVAL WATER USE DOMESTIC AND STOCK SAMPLING SITE BODELL. IVAN * RANCH HOUSE GEOLOGIC SOURCE MG/L MEO/I. MG/L MEQ/L CALCIUM (CA) 3 3 .1 1 .4 5 BICARDONATE (NCOS) 1 5 4 .9 2 . 5 7 MAGNESIUM (MG) 1 5 .0 1 .3 0 CARBONATE (COS) 0 . SODIUM (NA) 17.2 0.75 CHLORIDE (CL) 1 9 .0 0 .5 4 POTASSIUM (K> 8 .9 0.23 SULFATE ( S 0 4 ) 2 0 .1 0 .5 9 IRON (FE) .0 1 1 0 .0 0 NITRATE (AS N) 2 .5 0 0 .1 8 (MN) < .0 0 1 FLUORIDE (F) .7 4 0 .0 4 SILICA 1102) 44.2 PHOSPHATE TOT (AS P ) iTIONS 3 .9 3 TOTAL ANIONS 3 .9 2 STANDARD DEVIA TIO N OF ANION-CATIO N BALANCE (SIG M A) - 0 . 0 8 LABORATORY PH 7 .0 0 TOTAL HARDNESS AS CAC03 1 4 7 . AS FIE L D WATER TEMPERATURE 1 1 .0 C TOTAL ALK A LINITY AS CAC03 1 2 0 .4 8 CALCULATED DISSOLVED SOLIDS 240.94 SODIUM ADSORPTION RATIO 0 ./> 2 SUM OF DISS. CONSTITUENT 320.55 RYZNAR S T A B IL IT Y INDEX 7 .8 4 LAD SPEC.COND.(MICROMHOS/CM) 3 0 4 .0 LANGLIER SATURATION INDEX 0.01 PARAHETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 2 5 . CNDUCTVY.FIELD MICROMHOS 3 0 8 . FIELD PH 8.0 ALUMINUM. DISS (MO/L-AL) <.03 NICKEL.DISS (MG/L AS NI) .0 1 • S IL V E R .D IS S (H G /L AS AG) < .0 0 2 LEAD.DISS (MO/L AS PB) < . 0 4 DURON .D IS S (M G/L AS D> < .0 2 STRONTIUM.DISS (MG/I.-SR) .2 7 CADMIUM.D1S8(MG/L AS CD) < .0 0 2 TITANIUM D IS (M G /L AS TT> < .0 0 1 CHROMIUM. DIGS (MO/L-CR) < .0 0 2 VANADIUM.DISS(MG/L AS V) .0 1 3 COPPER.DISS (MG/L AS CU> .0 0 4 ZINC.DISS (MO/L AS ZN> .0 0 5 LITHIUM.DISS(MO/L AS LI) < .0 0 2 ZIRCONIUM DISIMG/I. ZR) < .0 0 4 MOLYBDENUM. D1 BIS (MG/L-MO > < .1 ARSENIC.DIOS(UO/L AS AS) 4 . 4

REMARKS.* UATER IS CLFAR * SON Or EDWIN BODELL * UATER SAMPLED THROUGH HOSE S

EXPLANATIONS MO/L •» MILLIGRAMS PER LITER. UO/L - MICROORAMS PER LITER. MEO/L MILL1EQUIVEI.ENTS PER LITER. PT - FEET. MT « METERS. ~ MEASURED. (E) - ESTIMATED. (R ) » REPORTED. TR » TOTAL RECOVERABLE. TOT - TOTAL. OW WA 02 W1 OW PW AT OTHER OTHER AVAILABLE DATA Y OTHER F IL E NUMBERS:

p r o j e c t : cost: LAST EDIT DATE: 14-5E P - 81 d y : tp SMJT PROCESSING p r o g r a m : F1730P V2 ( 0 / 9 / 0 0 ) p r i n t e d : 14- SEP -81 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL 004 H003 42 33 19 5 13 14 45 note: in correspondence, please refer to lad number: 0101130

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Sample Number WSS022 - J e ff Kennick - House Well

MONTANA BUREAU OP MINES AND SPOI.ORY UATER OUAI.ITY ANALYSIS BUTTE/MONTANA 59701 (404)494-4101 LAB NO. 01(11131 STATE MONTANA COUNTY MEAGHER LATITUDE-1.ONOITUOF 44D31'59*N 110054 ' 49 *H SITE LOCATION 9N 4E 24 ABB UTM f.'OORBINATI: B Zl? N51530S0 E504595 MflMS RITE USS022 TOPOGRAPHIC HAP WHITE SULPHUR SPRINOS 7 1 STATION ID 443159110544901 GEOLOGIC SOURCE * t t SAMPLE SOURCE UEL 1. DRAINAGE BASIN BC LAND SURFACE ALTITUDE 4 9 9 0 . FT < 10 ACENCY + SAMPLER MBMGtJLS SUSTAINED YIELD BOTTLE NUMBER US8022 YIELD HEAR METHOD DATE SAMPLED 22-.JU L -01 TOTAL DEPTH OF HELL 250. FT (R) T IN E SAMPLED 0 9 *.TO HOURS SUL A B O V E (-) OR BELOW OS 1 4 . FT ( R ) LAB + ANALYST MDMSSPNA CASINO DIAMETER DATE ANALYZED 00-AUG-G1 CASINO TYPE SAMPLE HANDLING 312 COMPLETION TYPE METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE DOMESTIC SAMPLING SITE KENNICK. JEFF * .5 MI S WHITE SULPHUR 3 PR GEOLOGIC SOURCE MG/LMEO/L MG/L MEO/I. CALCIUM (CA) 51.3 2.54 BICARBONATE (H C 03) 341 . 5 .9 2 MAGNESIUM (MG) 1 3 .3 1 .0 9 CARBONATE (C 0 3 ) 0 . SODIUM (NA) 104. 4.52 CHLORIDE (CL) 3 7 . 4 1 .0 4 POTASSIUM (K) 7.5 0 . 1 9 SULFATE • ( S 0 4 ) 7 3 . 3 1 .5 3 IRON (FE) .002 0.00 NITRATE (AS N) .42 0 .0 4 MANGANESE (MN) < .0 0 1 FLUORIDE TOTAL CATIONS B . 37 TOTAL ANIONS 0 .5 9 STANDARD DEVIATIO N OF ANION-CATION BALANCE (5 I0 M A ) 0 .9 7 LABORATORY PH 7 .7 7 TOTAL HARDNESS AS CAC03 1 0 2 .0 4 FIE LD HATER TEMPERATURE 9 . 0 C TOTAL A LK A LIN ITY AS CAC03 2 9 4 .0 8 CALCULATED DISSOLVED SOLIDS 5 2 4 .4 3 SODIUM ADSORPTION RATIO 3 .3 5 SUM OF DISS. CONSTITUENT 7 0 7 .8 0 RYZNAR S T A B IL IT Y INDEX 4 .8 7 LAD SPEC.COND.(MICROMHOS/CM) 009.3 LANSLIER SATURATION INDEX 0 .4 5 PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C) 1 7 . CNDUCTVY.FIELD MICROMHOS 0 0 4 . ALUMINUM. DISS (MO/L- AL) < .0 2 N IC K E L /D IS S (M G /L AS NT) < .0 1 SILVER.DISS (MB/L Af AO) <.002 LEAD.BISS (MG/L AS PB) < .0 4 BORON >DIf (M O /L AS B > .50 STRONTIUM.DIS3 (MO/L-SR) .3 4 CADMIUM.DISS(HS/L AO CD) <.002 TITANIUM DIO(MG/L AS TI> < .0 0 1 CHROMIUM. DISS (M fl/L -C R ) <.002 VANADIUM.niSS(MG/L AS V) .002 COPPER.DISS (MB/L AS CIJ) <.002 ZINC.DISS (MG/L AS ZN> < .0 0 4 LITHIUM.DISS(HO/L AS LI) < .0 0 2 ZIRCONIUM. D IS (M O /l. ZR> < .0 0 4 MOLYBDENUM. DISS ( HO/I.-MO > < .1 ARSENIC.DI8S(UG/L AS AS) 7 . 3

REMARKS! UATER IS CLEAR 3 IRON STAIN ON FILTER * SEND COPY TO! BOX 3 2 5 . H IIIT E SULPHUR SPRINGS. MT. 59 4 4 5 * LAB! FU CA OF 52.0 MO/L/ MO OF 13.9. NA OF 107. K OF 7.9 GIVE -.17 SIGMA * EXPLANATION! MG/L » MILLIGRAMS PER L IT E R . IIG/I. - MICROGRAMO PER L IT E R . MEO/I. ■ Mtl.LIEQ UIVELENTS PER L IT E R . FT FEET. MT * METERS. (M > MEASURED. (E> ESTIMATED. (R> - REPORTED. TR « TOTAL RECOVERABLE. TOT « TOTAL. QM UA 52 U I OU PU AT OTHER OTHER AVAILABLE BATA OTHER F IL E NUMBERS! PROJECT! COST! LAST EDIT BATE! 1A -S E P -81 BY! TP *H JT PROCESSING PROGRAM! F1730P V2 (0/9/00) PRINTED! 14 -G E P -01 PERCENT NEO/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 30 13 54 2 12 17 48 NOTE! IN CORRESPONDENCE. PLEASE REFER TO LAB NUMBER! 01 0113 1

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Sample Number WSS023 - Ronald Jackson

MONTANA BUREAU OF MINER AND GEOLOGY WATER OUAI.ITY ANALYSTS BUTTE.MONTANA 59701 (4 06)496-4101 LAB NO. 0101132 STATE MONTANA COUNTY MEAOIIER LATITUDE-LONGITUBE 44n33'49'N IIOBSS'IA’U SITE LOCATION , 9N AE 1 CCDD UTM COORDINATES 717 N5156040 £506450 HDMO SHE WR0023 TOPOGRAPHIC MAP WHITE SULPHUR SPRINGS 7 1 STATION ID 4 6 3 3 4 9 1 1 0 5 5 1 A03 GEOLOGIC SOURCE X » 4 SAMPLE SOURCE WC-.l.L DRAINAGE DAS.IN DC LAND'SURFACE ALTITUDE 4990. FT < 10 AOENCY + SAMPLER MBHOSJLS SUSTAINED YIELD BOTTLE NUMBER USG023 Y IE LD MEAS METHOD DATE SAMPLED 22-JUL-81 TOTAL DEPTH .OF WELL 155. FT (R ) TIME SAMPLED 11500 HOURS SWI. ABOVE(■■) OR DELON GO 9 0 . FT < R > LATl + ANALYST MI5M04FNA CASINO DIAMETER A IN DATE ANALYZED o n -A U O -n i c a s in g t y p e s t e e l SAMPLE HANDLING 312 COMPLETION TYPE * METHOD SAMPLED PUMPED PERFORATION INTERVAL UATER USE SAMPLING S IT E JACKSON. RONALD L . * GEOLOGIC SOURCE MG/L MEQ/L MG/L MEO/L CALCIUM (CA) 4 3 .4 2 .1 7 d ic a r d o n a t : (NCOS) 2 0 9 .8 3 .4 4 MAGNESIUM (MS) 1 3 .6 1 .1 2 CARBONATE (C 0 3 ) 0. snniiJH (NA) 1 2 .5 0 .5 4 CHLORIDE ( CL > 0.0 0 .2 3 POTASSIUM (K) 6 .4 0 .1 6 SULFATE < G 04) 1 7 .4 0 . 3 6 IRON (FE> < .0 0 2 NITRATE (AS N) .0 9 0 .0 6 MANGANESE (MN) < .0 0 1 FLUORIDE (F) .6 3 0 .0 3 S IL IC A (S 1 0 2 ) 6 0 .2 PHOSPHATE TOT (AS P) TOTAL CATIONS 3 .9 9 TOTAL ANIONS 4 . 1 : STANDARD DEVIATION OF ANION-CATION BALANCE (8 I0 M A ) 0 .7 9 LABORATORY PH 7 .7 7 TOTAL HARDNESS AS CAC03 1 6 4 .3 5 FIELD WATER TEMPERATURE 1 0 . C TOTAL A LK A LIN ITY AS CAC03 1 7 2 .0 7 CALCULATED DISSOLVED SOLIDS 266.37 SODIUM ADSORPTION RATIO 0 .4 2 SUM OF DIGS. CONSTITUENT 3 7 2 .8 2 RYZNAR S T A B IL IT Y INDEX 7 .4 8 LAD SPEC.COND.(MICROMHOS/CM) 395.4 LANGI.IER SATURATION INDEX 0 .1 4

PARAMETER VALUE PARAMETER VALUE CNDUCTVY,FIELD MICROMHOS 3 0 9 . FIELD PH 7 .9 ALUMINUM f DISS (MO/l.-AL) <.03 NICKEL.DISS (MO/L AS NI) .01 SILVERrDISS (MG/L AS AG) <.002 LE A D .D IS S (M G/L AS PD) < .0 4 BORON .DISS (MO/L AS B) <.02 STRONTIUM.DISS (MG/l.-GR) .5 2 CADMIUM.DISS(MG/L AS CD) <.00? TITANIUM DIS(MG/L AS T I) <.001 CHROMIUM. DISS (M O /L-C R ) < .0 0 2 VANADIUM.DISS(MO/L AS V) .0 0 6 COPPER.DISS (MG/L AS CU> <.00? ZINC.DISS (MG/L AS 7N> .0 2 8 LITHIUM.DISS(MO/L AO LI) <.002 ZIRCONIUM DIS(MG/L ZR> < .0 0 4 MOLYBDENUM. D ISS(M G/l.-M O > < .1 ARSENIC.D13S(UG/I. AS AS) 4 .3

REMARKS! UATER IS CLEAR * 1 HI NU WHITE SULPHUR SPRINGS *

EXPLANATION! HG/L - MILLIGRAMS PER L IT E R . UO/L - MICROORAMS PER L IT E R , MEQ/ MILL IEOUIVELENTS PER I.ITIlR. FT - FEliT. HT «• METERS. (M) - MEASURED. (E) - ESTIMATED, (R ) - REPORTED. TR « TOTAL RECOVERABLE. TOT ~ TOTAL.

QU UA S2 WI OU PU AT OTHER OTHER AVAILABLE BATA OTHER F IL E NUMBERS:

PROJECT! c o s t : LAST EDIT DATE! 16-G E P -81 b y : TP 4MJT PROCESSING p r o g r a m : F1730P V2 ( G / 9 /0 0 ) p r i n t e d : 16-S E P -0 1 PERCENT MEQ/L (FOR PIPER PLOT) CA MG NA K CL S04 HC03 54 20 13 4 5 0 83

n o t e : IN CORRESPONDENCE, PLEASE REFER TO LAR NUMBER! 010115 R*ndw

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Sample Number WSS024 - Bob Hanson - Irrig a tio n Well

MONTANA BUREAU Of MI.'!US AND (.iO LIit.. WATER QUAl. TTY ANAl.YSi: curnr. Montana svyoi < »oa> iva -ij 01 LAB NO. USOOO.VO STATE MUMTAMA c o u n t y MEAGHER l a t i t u d e - l o n g it u d e 46031'17'N IIODSI'IO'W s i t e i. oca n o w 0911 04E .14 UDDA UTM COORDINATES 7. ti r MSMR S ITE USS00 24 TOPOGRAPHIC MAP WHITE SULPHUR SPRIIMiS STATION ID 4631 J 71 ] 0 3 1 X 00.1 GEOLOGIC SOURCE X IOALVM* 400GRSM* SAMPLE SOURS?: WELL DRAINAGE CASIO DO LARD SUREACC At. I IT I! HE SO.51 . < 10 AGENCY 4 SAMPLER iiBMGtutin SUSTAIMEU YIELD 12 00. GPU c o n t . r NUMBER USSOOIM YIELD HI* AS HIM HOD REPORTED BATE SAMPLED 0(1-JUL-fl? TOTAL DEPTH OP WELL. 2 2 3 . PT (R i TIM E SAMPLED I ( I! fill HOURS SUL. ABOVE I - ) OR DEI. OW GS i -%■ r r LAD ■» ANALYST MUMGSFNm CASING DIAMETER 12 IN DATE ANALYSED 2 9 - SEP-02 CASINO TYPE STEEL SAMPLE HAMOLIMG 3120 COMPLETION TYPE 02*02 HFTMOD SAMPLED GRP.D PERFORATION INTERVAL 93 TO V? I T (R) UATER USE £»RISA IIUN 150 TO 134 PT < li > SAMPLING SITE DOS HANSON*J. S MI S OP WHITE SULPHUR SPR* GEOLOGIC SOURCE ALLUVIUM (OUATERNARY I HO/L MER/L HG/l. MEG/L CALCIUM (C A ) 7 0 .6 3 .5 2 SIGARBONATi: IMC03) 181 . 2.97 HAGNESIUM (MO) 1 3 .0 1 .0 7 CARDOHArL' (CU3) 0. GOD (Ull IMA) 14.1 0.41 CHLORIDE (C L i 32. t 0.91 POTASSIUM (K> 4.0 0 .1 2 SULFATE (SOI) 49. 2 1 .44 IRON •4 0.02 SILICA (ST02) 4 9 .4 PHOSPHATE TOT (AS P i TOTAL CATIONS 5 .3 3 TOTAL ANIONS 5. 45 «o <.03 NICKEL.DISS (MO/L AS: Ni) .02 GIL'/ES*DISS (MG/L AS At.) <.002 LEAO.DISS (Nfi/L PD) .09 DORON *DISS (MG/L AS B > <.02 STRONTIUM.BISS (I ,-SR) .24 CADMIUM.DISS(KG/L AS CD) <.002 TITANIUM TiISOIG/L AS1 I I ) . 003 CHROMIUM. OISS (MO/I.' •CR) <.002 VANADIUM * li ■ SS ( MO/L i ,S V) . 0 0 4 COPPER*DISS (MG/L AS CU) .007 21 NO .D IS S CMO/I. AS 2M) . 007 L ITHIUK> BISS(MG/L AS LI) .005 ZIRCONIUM DIS (MO/L < 1, CR (.0 03 MOL YIHiENUM, DISS ( MG/L ■-MO) .02 ARSEN) C * li) SS ( UO/1. A! i AS) 2.0

REMARKS: GAS BU3BL.e s :t OIRTY FILTER* ... WELL HAS DEEM PUMPED FOR 3 DAYS) SAMPLE WAS TAKEN FROM SPRINKLER HEAD. 34 SPRINKLERS RUNNING* ADDN'I. PERFS 190 TO 220 FT (R)*

EXPLANATION MO/I. " MILLIGRAMS PER LITE R * UO/L >• MICROORAMS PER LITER * MER/L Mlt.LIEOU IVELENTS PER LITER. FT « FEET* MT - METERS. (II) •» MEASURED* (?:> CGT1MATED* (II) ‘ REPORTED. TR TOTAL RECOVERABLE, TOT = TOTAL. OU UA 32 U I OU FU AT OTHER OTHER AVAILABLE DATA Y OTHER FILE NUMBERS I PROJECT! COST I LAST E D IT DATEI 1 3 -0 C T -0 2 y Y * TP sacs PROCESSING PROGRAM} FI730P V2 (11/3/01) PRINTED} I3 -0 C T -0 2 PERCENT MEO/I. (FOR PIPER PLOT) CA MO NA II CL SIX IIC03 C03 64.1 20.1 11.3 2.3 17.0 27.1 55.H 0,0 NOTEI IN CORRESPONDENCE* PLEASE REFER TO LAB NUMBER I 82G0040

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 136

Sample Number WSS025 - Castle Mtn. Lumber Co. - Fire Protection Well

MONTANA BUREAU OF KINGS AWI) GGOI OGY WATER HltAI. TTY ANALYST!'. WITTE/MONTANA 59701 (40/i>49*..4IO1 LAW WO. 02000/. 1 STATE MONTANA COUNTY ME ACHE It I ATTTHBG-l.nMOTTItttS 4/.0.T2' 211 n iiobba'P/'u SITE LOCATION cm i O/.E IT WAS A IJTM CDnitllTMATEG ?. M G HBMIS SITE Mesons TOPOGRAPHIC Mrtl> WHT1T SULPHUR SPRINGS 7 I STATION TW 4 11 tos-mzoi GEOLOGIC SOURCE 1 10AI. VMS S SAMPLE BOURSE WE 1.1. DRAINAGE BASIN nr LAND SURFAC.; ALT! I (Mil.' 5 0 (0 . FT jo AGENCY I SAMPLER MBMGSNGt. SUSTAINED YIELD BOTTLE HIIHWKR WG«023 YTEI.ll MEGS METHOD OATK SAMPI irn 10-Jill -ILT TOTAL I1EPTH OF MIM.L 131. FT (R> TIME SAMPLED i 0 10 0 HOURS SUL a b o v e ( - ) or isei.ow or; CO. FT < It 1 LAB t ANALYST HOMGSENA RASING BIAMI: TF.lt A IN (R) HATE ANALYZED O4~rC0"fl3 CASINO TYPF STEEL SAMPLE HANOI. INC Jin ROMPI. FT TOM TYPE one METHOD SAMPLED niton PERFORATION INTERVAL f TO 17.1 FT WATER USE FTHE PROTECT TON SAMPLING SITE CASTLE MTN LUMBER CO FIRE PROTECTION WELL GEOLOGIC BOURSE ALLUVIUM (RUATERNARY) MG/L HER/I MG/l. MEO/I CALCIUM ISA) 7/. ,4. .T. I) I BICARBONATE (HC03) 3 1 7 . 5 .2 0 HAGNEBIDM IMIS) 15. 1 1 .2 4 CARBONATE (c n ;n 0. r .o n m i (NA) 151 .7 2 .2 3 CHLOItmF (CL) 40 .2 I . I 3 POTASSIUM TOTAL CATIONS 7.60 TOTAL ANIONS 8. 25 STANDARD DEVIATION OF ANION-CATION BALANCE (SIGMA) LABORATORY PH 7 .8 3 TOT Al. CACI13 2 3 2 .9 2 FIELD WATER TEMPERATURE 5 4 . F CAC07, 2 5 9 .9 9 CALCULATE I) DtSSOI.VFB SOI. IBS 3 0 7 .3 3 RAT 1(1 1 .4 0 GUM OF IJISS. CONSTITUENT AAfl.'.’O arzMAir INDFX 4 .5 5 LAB BPirC.COMB.(MICROMHOS/CM) 720.4 INDEX 6. PARAMETER VALUE PARAMETER VALUE TEMPERATURE. AIR (C ) 7 0 . F ALUMINUM. BIGS (MG/l. Al. ) < .0 3 NICKEL<0108 (HO/L AS NI) <.01 SILVER/DISS (MO/L AS AO) < .0 0 2 LEAD.DISS (M K/I AS PR) < .0 4 BORON .DIBS (HG/L AS r.) .3 9 STRONTIUM; DIGS (MO/I.SR) .69 CADMIUM ; I1TSS (MO/L AS r.n> < .0 0 2 TITAH1UM BIS(MI5/I. AS TI) .011 CHROMIUM. DIGS (MG/L CR) <. 002 VANADIUM ; B ISS( MO/L AS V) .0 1 2 COPPER; BISS (MO/1. AS oil) .0 0 * ZINC >11 ISO (MG/l. AS 7N) .012 L IT H IU M .D IS C ( MG/l AS 1.1) .0 4 3 ZIRCON HIM DIS(MO/L AS ZR <.003 MOLYBDENUM; DISS(M G /l -MO)MO) < .0 2 ARSENIC. DIHIUMS/L AS AS) <5.2

REHARKSI ISAS BURBLl'SS tO HP TURBINE PUMP. 2 LARGE' PRESSURE TANKS ("IS O GAI. ) 4 LET PUMP RUM 45 MINUTES 11EF0RE SAMPLINGS. LABI FI) CA 3 0 .1 MG/l.S ANIONS K CATIONS VERIFIERS EXPLANATION! MO/L ■» MILLIGRAMS PER LITER/ IIO/I. - MTCROORAHS PER L IT E R / MEQ/L Mil LIEQIIIVEI.ENTS PER LITER. FT FEET. MT « METERS. (M) MEASURED ( F > • ESTIMATED/ (It) * REPORTED. TR « TOTAL RGCQVGRAULG. TUT / TO TAI.. OW WA ) WI OW PU AT OTHER OTHER AVAILADLF DATA Y OTHER F IL E NUMBERS 1 PROJECT I COST! LAST EDIT DATE 1 1 7 -FED- S3 BY! TP SBCS PROCESSING PROGRAM! F1730P V? Cll/3/l«l> PRINTEDJ i7~ F r a n:: PERCENT MEO/I. (FOR PIPER PLOT) CA MO NA l< CL SO 4 11003 cos 50.2 1.4.3 29.4 4.1 14.2 CO.9 (.4.9 o.o NOTE! IN CORRESPONDENCE. PLEASE REFER TO LAB NtJMDGRI I12R00A1

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 137 Sample Number WSS026 - Ralph Jordon

HONI ANA BUREAU OF HINEG AND GF.OLOGY UATER QUALITY ANALYST5 BIJTTE / MONTANA 39701 (4 0 4 )4 9 4 -4 1 0 1 LAB Hi). 020004? STATE MONTANA COUNTY MEAGHER LATITUDE -I. QUO I TUBE 4 4 0 3 2 '4 0 * H 1 I 01)34'22*U SHE LOCATION 09N 04E 13 ADAA UTM COORDI MATES 7. N E MOMS S IT E HBS02A TOPOGRAPHIC MAP WHITE SULPHUR SPRrNOO 7 t STATION in 443240110542201 GEOLOGIC SOURCE 120SDMS* * t SAMPLE SOURCE MELl. nRA (NAGI* BAOIM DC LAND SURFACE AI.TTTUDF S 0 4 0 . FT < 10 AGENCY + SAMPLER HKHGSUGG SUSTAINED YTELI) BOTTLE NUMBER USS024 YIEI.O MEAS HETHOn DATE SAMPLED TOTAL DEPTH OF HELL 17S. *T (R> TTME SAMPLED t HOURS SUL ABOVE( - ) OR OELOU OS 3 1 .3 FT IM I LAD 4 ANALYST HRMGHI'NA CAGING DIAMETER 4 IN DATE ANALYZED 0 4 -F E B -83 CASINO TYPE STEEL SAMPLE HANDLING COMPLETION TYPE * METHOD SANPLED PERFORATION INTERVAL UATER USE IRRIGATION SAMPLING S H E RALPH JORO O NiP.O .KOX 4 5 . UNITE SULPHUR SPR OEOLOOIC SOURCE SEDIMENTS (TER TIA R Y) MG/L MEQ/L HG/L MEQ/l. CALCIUM (CA) 2 . 5 0 .1 2 BICARBONATE (HC03) 2 5 3 3 . 41 .5 1 MAGNESIUM (MG) 3 .4 0.211 CARDONATE (COS) 0 4 .4 2.00 SODIUM (NA) 2 1 3 0 . 92.45 CHLORIDE (CL) 8 2 7 . 2 3 .3 3 POTAGSIUH (K) 19. 0.49 SULFATE (6 0 4 ) 13 3 2 . 2 7 .7 3 IRON (FE) .0 0 9 0.00 NITRATF (AS N) .34 0 .0 4 MANGANESE (MN) .0 0 7 0.00 FLUORIDE (F> 7 .7 0 .4 1 SILICA (SI02) 4 4 .0 PHOSPHATE TOT (AS P ) TOTAL CATIONS 9 3 .3 5 TOTAL ANIONS 9 5 .9 0 STANDARD DEVIATION OF ANION-CATION BALANCE (SIOMA) 1 ,5 9 LABORATORY PH 0 .4 3 TOTAL HARDNESS AG CAC03 2 0 .2 4 FIELD WATER TEMPERATURE 5 9 .3 F TOTAL ALKALINITY AS CAC03 2 2 2 1 .4 0 CALCULATED DISSOLVED SOLIDS 5 7 0 0 .3 4 SODIUM ADSORPTION RATIO 2 0 4 .0 4 SUM OF DISS. CONSTITUENT 4 9 0 3 .5R RYZNAR S T A B IL IT Y INDEX 4 .3 8 LAD SPEC.COND.(MICROMHOS/CM) 7070. I.ANGLIER SATURATION INDEX 0.07 PARAHETER VALUE PARAMETER VALUE TEMPERATURE. A IR (C> 40. F ALUMINUM. DISS (MG/L-AL) .03 NICKEL/DISS (HO/L AS NI) < .0 1 S IL V E R • DISS (H D /L AS AG) < .0 0 2 LEAD. IlTSS (MG/L AO PR) .10 DORON .DIGS (HG/L AS B) 25.2 STRUNTIUM/DISS (M0/L-6R) .4 2 CASHrUH/ OIOS( HO/L AS CD) < .0 0 2 TITANIUM DIS(MG/L AO TI) .0 0 3 CHROMIUM. D IS S <.002 ZINC.DIOS (MG/L AS ZN) <.004 LITHIUM. DTGIKHG/L AS LI) 2.02 ZIRCONIUM BIS(HO/L AS ZR .0 2 4 MOLYBDENUM/0 1 SO(MG/L-HO> .4 0 ARSENIC.DIS3(UG/L AO AS) 1 1 .0

r e m a r k s : w ater foams WHEN AGITATED( SALTY tYELLOW( s u s p e n d e d claysidirty f i l t e r s NO PRESSURE TANK/ WELL HAS BEEN USED VERY L IT T L E SINCE INSTALLATION IN APRIL 1902SOWNER CLAIMS THE UATER IS K ILL IN G HIS TREE3*SUB PUMP 12 GPU LABI FU NA 2230 M U/L) GIVES 9 7 .9 TOTAL CATKIN MEUVS AND BORON PRESENT AS LABI 1(31)03 GIVES 9 0 .2 TOTAL ANIOH HE0V8 FOR .2 SIGMA* EXPLANATION! MO/L - MILLIGRAMS PER L IT E R / UO/I. " HICROORAMS PER L IT E R / MEQ/L - MILLIEQ IilVELENTS PER L IT E R . FT - FEET. MT - METERS. (H> * MEASURED. (E> «■ ESTIMATED/ (R ) « REPORTED. TR - TOTAL RECOVERABLE. TOT " TOTAL. OU WA 32 UI OW PH AT OTHER OTHER AVAILABLE DATA OTHER F IL E NUMBERS!

PROJECT 1 COST! LAST EDIT DATE! 0 2 -MAR-83 BY! TP *BCS PROCESSING PROGRAM! F1730P V2 ( 1 1 / 3 / 0 1 ) PRINTED! 02-NAR-02 PERCENT MEQ/L (FOR PIPER PLOT) CA MS NA K CL 304 HC03 CD3 0.1 0.3 99.0 0.5 24.4 29.1 43.5 3.0 NOTE! IN CORRESPONDENCE. PLEASE REFER TO LAD NUMBER: 0200042

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 138 Sample Number WSSBANK - Bank Thermal Well

i • •• « a : • r jh.yi ; i a n a ; r * I S .if. nl. DD?!)! PUT 1 M1 ’AN* 4 1* a I 13 ifOh T ana Oiin i r MEAGHER *: *r loi'at ton *?N ,'iE 12 A AAA Lat t TvDC long -: jr utm c.anniiJnATi MliMli SI IF USSPANN TOPOGRAPHIC HA." WHtTE SULPHUR SPRINGS STATION IP 4A32r:il054?201 GFOiOOir SOURCE * > * rAm-tr sourcf HELL BRAINAGE FAT.IN r.r. ANf' GURrAftE ALTITUDE 5 0 2 0 . FT < 10 AGENCY + BAMPLCr, nBMGX.JLS SUSTAINED YIELP 5 0 . OPM BOTTI-E NUMBER WSGBANK YJFl.D MI.'ATi MLTHOP REPORTED PATE SAMPLED OS-Dl'C 81 TOTAl Prr-TH OF WEL1 3 3 0 . FT 4 1 .0 2 .0 5 (H C 03) 7 7 1 . 1 2 .9 6 MAGNESIUM (H6> I * . 5 0.7(5 (C 0 2 ) .0 SODIUM (MA) 4 3 3 . 1 0 .8 4 (CL.) 1 4 7 . 4 • t 5 POTASSIUM 1 7 .5 0 .4 5 (S 0 4 ) 2 1 1 . 4 . 3 9 IRON./_r--- .- <.001 CHROMIUM. D ISS (M G /L -C R ) .010 VANADIUMf DISS(H8/L AS V) <.001 COPPER.DISS (MG/L AS CU) .0 0 7 ZXNC f DISS' jOJS/L AS ZN) .022 LITHIUM.DISS(MG/L AS L I) 1 .1 5 ZZRCCNIUM D I5 ( M 0 /L ZR) < .0 0 3 MOLYBDENUM.DISGZMG/L-MO) <.02 ARSENIC fD ISSO JG /L AS AS) < .1 A R SEN IC .TR(U G /I. AS AS) <.1 SULFIDEj TOTALIMG/L AS S) 2.5

REMARKS! HATER COLLECTED FROM HEAT EXCHANGET. - NO P H l R J C TEMP LOOS - 45 C) NAOH ADPFP ON 1 2 /9 /0 1 r- SULFIDE IS A MINIMUM. HATER USED FOR SPACE HEATING * TOP Or CEMENT PLUG APPROX. 220 FT LAD! RU - SULFIDE ODOR EXPLANATION! MG/L « MILLIGRAMS PER LITER IJG/L - MICROGRAMS PER LITER. MEQ/l. MIL I IFQUIVELENTS PER LITER. FT FFH , MT * METERS. (Ml « MEASURED. tI' > * e s t i m a t e d . (R> ------REPORTED. TR TOT Al r.f:COvrr rtG NA m c l s.'m n r nr. r.ri3 3 3 .5 85.2 7 .0 19.3 20.4 40.3 o.o I n f OP'P'FSP iThLPnCE ■ REFC-T - 6 *’■ >111*1 .• . 0'' li 5 3

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 139

WHITE SULPHUR SPRINGS BANK WELL; 81Q2053

INITIAL SOLUTION

TCHTCRATURC * 4 5 .0 0 KGRCCS C I 'll* 7.620 ANALYTICAL CTHCAT * 22.282 ANALYTICAL CTHAN * 21.792

M i l l OXIDATION - RCDUCTIOH m i l

DISSaVCD OXYKH * 0 .0 0 0 NO/l CII XASURCO WITH CALONCL * 0.0 0 0 0 VOLTS aac CORALK ITCALC IDAVCS HCASURCR CH OT ZOCCLL SOLUTION * 0.0000 VOLTS 0 4 0 CORXCTCO CH • 0.0000 VOLTS i t cohtutcd r a m c o rx ctcd cii * o.ooo

M l TOTAL CONCCNTRATIONS OT INTUT STCCICS M l

TOTAL LOO TOTAL TOTAL STCCICS MOLALITY HOLALITT HG.LITRC

CA 2 1 .0 224X -03 -2 .9903 4.1000X101 HG A 3 .9 0 0 4 X 0 4 -3 .4 0 0 2 9.5000X100 NA 1 1.88291C 02 •1 .7 2 5 2 4.3300X102 K 1 4 .4 7 4 1 X 04 -3 .3 4 9 3 1.7500X101 Cl -1 4.I4515C 03 -2 .3 8 2 5 1.4700X102 SOI •2 2.19588C-03 -2.0504 2.1100X102 HC03 -1 I.2 9 5 9 X -0 2 -1 .8 8 7 4 7.91000CI02 S102 TOT 0 7 .2 7 0 9 X 04 -3 .1 3 8 4 4.37000CI01 TC 2 1 .7 5 4 2 X -0 t -5 .7 5 5 9 9.80000C 02 SR 2 .0793X -0S -4 .0 7 7 9 1.8400X100 r - i 3.3 1 5 1 X -0 4 -3 .4 7 9 5 0.3000X100 ANAL ICS 0 7.8029X-05 -4 .1 0 7 7 2.00000000 AL 3 3 .7 0 5 1 X -0 7 -0 .4 3 1 2 1.0000X 02 LI 1 1.45483C-04 -3 .7 8 0 7 1.1500X100 N03 -1 4 .4 4 9 2 X 07 •0.1905 4.0000X-02 C TOT 0 7 .3 0 5 7 X 04 -3 .1 3 0 3 7.9000X100 HN 2 2 .1 8 3 5 X -0 4 -5.0000 1 .2000X 01

IIHITC SULHU) STRINGS CAM! M i l l 0102053

titixscRiriioH or solution m m

ANALYTICAL C0HTU1CD HI ACTIVITY 1120 * 0.9993 CTHCAT 22.282 21.407 7 .0 2 0 TC02 * I.43I47CC -02 CTHAN 21.792 20.900 L0GTC02* 1.0441 TCHTCRATURC T02 = O.OOOOOOCIOO CII * 0.0000 TC* -4.701 45.00 KG C rcill * 9.75II29C-07 rr CALC S > 4.70123X100 C02 TOT * 1 .2 9 5 4 0 X 02 I t CALC DOT* 1.00000X 102 IONIC STXNGTII DCNSITY * 1.0020 TC SATO DOT- 1 .0 0 0 0 0 0 0 0 2 2.435003C 02 IDS * I713.0HG/L TOT ALK = 1.2961 IOC 101 HC0/K6 1120 CAREONATC AIK * 1.20231X 101 HCO/KG 1120 CLCCT « 4.CC1709C-01 HCO/KG H20

IN C0HTUT1HG TIC D1STR1DUT10N OT STCCICS. T t * -4 .7 0 1 COUIVALCNT CII * -0.302VOLTS

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. White Sulphur Springs Bank Well (continued)

wage IAT KT LOG IAP LOG KT IAP/KT LOG IAP/KT DCLGR

40 A8ULAR 4.3744E 20 7.0C07E 20 -17.3571 -17.1477 4.2041E 01 -0 .2 0 7 1 8 -0.30141 41 ALDITE 1.0500E 10 1.5003E 17 -17.7314 -10.8000 1.1075C 01 -0 .7 2 4 4 2 -1.34404 141 AL0II3A 3.7C7X 34 7.7374E 32 -33.4217 -31.0115 3.0G05C 03 -2.41022 -3.50879 S t ALUNIT -72.7577 -03.7400 -9 .0 1 1 4 0 -13.11717 43 ANALCN 2.570X 15 1.3700E 12 -14.5007 -11.0011 1.0013E 03 -2.7 2 5 5 4 -3.74783 10 AIAIYPRIT 4.4307C 07 1.C7C2C 05 -0 .3 5 2 ? -4.7217 2 .3 3 75E 02 -1.43125 -2.37477 114 AIMITC -71.0005 -01.3011 10.34044 15.08302 47 M10RTII 2.104CC 23 3.0042E 17 -22.0000 -10.5223 7.2724C 05 -4.13831 -4.02454 27 ARAGONIT 1.C71X 00 4.4531E 0? •7.7231 •0.3513 4 .2404E100 0.42022 0.91454 151 ARTIN 7.2000C 24 3.2744E 1? -23.0331 -10.4049 2.C279E 05 -4.54074 -4.42130 4? r e i r a -42 .7 0 4 0 -42.4770 -0.30574 -0.44510 S3 DOCIIH 3.7070C 34 1.375CE 33 -33.4214 -32.0415 2.754X 01 -0.5 5 7 9 2 -0.81513 70 CRUCITC 1.2400C 15 4.2570E 12 -1 4 .7 0 4 5 -11 .3 7 0 0 2.7244C 04 -3 .5 3 3 4 4 -5.1442? 13 CALCITE 1.071CC 08 2.2070E 07 -7.7231 -0.0444 0.342X100 0.72132 1.34125 144 ccleet 1.2014E 00 3.05C X 07 -7.7202 -0.5140 3.727SC 02 -1.4 0 5 4 4 -2.04434 70 CIIALC 7.1004E 04 4.0730C 04 •3.1451 -3.3104 1.443X100 0.1452? 0.24043 SO COLOR ■05.0202 -08.0800 2.25043 3.28010 21 CIKYSOTL -51 .0 0 3 3 -50.5270 -0 .4 7 4 3 3 -0.47053 30 CLCNEIIT 0 .7 2 7 X 17 2 .7 3 0 X 17 -10.0473 -10.5424 3.257X 02 -1.4 0 4 0 2 -2.14450 57 clinop 7.0074C 24 l.OOOOElOO -23.1180 0.0000 7.4074C 24 -2 3 .11077 -33.45422 100 SILGCL 7.1004E 04 3.5702E 03 -3.1451 -2.4400 2.0022E 01 -0.47043 -1.01485 2? o i o r s io t 2.0233T 30 5.0521E 30 -3 5 .0 7 3 ? -35.2470 3 .5 7 7 X 01 -0 .4 4 4 1 5 -0 .4 4 7 5 0 12 polonite 1.4077C 10 3 .7 0 3 X 1 8 -15.0508 -17.4020 3.5577CI01 1.55114 2.25018 50 ER10N 4.7500C 20 l.OOOOElOO -17.3049 0.0000 4 .7 5 4 X 20 -19.30407 -20.10377 113 rCOII3A 7.7701C 01 7.0730EI04 •0 .0 0 1 0 4.8050 1.300IC 05 -4.BB404 -7 .U 3 0 B 120 rtCTTT 3.3554C 03 1.2102E 04 -2.4743 -3.7150 2.75C7CI01 1.44074 2.07742 03 (1U0R 3.2I71E 11 1.C073E 11 -10.4723 -10.7430 1.701X100 0.25071 0.34477 20 rORSTRIT 1.1132E 33 1.3013E 20 -32.7534 -27.0850 0.5537E 04 -5.04703 -7.3 7 7 7 4 52 G1PCR0 3.707X 34 7.0C37E 33 -33.4217 -32.1033 4.0030E 02 -1.31041 -1.7 1 7 3 4 111 GOCTII -40.1501 -43.0175 2.04745 4.17734 112 GRLCMA -57.7330 -03.1700 5.25420 7.45175 117 GRCG1TC 4.2473E 14 1.0715E 10 -13.3717 -17.7700 3.7457EI04 4.57032 4.47422 17 GT1CUH 4.4307E 07 1.7707E 05 -0 .3 5 3 5 -4.7470 2.4743C 02 -1.40455 -2.33C 02 05 IIALI1C 5.02CCC 05 4.2102E I0I -4 .2 4 7 0 1.0243 1.3370E 04 -5.873C 0 -8.55118 40 IIALLOY 1.1007E 35 1.7320E 31 -3 4 .7 2 7 0 -30.7413 4.0155C 05 -4 .1 4 4 5 0 -4.04550 10? IEHATI 7.7734E 01 3.7305C 00 -0 .0 0 1 2 -5 .4 2 0 2 2.4 7 3 X 1 0 5 5.42700 7.70072 110 IWNTIIE 7.C307E 33 2.0074E-32 -3 2 .1 0 0 2 -31 .4 7 4 9 3 .0 7 7 X 01 -0 .4 0 7 2 7 -0.57501 37 IIYPHAG -47 .4 1 0 5 -3 0 .9 7 5 ? -8.42042 -12.25071 40 1LL11C -30.3372 -37.7704 -0.544C 2 -0.7 7 4 0 4 47 KAOLIN 1.1C07C 35 2.2027E 35 -34.7270 -34.0453 5.21C3C 01 -0.20247 -0 .4 1 1 2 2 44 KHICA -47.7745 -4 5 .7 4 3 2 -2.03123 -2.7 5 7 0 5 127 LAUHON 1 .U 7 X 27 7.327CE 30 -2 0 .7 5 1 ? -27.1347 1.5237EI00 0.10277 0.24434 140 LCON -57 .7 0 3 4 -4 5 .4 1 7 ? 7.51431 10.94222 08 HACKIT 3.3S54E 03 2.330X 05 -2 .4 7 4 3 -4.0310 1.4344EI02 2.15474 3.13777 77 HAGADI 2.3777E 18 5.01I7E 15 -1 7 .0 2 0 2 -14.3000 4.7041E 04 -3.32020 -4.83354 110 HAGICH 7.7734E 01 2.344X100 •0 .0 0 1 2 4.3700 4.254X 07 -4.37114 -7.27511 11 HAGNCCIT 7.4520E 0? 2 .7 7 0 X 09 -0.1277 -0.5242 2.4920CI00 0.37455 0.57730 IOC HAGKCT 7.U20E 04 3.0430E-12 -3 .0 4 0 3 -11 .4 3 0 5 2 .5 0 1 IE 100 0.37012 12.22574 04 HONTCA -42.0070 -42.3104 -0.57725 -0.84034 110 HONlCr 7.5713E 30 1.071X 35 -27.1177 -34.7700 7.0C47CI05 5.85032 0.3168B 117 N0N1AB 5.0024E 20 1.AS9AE-30 -25.3000 -2 7 .7 0 0 0 3.0142CI04 4.4771B 4.52077 58 HORDCN 2.0437E 22 1.000X100 -21.5401 0.0000 2.0437C 22 -21.54408 -31.34471 07 H1RADI 2.0425C 07 5.7770E 01 -0.57C 0 -0.23C1 4.5724E 07 -4.339C 4 -7.22751 5? NAIICOL 1.0C22E-O4 4.201X 01 -3.7741 -0.3744 4 .0 0 3 X 04 -3.3 7 7 5 3 -4.94411 01 NATRON 1 .I2 4 7 E 0 0 2 .5 7 7 X 01 -7 .7 4 0 2 - 0 .5 0 5 5 4 .3 3 C X 00 -7.34244 -10.71854 150 NCSOUE 7.4300E 0? 3.32C0E 00 -8 .1 2 0 0 -5 .4 7 7 7 2.2342E 03 -2.45007 -3 .0 5 7 1 3 55 PHILIP 2.0537E-1? 1.3C04E 20 -1 8 .5 4 4 0 -17.0000 2.0474CI01 1.31543 1.91500 45 M.OG -04 .0 7 0 0 -43 .5 3 0 0 -0.53777 -0.7 8 4 1 1 142 TRCIINT 2.0083E 14 7.0730E 12 -13.5374 -11 .0 4 1 3 3 .1 7 4 X 0 3 -2 .4 7 8 0 9 -3.43471 u s rrR iic 3.7744E 0? 1 .0 7 0 X 18 -8 .4 2 3 2 -17.7573 3 .437X 107 7.5341C 13.88274 54 PTROPH -41 .2 1 7 0 -42.4300 1.21238 1.74478 102 OUARTZ 7.1004E 04 1.7125C 04 -3.1451 -3.7104 3.7441EIOO 0.57334 0.83447 37 CtriOLIT -37 .2 4 4 0 -30.0775 -0.34715 -0 .5 3 4 4 ? 10 SIPLRITC 3 .4 4 0 X 11 1.40I4E 11 -10.4377 -10.7755 2.27D4CI00 0.35744 0.52045 101 SILGLAS 7.I004E 04 1.5402E 03 -3.1451 -2 .0 1 2 4 4.4470E 01 -0.33244 -0.48424 143 STRONT 5 .1 2 3 X 10 7 .1 7 1 X 10 -7.2704 -7.1432 7.1247E 01 -0.14722 -0.21432 38 TALC -57.2731 -40.2134 2.72043 4.25155 00 TIIHAR 2.0012C 07 0.232X 01 -0.5749 -0.2054 4.2701E 07 -4.34957 -7.*'727? 02 TlliNAT 1.I337E 08 7.7057E 01 -7.7454 -0.0041 I .1 4 4 X 00 -7.74132 -11154075 32 TRCH0L1T -120.0010 -134.1432 7.44220 10.04345 00 TRONA 1.7041E 12 2.3740E 02 -11.717? -1.4244 8.0243E 11 -10.09540 -14.49477 154 o t r r i -37.2440 -37.2120 -2.03244 -2.75711 155 PIAEP 3.7D7CE 34 1 .0 7 7 X 30 -33.4214 -35.7470 2 .230X 102 2.34043 3.41003 150 IMIRKT 1.I1C0E 27 3.0410E 20 -20.9513 -25.4154 2.9123C 04 -3.53577 -5.1 4 7 3 4 172 HANGAIIO 3.7021EI07 0.7700EI10 9.5754 14.8310 5.5514C 08 -7.25558 -10.54245 173 PTROLUET 2.I500E 0? 3.2040EI14 -8.0074 14.5145 4.5400E 24 -23.1030? -33.75103 174 DIKNSITC 2 .1 5 0 X 09 1.2331EI1D -0 .0 4 7 4 10.0710 1.7442E 27 -24.75041 -38.95479 175 NUETITC 2.1500E 0? 3 .191X 117 -8 .0 0 7 4 17.5040 4.7370E 27 -24.17141 -30.10024 -3 2 .1 7 1 0 7 170 b i m i t e 3.C722E 24 4 .0 5 9 X 02 -2 3 .4 1 2 0 -1 .3 1 3 4 7 .7 4 C X 23 -22.07041 177 IIAUENITC 34.0035 57.0474 -23.04370 -3 3 .5 4 7 2 3 170 HH0II2 0.4403E 18 1.0920C 13 -17.1711 -12.7231 3 .4 0 4 X 05 -4.44001 -4 .5 0 4 5 1 177 HN0H3 -51.0550 -34.7103 -1 7 .13749 -2 4 .74070 100 HA1IGANIT 1.707IE 12 5.7010E 01 -1 1 .7 0 4 2 -0.2300 3.4077C 12 -1 1 .44010 -1 4.47533 101 RIIOPOCIIR 3.C522C 11 2.3IC5C 11 -10 .4 1 4 3 -10.4340 1.441X100 0.22050 0.32101 183 NNCL2 1.0750E 11 0.0724CI07 -10.7003 7.74C0 1.2124C 1? -10.71437 -27.53037 104 HNa2tlU 1.0747E 11 I.5530E I05 -1 0 .7 4 0 4 5.1714 4.7177E 17 -14.14004 -23.52573 105 HHCL2i2H 1.074IE 11 1.1273CI04 -1 0 .7 0 0 7 4.0528 7 .5 1 1 X 14 -15.02174 -2 1 .04059 ICO HIICL2.4II 1.0720C 11 3.242X 103 -10.7074 3.5108 3.3005C 15 -1 4 .4 0 0 3 7 -21.00047 107 TCrtlRlTC 1.0134EI10 1.C307EI21 10.0050 21.2742 5.3457C 04 -5.27030 -7 .4 7 2 5 ? 100 RHOOONIT 2.3233E100 3.2030EI00 0.3001 0.5134 7.120IL 09 -0.14751 -11.84112 10? HUE CRN 3.5425C 03 3.413X 103 -2.4507 3.5332 I.037X 04 -5.70371 -8 .7 1 1 3 4 170 HNC04 7.0347E 10 9.031X 101 -7 .0 4 4 1 1.7557 1.0004C 11 -10.97702 -14.01350 171 NN2E04>3 -77.2700 -7.5100 -71.75705 -104.44774

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. White Sulphur Springs Bank Well (continued)

DISTRIBUTION OT STCCICS

act IOG A cor I STCCICS TTH HOLALW LOG HOL ACTIVITY LOG ATI . c o c rr. 3.073011101 7.40033E 04 •3.1144 4.23552C 04 -3.3731 5.51477E 01 -0 .2 5 6 5 1 CA -0 .2 5 2 3 7.74003CIOO 7.70307C 04 -3 .5 7 5 3 1.44C53E 04 - 3 .7 7 7 7 5.57332C 01 2 hg -0 .0 4 4 4 4.74437CI02 -1.7307 1.57304C 02 -1 .7 7 7 5 8.57005C 01 3 IIA 1.CSC07C 02 -0 .0 4 7 4 1.77707CI01 4.42737E 04 -3 .3537 3.77373C 04 -3 .4 2 3 2 8.5I776C 01 4 K -0 .0 5 4 4 1.73407C 05 I.72374C 00 -7 .7 4 3 4 1.51354C 00 -7 .0 2 0 0 8.70312E 01 64 II -0 .0 4 7 4 1.44704CI02 4.145I3C 03 -2 .3 0 2 5 3.53156C 03 -2 .4 5 2 0 8.51776C 01 5 CL -0 .2 4 3 5 1.04247CI02 1.72151E 03 -7 .7 1 4 4 1.04754E 03 •2.7770 5.45175C 01 6 504 -0 .0 4 4 4 7 IICOJ 7.45771CI0? 1.22457C 02 -1 .7 1 2 0 1.0554ir 02 -1.7746 8.41046C 01 10 COS 4.O4743CIO0 B.07477C 05 -4.0710 4.4o4S7C 05 -4.3500 5.51771E 01 -0.25B 2 1.7I343CI0I 3.07070C 04 -3 .5 1 0 0 3.10717E 04 -3.5074 1.005500100 0.0024 04 ICtttf -0 .0 4 7 7 :? on 5.45077C 07 3.7I0I3C 04 -5.4735 7.7374'C 06 -5 .5 6 3 4 B.51260E 01 4.14272CI00 3.23C54E 04 -3 .4 0 7 4 2.75406C 04 -3.5576 8.51260C 01 0.0477 41 C -0.041C 17 HCOII 4.4CC72C 03 1.00074C 07 -4 .7 4 3 3 7.43072C 00 -7.0251 8.67343E 01 73 HCS04 AO 5.CD573CI00 4.S7S10E 05 -4 .3 1 0 0 4.72544C 05 - 4 .3 0 7 5 1.O0562EIOO 0.0024 HGHC 2.35447CIOO 2.74435C 05 -4.5501 2.34303C 05 -4 .4 2 4 5 8.54206E 01 -0 .0 4 8 4 22 03 0.0024 0.07454C 01 7.41410E 04 •5.0170 7.47017C 06 -5 .0 1 4 4 1.00562EIOO 71 HGC03 AO -0 .0 4 7 0 2.51743C 01 5.S2250C 04 -5.2347 4.77007E 06 -5 .3 0 1 7 8.57037C 01 70 HOT -0 .0 4 3 0 7.17347C 03 3.0I370E 00 -7 .4104 3.27057C 00 -7 .4 0 1 7 8.6470QC 01 77 CAOH 0.0024 CA AO 1.43223CI01 1.05307C 04 -3 .7 7 7 2 I.05V74C 04 -3 .7 7 4 0 1.O0542CIOO 37 504 8.64700E 01 -0 .0 4 3 0 7.77434CI00 7.C8770E 05 -4.0051 C.54707E 05 -4.0601 30 CAIIC03 1.O0562CIOO 0.0024 4.CI457CI00 4.C2054C 05 -4 .3 1 6 7 4.04744E 05 -4 .3 1 4 5 31 CAC03 AO B.57760E 01 0.0454 I.OSOIOC 01 1.C313CC 04 -5 .7 3 7 2 1.57455C 06 -5.0020 47 CAD B.61064E 01 -0 .0 4 4 4 1.34077CI01 1.14477E 04 -3 .7 4 1 2 7.C4CI3E 05 -4 .0 0 5 0 44 HA504 1.00542EIOO 0.0024 7.OO730CIOO 7.40475C 05 -4.0766 7.45764E 05 -4 .0 2 4 1 43 NAIIC03 0.61046E 01 -0 .0 4 4 4 3.24514CI00 3.74070E 05 -4 .4 0 4 4 3.37434C 05 -4.4670 47 NAC03 1.O0562EIOO 0.0024 3.74545C 30 5.57735C 35 -34.2520 5.62C22C 35 -34 .2 4 7 6 74 NACl 8.6IC64E 01 -0 .0 4 4 4 4.03104C 01 4.47027E 04 -5.3477 3.05277C 06 -5 .4 1 4 2 44 KS04 0.0024 1.37524C 34 -35.0777 1.33272C 36 -35.C 753 1 .00562000 75 IXL 7.04340C 32 -0 .0 4 7 0 3.00777C 04 3.1CS45C 07 -8.4744 2.73241C 07 -0 .5 6 3 4 8.57037E 01 43 IIS04 0.0024 4.02245CI01 7.11034C 04 -3.1401 7.15032E 04 -3 .1 4 5 7 1.00562CIOO 74 II4 SI04 A0 -0.04C 4 II I 1.52245CI00 1.40372C 05 -4 .7747 1.36771C 05 -4.C 633 8.54206E 01 75 35 04 -0 .2 5 0 2 2.4SS7IC 03 2.44377C 00 -7 .5 7 7 7 I.458S4C 00 -7 .0 3 4 0 5.51771E 01 74 II7SI04 0.0024 1.4775CC 01 4.77534E 04 -5 .3014 5.07344C 06 -5 .2 7 7 0 1.00562EIOO 14 1175 AO -0 .0 4 7 7 IIS 2.41U5CI00 7.30307C 05 -4 .1 3 4 5 6.216B3C 05 -4 .2 0 4 4 8.51260E 01 47 -0 .7 4 2 5 I.04720E 04 3.27703C 07 •8.4044 1,77100C 07 -0 .7 4 6 7 5.44377C 01 40 S -0 .2 5 2 1 0.13057C 02 1.45777E 04 -5.0357 0.16700C 07 -6 .0 0 7 0 5.57403E 01 C CC -0 .5 0 7 7 4.2I774C 17 1.1I440E 23 -27.7530 3.46642C 24 -23.4601 3.U 057C 01 7 rc -0 .2 4 2 5 5.73035C 13 8.14475C 10 -17.0000 4.46132C 1C -1 7 .3 5 0 5 5.46377C 01 to cron -0 .0 4 5 4 5.04444C 03 8.04355E 00 -7.0735 6.73272C- 00 -7 .1 5 7 1 8.57740C 01 u non - 0 .0 4 5 4 7.24270C 00 4.00741E 13 -1 2 .1 4 7 0 5.95271E 13 -12 .2 3 2 4 B.57740E 01 17 CCI0UI3 8.4IC64C 01 -0 .0 4 4 4 1.2014CC 07 1.33733C 14 -13.0731 1.15432C 14 -13.7377 77 rc<0ll)7 1 .00542000 0.0024 7.47732E 10 C.70377C 15 -14.0504 C.75404E 15 -14.0400 70 rriOII)3 8.4IC44E 01 -0 .0 4 4 4 S.4C243C 10 4.05724E 15 -14.1637 5.7U 74C 15 -1 4 .2 2 0 3 77 Itia iM 1.00 5 4 2 0 0 0 0.0024 1.77044C 05 1.7737CE 10 -7.7047 ' 1.7S486C 10 -7 .7 0 2 3 co rr2 8.57760E 01 -0 .0 4 5 4 8.04440C 10 5.31713C 23 -22.2742 4.57318C 23 a 46«ilJIU 15 IT504 5.46377C 01 -0 .2 4 2 5 1.3724SE 17 1.50503C 24 -23.0222 8.22786C 25 -2 4 .0 0 4 7 14 CCCL B.57760E 01 •0 .0 4 5 4 2.77247C 22 2.34507C 27 -26.6262 2.03337E 27 -24.4710 70 ICCL7 6.0024 7.04057C 31 -30.1517 7.06B21E 31 -30 .1 4 7 5 1.005620 00 33 rccis 1.14137C 25 0.0024 CCS 3.23277E 02 2.13174C 07 -6.6713 2.I4375E 07 —4,6686 1.00 5 4 2 0 0 0 34 04 -0 .2 5 2 1 B.45737C 02 1.54117E 04 -5.0121 0.62455C 07 -4 .0 6 4 3 5.S7603E 01 io i m -0 .5 0 7 2 107 HN 1.20437C 30 2.175C2C 35 -34.6504 6.83027C 36 -35 .1 4 5 4 3.II057E 01 5.52413C 04 7.70101C 07 -8.1134 4.42171C 07 -0 .1 7 7 0 C.57760E 01 -0 .0 4 5 4 104 HWII - 0 .0 4 5 4 NNI ID 1.30740E 10 1.23412E 15 -14.7077 1.06277C 15 -14.7736 0.57760E 01 107 0 3 -0 .0 4 5 4 HNIIC 4.37777C 02 5.50531E 07 -4.2572 4.73325C 07 -4 .3 2 4 0 8.57740C 01 111 03 0.0024 107 HNS04 1.02377C 02 4.77144E OB -7.1660 6.02763E OC -7 .1 6 5 6 1.005420 00 5.03570E 14 7.01OOOC 17 -10.5477 2.B3465E 17 -10.5475 1.00 5 6 2 0 0 0 0.0024 110 HH(N03)7 -0 .0 4 5 4 1.77341E 03 1.43324C OC -7.0437 1.23224E 00 -7 .7 0 7 3 8.S7760E 01 103 ita 0.0024 1.47CUE 04 1.I744CE 11 -10.7274 1.1C307E 11 -10.7270 1.00542CIOO 104 NNCL7 -0 .0 4 5 4 3.530C3E 07 2.17250E 14 -13.6570 1.C0510E 14 -13.7247 B.57760E 01 105 HMCL3 B.57760E 01 -0 .0 4 5 4 1.44514C 04 1.757C2E 07 -0.7002 1.68326E 07 -B .7730 100 NNT C.57740C 01 -0 .0 4 5 4 7.20742E 13 1.04C74E 17 -16.7772 7.01635C 10 -17.0447 115 IINN07 3.1I057E 01 -0 .5 0 7 2 1.40711E 12 5.74455E 17 -14.2243 I.C5574C 17 -14 .7 3 1 4 51 AL 5.51771C 01 —0.2502 5.03344E 07 1.14624E 13 -12.7407 6.32471E 14 -1 3 .1 7 7 0 57 ALOII B.61C66E 01 -0 .0 4 4 4 4.70747E 05 8.05734E 10 -7.0737 6.74607C 10 -7.15C3 53 Al<0ll)2 8.S7037E 01 - 0 .0 4 7 0 3.50537E 02 3.47574E 07 -6.4323 3.16740E 07 -6 .4 7 7 3 54 ALIOIM 5.51771C 01 -0 .2 5 0 2 4.Z5554E 0? 7.40B7CE 14 -13.0220 S.23574E 14 -13 .2 0 1 0 55 ALT -0 .0 4 4 6 ALC 4.70474E 04 7.40772E 11 -10.1142 6.62574C 11 -1 0 .1 7 0 0 B.61C64C 01 54 7 1.00562E100 0.0024 4.43727E 04 5.20704E 11 -10.2740 5.31674C 11 -1 0 .2 7 4 4 57 ALT3 -0 .0 6 7 0 ALC 4.74372C 07 4.57754E 12 -11.1010 5.63873C 12 -11.2400 B.57037C 01 50 4 -0 .0 6 7 0 3.44537E 12 2.70405E 17 -16.5252 2.55744C 17 -1 6 .5 7 2 2 8.57037E 01 57 AL304 -0 .0 4 7 0 5.C5730C13 2.47707E 10 -17.5722 2.27503C 10 -17 .4 3 7 2 8.57037E 01 40 ALIS04 I7 0.0024 4.23C47EI01 4.S4434E 04 -3.1633 4.70477E 04 -3 .1 6 0 0 I.00562EI00 34 II3D03 AS -0.0731 2.4472CEI00 4.37577E 05 -4.3547 3.71457C 05 -4.4301 B.4477SC 01 37 K7C03 -0 ,0 7 1 5 3.77207C 02 4.44724E 07 -6.1705 5.47022C 07 -4 .2 4 2 0 8.4C174C 01 05 H03 -0 .0 6 3 0 I.14743EI00 1.44771C 04 -3.7027 1.47642E 04 -3.C 450 8.6470CE 01 01 II 0.0024 7.45210E 05 1.02575E 0? -8.7070 1.03152E 07 -8 .7 0 4 5 1.00562E100 02 LIOII 8.57760E 01 -0 .0 4 5 6 7.C00C6C02 7.5C450C 07 -6.1200 6.52264E 07 -6.1C 56 03 LIS04 -0 .2 4 2 5 1.O3430EIOO 2.07735E 05 -4 .4 7 7 7 1.I470BC 05 -4 .7 4 0 4 5.46397E 01 CO SR -0 .0 6 5 6 07 SRffll 2.04244C 05 2.72140E 10 -7.5652 2.33775E 10 -7 .4 3 0 0 B.57760C 01

HOLC RATIOS fROH ANALYTICAL HOLALITV HOLE RATIOS CRON CONTUIED HOLALITY LOG ACTIVITY RATIOS nr/n tt/CA ■ 5.3771EI00 IOG CAD2 s l . u u u i a /C A 4.0533CIOO 8 1.061IE 101 CL/HG < 1.3374EI0I LOG HG/II2 11.8623 CL/HG 8 CL/HA 2.2015C 01 a/«A ' 2.7307C 01 LOG NA/lll 4.0225 B CL/L 7.7646EIOO a/K ■ 7.35C3CI00 LOG K /lll 4.374C B a .'A l 1.11C7CI04 a/AL ■ 6.7473E113 LOG AL/II3 6.72C6 8 2.3427CI03 a /re ■ 2.0374CI03 LOG r r / i c 7.5522 Cl.TC B CL/504 1.0S77EIOO a/soi > 2.1572CIOO LOG CA/HG 0.4046 B CL.1IC03 3.17C5C 01 ci/im ‘ 3.3050T 01 LOG IIA/I. 1.6257 CA/HG 2.6177CI00 CA/HG ■ 2.5744EIOO HA.r 4.20C4CI01 HA/K ' 4.1747EI01

WHITE SaniUR STRINGS CANT. BELLI 0102053

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. BIBLIOGRAPHY

Allmendinger, R. W. Sharp, J. W., Von Tish, D., Serpa, L ., Brown, L., Kaufman, S., Oliver, J ., & Smith, R. B. (1983). Cenozoic and Mesozoic structure of the eastern Basin and Range province, Utah, from COCORP seismic-reflection data. Geology, 11, 532-536.

Anderson, R. E., Zoback, M. L ., & Thompson, G. A. (1983). Implica tions of selected subsurface data on the structural form and evolu tion of some basins in the northern Basin and Range province, Nevada and Utah. Geoloqical Society of America B ulletin, 94, 1055-1072.

Beutner, E. C. (1977). Causes and consequences of curvature in the Sevier orogenic b e lt, Utah to Montana. In Wyoming Geological Association 29th Annual Field Conference guidebook (pp. 353-365). Casper, WY: Wyoming Geological Association.

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Sonderegger, J. L., & Bergantino, R. N. (1981). Geothermal resources map of Montana (Hydrogeologic Map 4 ). Butte, MT: Montana Bureau of Mines and Geology.

Sonderegger, J. L., & Schmidt, F. A. (1981). Geothermal resources in Montana. Proceedings of Montana Academy of Science, 40, 50-62.

Spencer, E. W. (1977). Introduction to the structure of the earth. New York: McGraw-Hill.

Stewart, J. H. (1972a). Initial deposits in the Cordilleran geosyncline: Evidence of Late Precambrian (850 m.y.) continental separa tion. Geological Society of America B u lletin , 83, 1345-1360.

Stewart, J. H. (1972b). Late Precambrian evolution of North America: Plate tectonic implications. Geology, 4., 11-15.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 155

Stewart, J. H. (1978). Basin-range structure in western North America: A review. In R. B. Smith & G. P. Eaton (Eds.), A compilation in Cenozoic tectonics and regional geophysics of the western Cordillera (Memoir 152, pp. 1-32). Boulder, CO: Geological Society of America.

Stoker, R. C., & Niemi, W. L. (1978). First National Bank of White Sulphur Springs well d rillin g evaluation. Unpublished report, E. G. & G. Idaho, In c ., Idaho Falls, ID.

Struhsacker, E. M. (1976). Geothermal systems of the Corwin Springs-Gardiner area, Montana: Possible structural and litho- loqic controls. Unpublished master's thesis, Montana State University, Bozeman.

Suttner, L. J ., Schwartz, R. K., & James, W. C. (1981). Late Mesozoic to Early Cenozoic foreland sedimentation in southwest Montana. In Montana Geological Society 1981 Field Conference guidebook (pp. 93-103). B illing s, MT: Montana Geological Society.

Tanner, J. J. (1949). Geology of the Castle Mountains area, Montana. Unpublished doctoral dissertation, Princeton University, Princeton, NJ.

Telford, W. M., Geldart, L. P., Sheriff, R. E., & Keys, D. A. (1976). Applied geophysics. Cambridge, MA: Cambridge University Press.

Thom, W. T. (1957). Tectonic relationships, evolutionary history and mechanics of origin of the Crazy Mountain Basin, Montana. In Billings Geological Society 8th Annual Field Conference guidebook (pp. 9-2TT Billings, MT: Billings GeologicalSociety.

Thompson, G. R., Fields, W. R., & Alt, D. (1981). Tertiary paleo- climates, sedimentation patterns and uranium distribution in southwestern Montana. In Montana Geological Society 1981 Field Conference guidebook (pp. 105-109). B illin g s, MT: Montana Geological Society.

Walcott, C. D. (1899). Pre-Cambrian fossiliferous formations. Geological Society of America B u lletin , 10, 199-244.

Ward, S. H., Parry, W. T ., Nash, W. P., S ill, W. R., Cook, K. L ., Smith, R. B., Chapman, D. S., Brown, F. H., Whelan, J. A ., & Bowman, J. R. (1978). A summary of the geology, geochemistry, and geophysics of the Roosevelt Hot Springs thermal area, Utah. Journal of Geophysics, 43, 1515-1542.

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Ward, S. H., Ross, H. P., & Nielson, D. L. (1981). Exploration strategy fo r high-temperature hydrothermal systems in Basin and Range province. American Association of Petroleum Geologists Bulletin, 65, 86-102.

Weed, W. H., & Pirsson, L. V. (1896). Geology of the Castle Moun tain mining d is tric t, Montana. United States Geological Survey B ulletin, 139.

Weinheimer, G. J. (1979). The geology and geothermal potential of the upper Madison Valley. Unpublished master's thesis, Montana State University, Bozeman.

Winston, D. (1986). Middle Proterozoic tectonics of the Belt basin, western Montana and northern Idaho. In S. Roberts (E d.), Belt Supergroup: A guide to Proterozoic rocks of western Montana and adjacent areas (Special Publication 94, 245-257). Butte, MT: Montana Bureau of Mines and Geology.

Winston, D. (1987). Sedimentation and tectonics of the Middle Proterozoic Belt basin and th eir influence on Phanerozoic compres sion and extension in western Montana and northern Idaho. In J. A. Peterson (Ed.), Paleotectonics and sedimentation in the Rocky Mountain region, United States (Memoir 41, pp. 87-118). Tulsa, OK: American Association of Petroleum Geologists.

Winters, A. S. (1965). Geology and ore deposits of the Castle Mountain mining d is tric t, Meagher County, Montana. Unpublished master's thesis, Montana School of Mines, Butte.

Wolfe, P. E. (1964). Late Cenozoic u p lift and exhumed Rocky Mountains of central western Montana. Geological Society of America B u lletin , 75., 493-502.

Woodward, L. A. (1981). Tectonic framework of the disturbed belt of west-central Montana. American Association of Petroleum Geologists Bulletin, 65, 291-302.

Zieg, G. A. (1986). Stratigraphy and sedimentology of the Middle Proterozoic Upper Newland Limestone. In S. Roberts (E d.), Belt Supergroup: A guide to Proterozoic rocks of western Montana and adjacent areas (Special Publication 94, pp. 125-216). Butte, MT: Montana Bureau of Mines and Geology.

T IO N

T. 9 N.

rourmil

43 T v b p G s Tad

-Gw

•Gpi -Gm

46 -GDd 46 Mm

Qa Qal

-Gpi

c€D,

;€w

IO N . -GOd 9 N. \ ___ MDt

IPa Mm Jm IP t Mbs

, \ I A T.\ X X\ \ ro„ Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Qal

Qal p-Gg

p € g

T s

pGs

p-Gs Q ls

74 < 1 .88 / PC Kk I P t ^ Qal

p€g / k88 4 3 \

f t

p«g

- 32 30

rjL'jrl v" Qal

/ // ^ ,c9v^’- r / —// 1/ X'ilC-v/W," N -VnN'j 42/ / ^ ‘/( • /J / '"x' ' l C. N«-/' / (P it Is ■ > ; v.ttoiz \ O j -

36 / EXPLANATIOI

'P€9' J \> t\ q qI Quaternary alluvium

Q ls Landslide deposits 51' MmA M b s.4e

p € g T ~< I 1 \ -* I ' > Ts Tertiary sediments

451 Tvb Volcano Butte basalts

N N \ T rp Rhyolite porphyry i s - 1 ^ l j .> I /■ I V Y : ; 1. Q ls Castle Mountain :.>C# granite and syenite 4vyi.rf* f e 4 /H•*■ ?■ 1 ; / ' . 1 ^ I 1 r'1' . v v \ 1 *

32 30

EXPLANATION

J\ 83^\ \\J > Quaternary alluvium ' \ + A rpa* - QUATERNARY Landslide deposits

Tertiary sediments //V s' -

Volcano Butte basalts

Rhyolite porphyry TERTIARY

Castle Mountain granite and syenite

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. N\

Cretaceous (undivided)- Mowry and Ku Thermopolis Shales *,Frontier Formation

Kk Kootenai Formation

Jm Morrison Formation

TPq Quadrant Formation

IPa Amsden Formation

IPt Tyler Formation i A ' 7 s' , 7 \ - s. I Xx7n -l /' '' x • • ? " ;",'■ I I r \ , i \ ^ r " - - -■' Mbs Big Snowy Group I'r - ; '- '> / j : ;' -'/ L ' -"■ r.'A N- t s. 1 7 N- s -*s- \ . i , 1 -N-' w \,. —' ■• ~ ^ ,y C s' - 's v,'*'''t Mm Madison Group - undivided N I 7 7>7 A 'I.v i : N-Ji\ -77

Mmc Mission Canyon Limestone

Ml Lodgepole Limestone

M Dt Three Forks Formation V - 7 - ; v i

Dj Jefferson Formation

-GDd Red Lion - Maywood Formations

-Gpi Pilgrim Limestone

-Gp Park Shale

•Gm Meagher Limestone

■Gw Wolsey Shale

•Gf Flathead Sandstone

p£s Spokane Shale

p-Gg Greyson Shale lwO| O w ♦ l p-Gn Newland Limestone

T a d Andesite

Cretaceous (undivided)- Mowry and Ku Thermopolis Shales; Frontier Formation - CRETACEOUS Kk Kootenai Formation

Jm Morrison Formation 3- JURASSIC jtie

!Pq Quadrant Formation PENNSYLVANIAN IPa Amsden Formation

IPt Tyler Formation

Mbs Big Snowy Group

'.S '/s ir'' w s 's -'-i '/ i r ' S ' Mm Madison Group - undivided -MISSISSIPPI Mm c Mission Canyon Limestone

^ / isV'x '' t-.,m :./v -:; Ml Lodgepole Limestone

. \ ^ i - . - .'x \ v /:t;, / Three Forks Formation A A 'l M Dt ' ' I V" Dj Jefferson Formation -DEVONIAN

-GDd Red Lion-M ayw ood Formations —

-Gpi Pilgrim Limestone

■GP Park Shale CAMBRIAN -Gm Meagher Limestone

■Gw Wolsey Shale

-Gf Flathead Sandstone

N \ p £ s Spokane Shale a . \ 3 S o \ . k . CT>l_ p-Gg at Greyson Shale a. - PRECAMBRIAN 3 . CO p-Gn *a3 Newland Limestone GO

p-Gs

17,0 AMN

APPROXIMATE DECLINATION, 1977

R.6 E. R.7 E.

p € s Spokane Shale \ p-Cg Greyson Shale

p-Gn Newland Limestone

Formation contact— dashed where a pi

■ —— Fault contact — dashed where approxin

\ \ N . — Fault —showing relative lateral movem -Gpr -v v \ Thrust fault — teeth on upthrown side approximate O'v "^N N\ \ xv ^ ^ G D 3< ^ x s \ x Normal fault — barbells on downthrowr ■ S S\'kv \ \ where approximate ■Sj. N S N N ^ n \ N] !La T Normal fault reactivated along previo \ M D * - > < n S' V n thrust, dashed where approximate \ N. \ \ n\ + -10

1 KILOMETER _ Syncline

Overturned syncline

104° 116° 112' 4 9 ° Minor fold showing trend and plung<

Strike and dip of beds

47 _ii° Inclined Vertical 75 MAP AREA "ch Overturned 45 Horizontal

INDEX MAP SHOWING LOCATION OF AREA

Geology by William G. Gierke (1986) Modified from Gardar G. Dahl, Jr. (1971) and George B. Phelps (1969) PLATE

Spokane Shale Ql 3 O O' Greyson Shale

a) Newland Limestone ao

Formation contact— dashed where approximate

Fault contact —dashed where approximate

Fault — showing relative lateral movement sense

Thrust fault — teeth on upthrown side, dashed where approximate

Normal fault — barbells on downthrown side, dashed where approximate Normal fault reactivated along previous Laramide thrust, dashed where approximate Anticline showing trend and plunge of axis

Overturned anticline

Syncline

Overturned syncline

Minor fold showing trend and plunge of axis

d dip of beds Inclined Vertical Overturned Horizontal

GEOLOGIC CROSS SE

A 7000-1

6000-

Qal Ts Qal 5 000- L. 4 0 0 0 - pGg p-Gs

3000-

2000

70001

6000- ,Qal 5000- a> CD U. 4000- p€s p€g

3000-

2000

7000 1

6000- Js Qal €w -6m MmcTs

5000 -Gm Mbs

4000- p-Gs Mmc

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. SECTIONS OF THE WHITE SULPHUR SPRINGS AREA, I By William G. Gierke 1986 Craig thrust Moors Mountain thrust Tod -j { rMbs_

Moors Mountain thrust Willow Creek syncline p€g p-eg Qal

Mb! Kk -Gpi n p-Gg tttej \ JVnAMDt Mm Mbs

•€w

•GDdMDt

Mbs

Mmc •eoi

A F * E a > MONT a Na

I^ 'y o n ,ault

>40q i>

Clnm i

“W ight om er further reprod pr°hibiteci without 1 4 0 0 Perrpissi0n. ® Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced

Feet Feet 7000 -|7000 2000 4000- 2000 5000 6000- 3000- 4000- 5000- 000- 6 Ts p-G s p-Gg p€s r p€s Qal ,Qal •Gm Ow- ?^ *? m -G w -O MDt p-Gg Mmc Js Mbs Mm Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Moors Mountain thrust Willow Creek syncline P-Gg p-Gg Qal Ts IPa

■Gw-

Mbs

•Gp -GDd vMDt

MDt •GDd

Mbs

Mmc •GDi

Scale 1:24 000 .5 0 I MILE

.5 I KILOMETER PLATE 2

Willow Creek syncline -1800 Mt Qal

Kk MDt -1400

Mm Trp -1000 / p€s?

600 •€w

Castle Mt. stock

r 2200

- 1800

Teg p£g -1400 Meters Meters Meters

HOOO

600

I MILE

19 J O

1 3 .5 0

1 3 .2 0

1 3 8 5 21.00

I 7 .9 i

1 2 . 9 4 1 4 . 9 6

1 4 .2 0

18. 19.

'30" 55' 110° 52'30" 50' ...... i ...... I I'

t O . 7 3

2 2 . 4 6

2 3 . 1 7

2 1 .7 3

2 2 . 4 6

17.91

1 7 3 6

1 6 .6 7 2 0 . 7 7

1 3 0 5

1 7 .9 2

1 3 .5 3 1 0 .7 6

1 1 .6 3

110° 52 30' 50 47*30'

2 3 . ( 7

2 1 .4 2

• 19.20

1 0 .6 7 2 0 . 7 7

( 7 . 9 2 ^10.47 # ( 7 . 0 0 BASE 2 '•*”

32*30-

(0 .7 9

V v * Reproduced with permission of the copyright owner. FurtherFurther reproductionreproduction prohibitedprohibited withoutwithout permission.permission Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 10.50

SCALE 1:48 0 0 0 .5 _____ 0 I MILE

I .5 0 KILOMETER l-l M M MI-1 P

CONTOUR INTERVAL Imgal 1 6 .3 4

1 4 . 9 8 + MBMG gravity station (Michael Stickney, 1981) with relative Bouguer anomaly value

l9;#7 Gravity station (William G. Gierke, 1982) v

BASE 2 ,®47 Base station with relative Bouguer anomaly 12.00 value

1 3 . 0 0 Observed Gravity at Base Station I (980484.00) was choosen arbitrarily to achieve positive relative Bouguer values with the reduction program used.

Note: No terrain corrections applied

PLATE 3

By W illia m G. G ierke 1986

11.15 1 4 .6 0

18.80

164 ' 18<41

1 8 . 3 4

14 3 4

1 0 . 8 4

12.00

1 8 . 7 8 16.32

3 . 0 0

1 0 .2 7 1 2 . 0 8 1 2 .1 7

1 8 .2 0

1 7 . 2 8

1977

46 30

1 4 - 3 4

1 9 .7 9

13.91

1 7 .2 9

IB .61

/ / Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 5 7 3 0 III 0 0

8-81 O 4 9 6 8 O 1965

1946 4970

8 -8 1 •4 9 3 7 8-61 .4 9 5 9

7-81 4 8 8 4

8-73 4954

4 9 0 0 8-81 4919

8-81 O 12-63 4921 4926

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. : r t a b l e m a p , w h it e s u l p h u r s p f

8-81 ,4970

Lfl (968

O 1969 O 5001 ,

1948 2-80 4997, 5019 1946 1947' 4970 500C

8-79 5014 !2-63\ 12-63 5051 ) f 5051

1952 8-81 5016 5057. 1-81

5001

8-81 4982 1964 4957 O z S l 4987/ 8-81 10-79 5069 6 4956 498'

8-81 8-81 4960

12-80 4958 8-81 4987 8-81 9-80 8-81 4998 4985

110° 52' 30" 50' 5120

5110

5 0 9 0 i d ? ? S ,0 °

12-62 \ 5 0 8 0 10-61 5115

4-62 7-81 O 5065 8-81 5217

I 12-63 £ 5051

8-81 5069;

8-81 5108 > If 3 2 3 0

Scale l: 24 000 I MILE

I KILOMETER

CONTOUR INTERVAL 10 FEET-dashed where approximate TN MN

o water well location ” date measured Declination, 1977 4987 - water table elevation • thermal well (ft, msl)

spring

8-81 O 12-63 4921 4926

4910

4 9 2 0

8-81 4948

7-81 4956 . 0 9 f t * .

8-81 4 9 6 0

12-80 8-81 4 9 5 8 4 9 8 7 8-81 8 -7 9 4931 ■983 9 -8 0 8-81 4 9 9 8 4 9 8 5

■ 9 -8 0 .5012

12-77 O 4987 7 -8 0 5 0 0 5 o '

1942 . 4 9 9 6

3-63 ' 7-SI 0 5 0 0 2 4 9 5 7 O

7-81 7-81 4 9 5 6 O 5 0 0 0

o water well location “ date measured Declinotion,l977 4 9 8 7 - water table elevation • thermal well (ft, msl)

f> spring

j * thermal spring

^ ^ Stratigraphic profile (Appendix D)

Groundwater flow direction (approximate)

.4 9 7 0 ' Groundwater elevation contour (dashed where approximate) in ft,msl

o 1 4 6 3 0 PLATE 4

By W illiam G. G ie rke

1 986

III 0 0

II0 ° 5 7 '3 0 "

9 .2

•*.0

9 .4

no* 5 5 '

10.0

\Oy

10.0

6.3 6.0

10.0 7.8

,4 1 3 ,

15,3 11.4

,15.0

13.0 12.2

9 .0

110° 52' 3 0 " 5 0

3 4 '3 0 "

9 .4

SCALE 124 000

.5 0 MILE

I .5 KILOMETER m :

Contour Interval 10 intervals per decade, °C

I0..0 o Well location with water temperature in °C

• Thermal well

/ \ P Thermal spring Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 12.2

11.7 9 .0

11,0

f0.Q

9 .2 O 90

Contour Interval 10 intervals per decade, °C

10.0 o Well location with water temperature in °C

• Thermal well

>• Thermal spring

Area with ground water temperatures suitable for heat pump use.

TN ..MN j 17°/

1977

46°30' 3 0 " PLATE 5

By W illiam G. Gierke 1986

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. MAP, FLUORIDE, WHITE SULPHUR SPI

110° 5 2 ' 30'

.45 O

.63 O

.5 6

.2 9

6 .3

7.07

7 .7

2.21

.5 0

• 88

.19 •4 0

•63

V Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. JLPHUR SPRINGS, MONTANA

110° 5 2 ' 30" 5 0 '

34 .35 O

.2 9

.44

46 32 30

SCALE i: 24 000

.5 0 I MlLEJ

.5 0 I KILOMETER BCZQZBZE

CONTOUR INTERVAL 5 intervals per decade, mg/l FLUORIDE

.56 o' well location with fluoride concentration (mg/l)

Reproduced with permission of the copyrigM o w T e r. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. .2 9

6 .3

7.07

7.7

2.21

.5 0

.30 .88

.19 4 0

.40 .3 7

4 6 3 0 ' .43

.44

4 6 32 3 0 -

SCALE i: 24 000

.5 0 I MILE

• 5 I KILOMETER

CONTOUR INTERVAL 5 intervals per decade, mg/l FLUORIDE

.56 o well location with fluoride concentration (mg/l)

• Thermal well

Thermal spring

.37 O

1977 PLATE 6

4 6 3 0 ' 30" By W illiam G. Gierke 1986

110° 57 30

4 3 5

562

5 7 8

472

627

55' 110° 5 2 '3 0 " \

435 O

3 9 5

682

509

2169

,2371

8 0 6

509 728

387 809

650

110° 52' 30"

_ .1 _ _ II 3 4 3 0 -

4 0 3

358

509

253

4 6 °3 2 '3 0 " - SCALE 1:24 000 I MILE

I .5 0 I KILOMETER l= h _ i- h i— i t—-i i— i i - - - i CONTOUR INTERVAL 8 Intervals per decade, LAB SPEC. COND. (micromhos/cm)

6 5 0 well location with spec. cond. (micromhos/cm)

Thermal well

Thermal spring

Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 5 0 9 728

387 8 0 9

6 50

513 625

3 9 4 410

.5 0 I KILOMETER

CONTOUR INTERVAL 8 intervals per decade, LAB SPEC. COND. (micromhos/cm)

G50 o well location with spec. cond. (micromhos/cm)

• Thermal well

f Thermal spring

1977 PLATE

By - 4€?30' 30" William G. Gierke 1986 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.