7019 - apps.dtic.mil · 5 report documentation page 0-m o 74-0188 public reporting burden for this...

rh NWC TP 7019Volume 1

A Water Geochemistry Study of Indian Wells Valley,tI Inyo and Kern Counties, California

Volume 1. Geochemistry Studyand Appendix A

I -by

J. A. Whelan and R. BaskinUniversity of Utah, Salt Lake City, Utah

andA. M. Katzenstein

Geothermal Program OfficePublic Works Department

SEPTEMBER 1989

1.NAVAL WEAPONS CENTER

CHINA LAKE, CA 93555-6001

.,. 3E 0519894Approved for public release; distribution isL U 0 ,unlimited.

Irt.

L" C /t.' ,,~<

5 REPORT DOCUMENTATION PAGE 0-M o 74-0188

Public reporting burden for this collection of information is estimated to average 1 hour per respone. including the time for reviesrng instructions. searching existing data sources. gathering andmaintaining the data needeid, and comp~lting and reviewing the ollection of information. Send omments regarding this burden estimate or any other aspect of tis ooliscllaan of information. including

suggestions for reducing this burden, to Washington Headquarters Services., Directorate for Information Operations and Reports, 1215 Jefferson Davis Highway. Suits 1204. Arlington. VA31. AGENCY USE ONLY (Leae bilrilo 2. REPORT DATE 3. REPORT TYPE AND DATES COVERED

1989, September Final, 86 Sep-87 Feb4. TILE AMD SUBTITLE S. FUNDING NUMB3EPS

AWater Geochemistry Study of Indian Wells Valley, Inyo and Kern Counties Prog. Element No. 63724NICalifornia, Volume 1. Geochemistry Study and Appendix A (U) Project No. R0829____________________________________________________ Work Unit No. 520A

6. AUTHOR~S)

Whelan, J. A., R. Baskin, and A. M. Katzenstein

7. PERFORING ORGANIZATION NAME(S) AND ADDRESS(ES) All PERFORMING ORGANIZATIONREPORT NUMBER

Naval Weapons Center NWC '1? 7019, Volume 1China Lake, CA 93555-6001

9 . SPONSORING/MOIITORING AGENCY NAME(S) AND ADDRESS(ES) 10. SPONSORINGMOITORINGAGEN4CY REPORT NUMBER

Naval Weapons CenterK China Lake, CA 93555-6001

11. SUPPLEMENTARY NOTES

12n. OISTRISUTIOWIAVAILABIUTY STATEMENT 1 2bL DISTRIBUTION CODE3 A Statement; approved for public release; distribution is unlimitedI

313. AB3STRACT (ildaarn 200 words)

(U) The geochemistry of groundwater in Indian Wells Valley (IWV) was studied using water analyses available from theU. S. Geological Survey supplemented by samples taken by the University of Utah and the Naval Weapons Center (NWAC). The£ geochemical findings reveal possible sources of leakage of geothermal waters into the IWV.

(U) In the IWV and related areas, of 254 water types possible, some 55 are present. By grouping similar types of watertgether, eight major water types were mapped:

1 . Alpine waters (calcium-sodium-magnesium-bicarbonate type)to 2. Sodium-chloride waters

3. Sodium-carbonate waters4. Sodium-bicarbonate watersI5. Sodium-bicarbonate-chloride waters6. Sulfate waters7. Red Hill/Little Lake/Lumber Mill Waters (calcium-(sodium-magnesiun)-bicarbonate-chloride-(sulfate)) waters8. The waters of the well fields (usually sodiumr-calcium, but sometimes calIcium-sodium-bicarbonate-chloride)

(U) Geothermal leakage into IWV occurs from Coso, areas west and just north and south of the main gate of NWC, thesouthwestern part of the IWV, and Haystack Peak in the Spangler Hills. (Contd. on back)

K4 SUBSJECT TERMS IL. NUMBER OF PAGES

Geochemistry Aquifer Groundwater 88

Geothermal Geothermometry Is. PRICE CODE

17. SECUWIY CLASSIFICATION it. SECURTY CLASSIFICATION 1S. SECURITY CLASSIFICATION 20. LIMTATION OF ABSTRACTUOF REPOIRT OF TIS PAGE OF ASTRACTUNCLASSIFIED UNCLASSIFIED UNCLASSIFIED

NSN 7540-01-280-5500 Standard Form 298 (Rev. 2-89)I 256. ~t0-'"j ANSI tfdZ

UNCLASSIFIED ISECURITY CLASSIFICATION OF THIS PAGE (When Data Entered)

19. (Contd.) 3(U) Thrust faulting and associated listric, landslide, and relaxation faulting in the Sierra, the Coso and Argus Ranges, and

under the IWV provide other avenues for subsurface inflow. Data indicate significant inflow into the IWV from Rose Valley.Inflow from the Sierran granitics is indicated by the Tungsten Peak Mine, which produced 180 acre-feetof waterperyear whenin operation. Besides evaporation from China Lake Playa and transpiration by plants, other possible losses from the IWV aresubsurface outflow to Searles Valley through Salt Wells and Poison Canyon, interbasin flow to Searles Valley beneath theArgus Range, and interbasin flow south towards Koehn Lake.

(U) With the exception of a few wells in the Ridgecrest field, water quality has changed little with time. Water quality may Iimprove, deteriorate, or remain constant with depth, depending on well location.

(U) The geochemical data of this report, when integrated with the structural and other data, may point to additional criticalsites that should be sampled. I

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qt,nird I", ' {, ,Z-SECURITY CLASSIFICATION OF THIS PAGE

UNCLASSIFIED

3 NWC TP 7019, Volume 1

CONTENTS

1 Introduction ............................................................................... 3Conversion Factors ........................................ 3Well-Numbering System in California ......................................... 6

Climate of the Indian Wells Valley ................................................... 6

Previous Studies ............................................................................. 7

Geology ................................................................................... 9

Theory Behind Geochemical Investigations..........................11On-Site Measurements: Temperature, pH, and Conductivity .................... 11Analyses of Elements and Compounds .......................................... 12

I Study Techniques ....................................................................... 14Sampling Techniques/Instrumentation .......................................... 14Analysis Techniques .............................................................. 15Interpretation Techniques ........................................................ 16

Gross Water Classification by Major Ions .......................................... 18

Conductivity Versus Total Dissolved Solids ........................................... 19

Determination of Groundwater Flow System Cells .............................. 19

Thrusting and Listric Faulting Could Provide Major Water Collectors .............. 27

Water Types ............................................................................ 28Water Types Defined by This Study ........................................... 28Groundwater of the Inyokern Intermediate and Ridgecrest Well Fields ........ 325 Water Types According to Township ............................................... 33

Changes of Water Quality ........................................................... 38Changes With Depth .............................................................. 38Changes With Time .............................................................. 38

Geothermometers ..................................................................... 43

Summary and Recommendations .................................................... 49

References .............................................................................. 51

Appendixes:A. Indian Wells Valley Geothermometry 1920 to 1986 ................... A-1B. Conductivity Versus Total Dissolved Solids Curves ........................ B-1C. Water Chemistry Terrain Triangular Plots ............................... C-1v. Tiidangular Plots Showing Carbonate-Sulfate Affinities ..................... D-IE. Sampling Data, Analyses, andi Stiff Diagrams

Done Specifically for This Study ................................ E-1F. Data Regarding Computer Printouts ........................................... F- I

G. Modified Stiff Diagrams ....................................................... G-1

NWC TP 7019, Volume 1 1Figures:

1. Location of the IWV Groundwater Basin (Modified From Lipinskiand Knochenmus, 1981) .................................................... 4 I

2. Diagram Locating Well Sites Using USGS Well-Numbering System ...... 53. Water Types at the Naval Weapons Center and in the Indian

W ells Valley .................................................................. 20 I4. Triangular Plot of Water Types in the Indian Wells Valley and

Other Areas .................................................................... 255. Weathering of Carbonates and Sulfates ................................... 266. Grumpy Bear Well in 22S/36E-21 ....................................... 287. Sodium-Chloride Waters .................................................... 298. Sodium-Carbonate and Sodium-Bicarbonate Waters ..................... 309. Tungsten Peak Mine in 26S/38E-10H, on 9-16-86 ...................... 31 I10. "Sewage Water," in 26S/40E-22H2, on 6-8-82 .......................... 31

11. Little Lake Spring, in 23S/28E-17, on 9-18-86 ........................... 3312. TDS at Well 26S/39E-21N and Closest Surrounding Wells ........... 3913. TDS Versus Depth in Wells in 26S/39E-19 .............................. 4014. TDS Versus Depth in Wells in the Sections Noted ......................... 4115. Temperature Contour Lines as Calculated From the

Quartz-Conductive-Cooling Geothermometer ............................. 4516. Temperature Contour Lines as Calculated From the

Na-K-Ca Geothermometer ................................................. 4717. Approximate Locations of Three Thermal-Gradient Drill Sites I

at NW C ....................................................................... 48

Tables:1. Glacial Periods ........................................ 102. Detection Limits and Analysis Techniques ................................ 153. Conversion Factors for Milliequivalent Conversions .................... 164. Analyses of Sodium-Chloride Type Brines ................................ 29 I

IACKNOWLEDGMENTS

We greatly appreciate the cooperation and assistance received from the people of Indian IWells Valley; the Eastern Kern County Resource Conservation District; Kerr-McGee Co.,Trona, Calif.; Leslie Salt Co., Newark, Calif.; California Energy Co., Santa Rosa, Calif.;and the U.S. Geological Survey (USGS), Water Resources Divisions. Dr. Carl F. Austin, 1of the Geothermal Program Office, Public Works Department, Naval Weapons Center, wasparticularly helpful in arranging for sampling of wells in areas of poor spatial coverage.James Nichols (a university intern) and John Wolfe (an undergraduate student) did muchextensive computer work on the project through special topics courses at the University of mUtah, and also contributed significant ideas during the interpretive stages.

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NWC TP 7019, Volume 1

1

I INTRODUCTION

This report summarizes the results of a study of the geochemistry of groundwater in

Indian Wells Valley and uses the geochemical results to make inferences about possibleleakage of geothermal waters into the Valley. The Eastern Kern County ResourceConservation District (EKCRCD) supported much of the geochemical studies with agenerous grant to the Department of Geology and Geophysics, University of Utah.Additiond chemical work and evaluation of geothermal potential was done by theGeothermal Program Office, Naval Weapons Center (NWC), China Lake, California.

Groundwater studies have been done in Indian Wells Valley since those of Lee (1913)to the present (see the section Previous Studies). These studies are of varying quality. Inaddition to the nearly 1,200 water analyses taken from previous studies, 23 new sites weresampled for water analysis. In total, over 370 sites were sampled (many with numerousanalyses) for this study. The EKCRCD and the Geothermal Program Office realized thatgroundwater alone is but one component of the local geological environment and that toadequately understand groundwater, the total geological environment must be understood.For that reason, the studies conducted by these two organizations included studies ofstructural geology and shallow heat flow, this study of water geochemistry, and waterisotopes. The isotope studies will be published later. As far as we know, these variousstudies combined are the first truly integrated study of a groundwater system in a desertbasin. Appendixes A through G of this report offer more detailed and extensive3 information on work done for this study.

Indian Wells Valley is located in eastern Kern County, southern Inyo County, andnorthwestern San Bernardino County (Figure 1). The principal settlements in the area areRidgecrest, China Lake, Inyokern, and Little Lake. The largest employer in the area isNWC. Commissioned in 1943, the Center employs approximately 5,000 civilians and1,000 military personnel, and directly supports approximately 2,500 contractor personnel3 in the Valley.

3 CONVERSION FACTORS

The results of chemical analyses and temperatures in this report are given in metric unitsrather than the more familiar English units. Concentrations are reported in milligrams perliter (mg/L) or micrograms per liter (pgg/L), and water and air temperatures are reported indegrees Celsius ('C).

Milligrams per liter is numerically nearly equal to the unit parts per million (ppm) forconcentrations of less than about 7,000 mg/L. Parts per million was formerly used by theUSGS to report the results of its chemical analyses.

I Micromhos per centimeter is now reported as microsiemens per centimeter. The

quantities are equivalent and the nomenclature is interchangeable.

13£

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11000" 11130 '

OWENSIJLAKE

3 M NAP

CENTER BOUNDARY _ ANELE AREA

<Approximate:R., boundary of .....

ground-water basin

COSO RANGE

36000 - £ I~VALLEY! /\. .ROSE

36000'r V LLE

SEARLES

INYO co I INDIAN WELLS I VALLEY

KERN CO-B ,rown 4.CHINA Troan

' AVALLEY 2 LA KE,,, lrn \. . .. -, L ,"

Rdgcrsujl~...Rigerejh \" X POISON CANYON

c'" 1cI SALT WELLS

35030' -

.. / I

141

10 NILESI

FIGURE 1. Location of the IWV Gmundwaer Basin(Modified From Lipinski and Knochenmus, 1981). 3

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I3 NWC TP 7019, Volume 1

£

Ii41W. ___ .5 1. 3.L l.t.

T.2 iI -,

6 5 30 2 6

I \E F G H'19 2229

£\ M Loj K J\ - lN/SE-z9u-\N P 0 R

FIGURE 2. Diagram Showing Relationship of Townshilp, Section, and Subdivisioni for Locating Well Sites Using USGS Well-Numbering System.

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INWC TP 7019, Volume 1 3

WELL-NUMBERING SYSTEM IN CALIFORNIA

Figure 2 shows the relationship of a township, section, and subdivision for locating Iwell sites using the USGS well-numbering system. Well locations in this report are givenin this format.

The USGS well-numbering system used in California indicates the location of wellsaccording to th.z: rectangular system for the subdivision of public land. This rectangularsystem is based on divisions called townships, which are 36 square miles (although thesize can vary considerably in actual practice) ana are numbere-d according to their Irelationship to a base line and a meridian. The townships in Indian Wells Valley aremeasured from the Mount Diablo Base Line and Mount Diablo Meridian. In Figure 2, theMount Diablo Base Line provides the north-south reference and the Mount Diablo Meridian Iprovides the east-west reference. For example, T1N/R5E is one township north of theMount Diablo Base Line and is five townships east of the Mount Diablo Meridian.

Well numbering follows the township-numbering system and uses further, more Ispecific, designations. Figure 2 shows the location of well number 1N/5E-29L1; the firstnumbers and letters designate the township (TIN) and the range (R5E),; the third numbergives the section (sec. 29); and the letter indicates the 40-acre subdivision of the section.The final digit is the serial number assigned to this particular well; the wells in each 40-acresubdivision are given serial numbers to identify them within that subdivision. g

CLIMATE OF THE INDIAN WELLS VALLEY I

Climatological data were obtained from the Final Environmental Impact Statement,Proposed Leasing within the Cuso Known Geothermal Resource Area (Bureau of Land IManagement, 1980). The climate of Indian Wells Valley, typical of the southern Californiahigh desert region, is characterized by hot summers, cool to cold winters, large diurnaltemperature changes, low humidity, and little cloudiness or visibility restricticns other than Ioccasional blowing dust.

Local topography is an important climatic factor. The Sierra Nevada mountains to thewest form a barrier to passing storms and frontal systems, and create a rain shadow effect.The air is warmed as it descends down the lee side of these mountains, and the potential forcondensation is decreased. As a result, precipitation varies from 20 to 55 inches on thewindward (west) side of the Sierra to less than 10 inches annually on the east side. Annual Iaverage precipitation in the center of the Indian Wells Valley is about 3 inches.

Snowmelt is an important part of groundwater recharge in the Indian Wells Valley area.The Bureau of Land Management has developed a formula to predict snowfall based on Ielevation:

Y =0.57 x e1 .5 1 x 10-3 x X Iwhere h

X = elevation in feetY = the average annual snowfall in inches

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II NWC TP 7019, Volume 1

The correlation coefficient was 0.84. Nine inches of snow is equivalent to about 1 inchof water. The average of the mean annual temperature at the NWC weather station is64.0'F. Monthly normal temperature range is from 43.10 F in January to 86.2'F in July.Ile daily temperature extremes show a normal daily minimum in January of 28.7'F whilethe normal high of 102.3'F occurs in July. The 50% probability date of the last spring3 frost is around April 1.

The mean monthly relative humidity values at China Lake range from 23% in July to52% in December. There is an average of 74 days (20.3%) per year of total cloud cover,with a maximum number of cloudy days per month during the winter season and amaximum number of clear days per month during the summer and early fall seasons.

Prevailing winds are from the south-southeast or north-northwest at all times of theyear. Long-term data show average annual wind speed at China Lake to be 8.2 mph, withthe highest monthly average (10.4 mph) occurring in May. There are occasionally highwinds from the north and from the west, the strongest ever recorded in China Lake was 81mph in March 1952.

Summer thunderstorms are not uncommon; localized torrential rains and flash floodingcan occur from June through October. Every few years, heavy lasting summer rains occurwhen a hurricane off Baja California pumps moisture into the area and traps it against theeast side of the Sierra, temporarily reversing the rain shadow effect.I

3 PREVIOUS STUDIES

Many studies of varying length and quality have been done of groundwater in theIndian Wells Valley. None, however, addressed the regional groundwater flow system orgroundwater flow system cells (areas of groundwater types) to any extent.

The earliest studies were those of Lee (1913). Another early study of groundwater wasthat of Whistler (1923). The first USGS study of the area was that of Thompson (1929).He published some analyses and proposed a water budget for the basin. The first Navy

3 study of groundwater was that of Buwalda.*

In 1951, Wilcox, Hatcher, and Blair published a paper on the quality of water of theIndian Wells Valley.

In 1959 Dutcher published data on water wells in the Fremont Valley area. In 1963Moyle published data on water wells in Indian Wells Valley area. His publication containsavailable well data and 220 water analyses (not all comr lete). Quality control over theanalytical work appears to be good.

Findings of Kunkel and Chase. Kunkel and Chase (1955), in a USGS study forthe Navy, calculated a water budget; supporting tables are available in Kunkel, Chase, andHiltgen (1954).

I * Buwalda, J. P. 1944. Underground Water Supply in Indian Wells Valley,for Inyokern Naval Ordnance Test Station: unpublished report to Commanding3Officer.

7


In 1969 Kunkel and Chase published a USGS open-file report entitled "Geology andGround Water in Indian Wells Valley, California." (See the Geology section of this report.)

Kurkel and Chase did not have either the number of analyses now available or thepresent computer capabilities. They grouped different waters together based on a schemeinvolving 50% of the milliequivalents (1969, p. 51). They compare their Group I waters m(low total dissolved solids (TDS) sodium-carbonate waters with low fluoride and boron) tothe alpine maters and place this group in the Inyokrn well fields and areas to the north.(For a discussion of what exists north of Inyokern, see the sections on sulfate waters andRed Hill/Little Lake/Lumber Mill site waters in the Water Types section.)

Waters classed Group I are also sodium-carbonate waters of low TDS but with higherboron and fluoride contents. Kunkel and Chase place these waters from the main gate of INWC to about 1 mile n'rth of the intermediate well field. They consider their Group IIwaters to be alpine waters modified by base exchange (ions from water going into amineralized zone releasing different ions into the water). They attribute the minerals with Iexchange properties to be zeolites. We believe that clays in the alluvium and valleysediments are more probably the minerals exhibiting a base-exchange potential.

The waters classed Group II are sodium-chloride waters. These, of course, includewaters in and near China Lake playa (a dry lake) and waters to the south and east ofRidgecrest. Kunkel and Chase postulate a clay barrier restricting the movement of the latterwaters eastward. They attribute the sodium-choride waters south and east of Ridgecrest to Icome from a former lake or lakes in the area. An alternative explanation, geothermalleakage, is discussed in the Summary. I

Kunkel and Chase presented conclusions on the water budget of the valley based onboth data and extensive assumptions.

Caleulating a Water Budget. Conclusions on any water budget will vary Idepending on the quality of the data and the assumptions made. Calculating a water budgetis beyond thie scope of this paper. Some data possibly affecting assumptions are containedin the conclusions section of this report. A 1988 critical review given by Dr. C. F. Austin, mNWC Geothermal Program Office, of the various water budgets published for the Valleywas published verbatim by the News Review of Ridgecrest, California.*

USGS Reports. The USGS has published several open-file reports in cooperationwith NWC to update observations on water levels and to furnish water analyses for 1 yearor a few years. Among these reports ?re Koehler (1971), Banta (1972 and 1974), Lamband Downing (1978), and Berenbrock (1987).

Other Documents. The Geothermal Program Office, Public Works Department,NWC, maintains a Coso library open to the public. In addition, the California Energy ICompany, Inc., the geothermal developer at Coso, has much proprietary information onthe geothermal reservoir and the hydrology and structural geology of the entire region.

In the Coso Geothermal Field the principal geothermal brines are of the sodium-chloride type, and the recharge area is the Sierra (Fournier and Thompson, 1980). Someadditional significant references are Austin and Pringle (1970), Moyle (1977), and Spane(1978).

* Copies are available from the NWC Geothermal Program Office uponrequest.

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In 1975, Warner, in a USGS report, stated that the dissolved solids content in someareas was increasing slightly, however, where this had occurred it was not yet serious.

In 1971 Bloyd and Robson published a paper entitled "Mathematical Ground-WaterModel of Indian Wells Valley, California." Austin (1987) wrote a critical review of the3 concepts in this paper.

In 1973, Dutch r and Moyle published the water-supply paper "Geologic andHydrologic Features of Indian Wells Valley, California."

In 1984, Dr. Pierre St. Amand proposed that the Indian Wells Valley grcandwatersystem is a closed basin, and he prepared a water budget for the basin on that assumption.*

I GEOLOGY

The Sierra Nevada mountains to the west of India i Wells Valley consist of graniticrocks with roof pendants of metamorphic rocks. Some contact metamorphic rocks alsooccur (such as the Tungsten Peak Mine). The Coso Range to the north is complex; Sierranbasement rocks have been penetrated by both basaltic (dark colored, low silica) andrhyolitic (light colored, high silica) volcanic rocks of Tertiary to recent age. An excellentsurface map of the Coso Volcanic Field is that of Duffield and Bacon (1981). The ArgusRange locally to the east and the Spangler Hills to the southeast are also predominantlySierran basement type rocks. The El Paso Mountains to the southwest are also Sierran butcontain Eocene (Tertiary) basalt and both continental and marine sediments, andconsiderable Paleozoic marine sediments. The USGS authors from the variousgroundwater offices that have reported on the Indian Wells Valley in the past 2 decadeshave all considered the bedrock to be impermeable and largely non-water bearing. Thepermeability of plutonic and volcanic rocks is discussed in the Summary.

The Valley itself is traditionally considered to consist of alluvium, lacustriiie (lake)deposits, windblown sands, playa silts and clays, and probably a thick section of estuarineand marine sediments at de-ith. However, careful field work on the east fice of the Siereashows that much of the composition should be glacial tills and glacial outwash debris(Austin, 1988). The alluvium on the west side of the valley in parvicular occurs as alluvialfans and glacial outwash debris coming into the vi ley from mountain canyons and valleyfill. Kunkel and Chase (1969) divide the valley alluvium into "older" and "younger" units5 and give them formation names. The lake deposits are Pleistocene (Ice Age) and areinterbedded within the alluvium. Kunkel and Chase proposed a simple stratigraphy withthe older and younger alluvium deposits separated by the older lake deposits (young lakedeposits are represented by the pinnacles in Searles Valley). The Tertiary and Pleistocenewas a complex age. Austin (1988) suggests that the pluvial periods documented by Norrisand Webb (1976) have all affected the Indian Wells Valley.* Austin lists the followingglacial events, presented here as Table 1.

3 January 1984 draft copy of NWC TP 6404, "The Water Supply of IndianWells Valley, California," published in 1986.5* Dr. C. F. Austin, personal rommunication with Dr. J. A. Whelan, 198

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TABLE 1. Glacial Periods.(From Norris and Webb, 1976). 1

Name of period Years before present

Mauthes 0-650 IUnnamed 1,000Recess Peak 2,000-6,000Unnamed 6,000-7,000Hilgar . 11,000Tioga 20,000 3Tenaya 26,000Tahoe 50,000

Mono Basin 87,000Donner Lake 250,000

Casa Diablo 400,000 1Sherwin 750,000McGee 1,500,000Deadman Pass 3,000,000

In 1984 the geology was determined of a well drilled by the Navy just inside the NWCboundary by the Inyokem substation (Whelan, unpublished report, 1984). Tree rootlets Iwere encountered at 400 feet. At greater depths in this 1,000-foot well were two zoneswhere the alluvium was cemented with caliche. Whelan assumed these to be "splash"zones formed at a shoreline. If his interpretation is correct, separate lakes were present Ithere twice, or one lake was transgressing and regressing. In either case, the valley fill ishighly complex as well as folded.* Scattered local confined zones may exist but there is noevidence that the basin as a whole has any recognizable division into broad horizontallayers of different kinds of waters.

Works of the USGS considered Indian Wells Valley to be a simple down-faulted blockbounded by high-angle faults. Zbur (1963), on the basis of seismic refraction, gravity, andaeromagnetic studies, postulated a maximum of 6,200 feet of valley fill. However, he alsoassumed the valley was bounded by high-angle faults. Austin and Moore (1987) presentedconvincing evidence that the Coso Range was formed by low-angle thrust faulting. More Iand more evidence is surfacing that the Sierra and Argus Ranges are both stacked thrustsheets complicated by major listric faulting." Certainly thrusting is important throughoutthe Basin and Range geologic province and also into the Colorado Plateau.

If, as now seems probable, thrust faulting has been important in local geologic history,then the basement under the valley fill in Indian Wells Valley could well be sedimentaryrocks.*** This possibility has significant implications as to both regional groundwater

* Dr. C. F. Austin, Ward Austin, and D. O'Brien, personal communication with IDr. J. A. Whelan, 1988.

R. Erskine, personal communication with Dr. J. A. Whelan, 1988.D. O'Brien, personal communication with Dr. C. F. Austin, 1988. II

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II NWC TP 7019, Volume I

hydrology and the complex pattern of groundwater flow system cells in the valley. See thesection Determination of Groundwater Flow System Cells for more information.

The basic geologic map of the area is the Trona Sheet, Geologic Map of California(Jenkins, 1962). Nilsen and Chapman (1971) prepared the Bouguer gravity map ofCalifornia, Trona Sheet. Jenkins and Nilsen and Chapman did not recognize the thrustfaulting in the Coso Range or Sierra (Austin and Moore, 1987).

THEORY BEHIND GEOCHEMICAL INVESTIGATIONS

The quality of natural water is determined by the concentrations and types of dissolvedmaterial contained within the water. The dissolved material in the water may have beenderived from the atmosphere, biological sources, soils, or minerals, or through human-induced activities. Bacteria, evaporation, mixing, and chemical reactions may further alterthe water as it passes through the hydrologic cycle. In the Indian Wells Valley, widespreadgeothermal activity is a major contributor to the groundwater chemistry.

To determine the chemical quality of water, an analysis must be performed on thesample. This analysis involves both the careful measurement of certain parameters of thewater sample as it is taken from its natural environment and the proper preparation of thesample for later analysis so that the concentrations of the dissolved ions do not change.

ION-SITE MEASUREMENTS: TEMPERATURE, pH, ANDCONDUCTIVITY

On-site measurements at the sampling source include temperature, pH, andconductivity. These three parameters can change rapidly with time and must be measuredas soon as the sample is taken.ITemperature

Temperature readings of groundwater are an important source of information. Manyfactors concerning the measurement and actual ionic composition of water quality areinfluenced by temperature, including pH, conductivity, and the concentration of dissolvedions. Temperature readings must be included in corrections for pH and conductivitybecause both are based on a certain property of the water at a specific temperature.

Temperature readings are also important in the Indian Wells Valley because of theknown presence of geothermal features in close proximity to or within the valley.Geothermal features may contribute heat or heated water to the local groundwater systemand cause major changes in the chemistry of the water. If an abnormally high temperaturewere measured at a sampling location, that would indicate that the groundwater reservoirwas connected in some way with a higher-than-normal heat-flow area. For example, waterfrom a Navy well at the Inyokern substation is 27*C. Thus, a geothermal area may becontributing heat to the local reservoir, or geothermally altered waters may be mixing withthe more typical groundwaters. An analysis of certain constituents that are found ingeothermal waters compared with analyses of neighboring non-geothermal waters is

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sometimes a fairly reliable method of determining if an intermixing of waters is occurring inthe area. This method will be discussed in the Water Types section of this report. £Measuring pH

The measure of pH in a sample must also be taken immediately after the water isremoved from its natural environment. Reported in the base 10 log of the hydrogen ionactivity (in moles per liter), pH gives an indication of the type and amount of reactions thewater was undergoing at the time of sampling.

The pH values change as hydrogen ions are produced or consumed during chemicalreactions in the groundwater system. Values of pH are commonly lumped into three major Idivisions: basic (pH > 7.0), neutral (pH = 7.0) or acidic (pH < 7.0). A water containingequal amounts of hydrogen ion and hydroxide ion (H+ = OH-) at 250 C has a pH of 7.00.If hydrogen ions are added to this water, the solution becomes more acidic and the pH Ivalue decreases. Conversely, if the hydrogen ions are consumed in a reaction, the solutionwill become more basic and the pH value will increase.

Most natural waters have a pH ranging from about 6.0 to about 8.5 (Hem, 1985, p.64). The range of pH in Indian Wells Valley was from 4.60 (26S/40E- 14N 1, 06-21-72) to10.10 (25S/40E-33L1, 03-25-75). 1Conductivity

Conductivity is a measure of the ability of a substance to conduct electricity. In water-resource investigations, specific conductance is measured and is defined as the ability of asolution to conduct electricity at a specified temperature and through a unit length and crosssection. The standard temperature at which specific conductance is measured is 25°C; the Iunit lepgth and cross section are 1 centimeter and 1 square centimeter. Specificconductance ca-i be plotted against measured or calculated total dissolved solids (TDS) anda relationship equating specific conductance to TDS can be established (curves are given in IAppendix B).

ANALYSES OF ELEMENTS AND COMPOUNDS IAnalyses can be obtairied for all elements and compounds. A complete analysis of all

the possible constituents is not necessary for geochemical investigations. Contributions of Imany of the elements found in natural waters are small and do not affect the overall qualityof the water. Analyzing for a large number of ions can become cost prohibitive.

The major positive ions (cations) that were chosen for the study of water quality inIndian Wells Valley and that most affect the quality of water were calcium (Ca++), sodium(Na+), magnesium (Mg++), and potassium (K+). These cations were chosen because theyare the most common positive ions contributing to the water quality of the area.

The major negative ions (anions) chosen for water-quality study were chloride (Cl-),sulfur in the form of sulfate (SO4-), bicarbonate and carbonate (HCO3" + CO3--), andfluoride (F-). These anions were chosen because they are major contributors to waterquality in the valley. 3

12 g


Other elements were included in the analyses because of their effect on humans,livestock, and plants, or because they are geothermal indicators. These elements are silica(SiO 2), boron (B), iron (Fe), and arsenic (As).

Calcium. Calcium is the major cation of the alpine waters. Calcium causes water to be"hard." The low TDS contents keeps the alpine waters "soft." In the evolution of desertwaters there is a tendency for waters to change to more sodium-rich waters.

Sodium. Sodium is a very soluble cation. As waters react to the desert environmentIthey tend to become enriched in sodium.

Potassium. Potassium is associated with sodium and behaves in a similar manner.3Low sodium-to-potassium ratios may indicate a possible geothermal water.

Magnesium. Although magnesium is generally present in greater amounts thanpotassium, it is somewhat anomalous to the groundwaters of Indian Wells Valley. TheIsource of magnesium is probably the basalts in the northwest portion of the Valley.

Bicarbonate and Carbonate. Bicarbonate and carbonate are the principal anionscontributing to the hardness of water. The carbonate-bicarbonate system is very complexchemically, and variables such as carbon dioxide partial pressure, pH, temperature, type ofenclosing rocks, and other ions present affect the system greatly.

3Chloride. Chloride is the least reactive of the anions. Many geothermal brines are ofthe sodium-chloride type.

Sulfate Sulfate is the least common of the major anions. Four sources of sulfates arein Indian Wells Valley groundwaters: (1) the oxidation of pyrite in Tertiary lake clays, (2)the oxidation of sulfides in mineralized areas, (3) sewage pond leakage (sodium sulfate isadded to detergents), and (4) leakage from geothermal steam caps. Another source ofsulfate could be sedimentary gypsum or anhydrite beds; however, neither gypsum noranhydrite has been found in the valley or surrounding mountains.

3 Fluoride. Although Hem (1985, p. 120) places fluoride as a major element, it isactually a trace element. It is usually lumped with chloride as a major element.

Silica. Silica (SiO 2) is important chiefly as an indicator of geothermal leakage. Adiscussion of the silica geothermometer is given by Fournier (1981, pp. 113-18).

iBoron. Extreme concentrations of boron occur in the surface and shallowgroundwaters of China Lake Playa.

Arsenic. Arsenic is of concern because of its toxicity to humans and other animals.Hem (1985, pp. 144-45) gives the Environmental Protection Agency (EPA) standard fordrinking water as 50 micrograms per liter (jtg/L). Many analyses of waters from the IndianWells Valley indicate concentrations of arsenic in excess of 50 milligrams per liter (mg/L).

However, Hem (1985, p. 145, citing McKee and Wolf (1963, p. 140)) notes that waterswith 1,000 gig/L have been used for drinking for short periods of time with no apparentharmful affects but that long term-use of concentrations of 210 gg/L was reported to be5 poisonous.

Berembrock (1987, p. 40) reports a well (25S/40E-33L1) that on two samplings (05-21-80 and 06-09-82) gave arsenic concentrations of 2,000 and 2,900 ptg/L respectively.

113

N-WC TP 7019, Volume 1 3The mean arsenic content of waters in which arsenic was reported was 152 gg/L. The

arsenic concentration frequency distribution is skewed towards high values by a few veryhigh citations, giving a misleadingly high mean. The median or mid value was 15 gg/L.We believe that the median is a more m,=L ngful statiic -"& this case, in that Valleydrinking water that contains arsenic is far closer to the median than the mean.

STUDY TECHNIQUES 3SAMPLING TECHNIQUES/INSTRUMENTATION 3

Sampling techniques were set up to ensure the quality of the on-site measurements andsample preservation. Although the actual sampling routine varied slightly at each site,USGS Water Resources Division procedures were strictly adhered to. 3

Temperature was measured with an alcohol-based thermometer calibrated against aNational Bureau of Standards (NBS)-tested thermometer. The thermometer was rinsedwith de-ionized water before and after each use and was dried with lint-free wipes to Icontrol contamination.

A Beckman 21 pH meter in conjunction with a Beckman pH electrode and a Coming Utemperature probe was used to measure pH. The meter was tested immediately before eachsample was measured with 4.0-, 7.0- and 10.0-pH standards. Two consecutive readingswere taken immediately after the sample was removed from the well or spring, and if thedifference between the two was greater than 0.1 unit, then a third reading was taken to 3resolve the discrepancy. The pH value was recorded on a field sample sheet. Appendix Econtains the field sample reporting sheets for this investigation. g

A Lab-Line Lectro-MHO-Meter Model MC- 1 Mark V conductivity meter in conjunctionwith Lab-Line Instruments, Inc., conductivity cups was used to measure specificconductance. The meter was standardized each morning before use with three standardsbracketing a range from less than 100 microsiemens per centimeter to 2,500 microsiemensper centimeter. The cells were rinsed with de-ionized water a minimum of three timesbefore each use, then rinsed twice with the sample water before being filled for the reading.This procedure ensured that contamination from the previous sample and dilution from the Ide-ionized water was kept at a minimum.

Three 1-liter polyethylene bottles were filled at each sampling location. The bottles Iwere prepared for sampling as follows. One was filled with filtered water, one was filledwith unfiltered water, and one bottle was acidified to preserve certain ions. The non-acidified bottles were rinsed twice with the sample water before filling. Acidified bottleswere rinsed with HN03 at the lab and the water was filtered through a 0.45-micrometernitro-cellulose filter with a Geofilter Peristalic Pump. The unfiltered water was takendirectly from the spring or well head. Each bottle was labeled, sealed, and cooled forshipment to the laboratory for analysis.

14

U3 NWC TP 7019, Volume 1

ANALYSIS TECHNIQUES

Laboratory analysis for the samples collected during this study was conducted by ACZ

Laboratories, Colorado Springs, Colo.

The best measurement of quality of an analysis is to take the difference of the positivecharges on cations and the negative charges on anions, divide that number by the sum ofthe two charges, and multiply by 100, giving a percent error. A satisfactory analysisshould have a percentage error of plus or minus 5%. The positive and the negative chargesare given on the laboratory reporting sheets (Appendix E).

Also, when a report of an analysis is received, the investigator should look for obviousor probable errors, and if any results appear erroneous, contact the laboratory and have theanalysis checked for typographical errors on the reporting sheet, dilution errors, or othersuch possibilities.

5 Table 2 gives the detection limits and analysis techniques for the elements andcompounds used in this report.

3 TABLE 2. Detection Limits (mg/L) and Analysis Techniquesfor the Elements and Compounds Used in This Report.

The abbreviations used are USGS: U.S. Geological Survey; EPA: EnvironmentalProtection Agency; AA: Atomic Absorption; ICP: inductive coupled plasma.

Chemical Analysis technique Detection limit,

Arsenic USGS (1-2-62-78), AA automated-hydride 0.001Bicarbonate a EPA 310.1 titrimetric (chemical) 1Calcium EPA 200.7 ICP (AA) 1Carbonate EPA 310.1 titrimetric IChloride EPA 32.2 automated ferricyanide 1Fluoride EPA 340.3 automated complexone 0.02Iron EPA 200.7 ICP 0.02Magnesium EPA 200.7 ICP 1pH EPA 150.1 meter (units) 1Potassium EPA 200.7 ICP 1Silica EPA 200.7 ICP 0.1Boron EPA 200.7 ICP 0.02Sodium EPA 200.7 ICP 1Solids (dissolved) EPA 160.1 gravimetric 108*C (precipitation and 2

weighingSulfate EPA 375-3 gravimetric 4

a As CaCO3.

1 15I


INTERPRETATION TECHNIQUES

The methods of interpretation for water quality data are many and, as with other types iof data, contain many pitfalls. Care must be taken in the collection, preservation, andanalysis of the water samples along with the interpretation of the analyses.

The analytical methods used to determine the concentration of the major constituents(solute) in each water sample are reported by the laboratory as the weight (in milligrams) ofa given solute per unit volume (liter) of solvent. Minor constituents such as arsenic andboron are reported by the USGS in tg/L and by ACZ Laboratories in mg/L.

Water analyses from other sources may be reported in various other units. Conversionfactors for these unirs can be found in Hem (1985).

Chemical Equivalence Between Cations and Anions ITo compare different ionic species, a conversion involving the weight and electrical

charge of each ion is used. When the formula weight of an ion is divided by the charge ofthat ion, the result is termed the equivalent weight. If this equivalent weight is then divided Iinto a concentration value reported in milligrams per liter, the result becomes milligram-equivalents per liter. For convenience, milligram-equivalents per liter has been shortenedto milliequivaleits per liter (meq/L). Table 3 contains the necessary equivalent weights for Img/L to meq/L conversion.

TABLE 3. Conversion Factors for MilliequivalentConversions (From Hem, 1985).

Element and reported species Multiplication factor

Bicarbonate (HCO 3) 0.01639

Calcium (Ca++ ) 0.04990 1Carbonate (CO- -) 0.03333

Chloride (CI') 0.02821

Fluoride (F -) 0.05264

Magnesium (Mg++) 0.08229

Potassium (K+) 0.02558

Sodium (Na + ) 0.04350

Sulfate (SO 4 "') 0.02082

16


The following is an example of a conversion for milliequivalents. The analysis is ofwater from 27S/39E-2161, in mg/L.

Bicarbonate 122Calcium 41Carbonate 0Chloride 17Fluoride 0.40Magnesium 0.11Potassium 8Sodium 41Sulfate 49

U Calculations:

i Cations, mg/L

Calcium 41 x 0.0499 = 2.05Magnesium 11 x 0.08299 = 0.91Potassium 8 x 0.02558 = 0.20Sodium 41 x 0.04350 = 1.78

3 Total cations 4.91

Anions, mg/L

Bicarbonate 122 x 0.01639 = 2.00Carbonate 0 x 0.03333 =0.00Chloride 17 x 0.02821 = 0.48Fluoride 0.4 x 0.05264 = 0.02Sulfate 49 x 0.02082 = 1.02

I Total anions 3.52

Percent error = ((4.91 - 3.52)(4.91 + 3.52)) x 100 = 16.29%

The use of milliequivalents per liter denotes that the unit concentration of all ions arechemically equivalent, i.e., that for each unit of positive ion (cation) there is one unit ofnegative ion (anion). In a stable environment, the balance of cations and anions should3 equal zero.

This chemical equivalence between cations and anions provides a quick yet reliablemethod of evaluating the quality of both the sampling technique and the laboratory analysis.If one assumes that the environment the sample was taken from was in equilibrium, then acomparison of the computed milliequivalents per liter for the major cations (Na, K, Ca, andMg) versus the major anions (Cl, S04, F, C03, and HCO3) will enable a balance to be5made, and if no balance exists, to show the degree of error present.

Hem (1985) states that "Under optimum conditions, the analytical results for majorconstituents of water have an accuracy of plus or minus 2 to plus or minus 10%."Balances have been computed for all of the analyses used in this report.

£ 17I

UNWC TP 7019, Volume 1 3

Stiff Diagrams

Graphical representation of milliequivalents per liter allows the user a visual means ofIcomparing gross water composition without the need for tables of data.

A modified "pattern" diagram, similar to the one described by Stiff (1951) was chosen 3to aid in the classification and analysis of water types in Indian Wells Valley. This pattem,commonly called a modified Stiff diagram, reduces the effects of dilution or concentrationon the shape of the pattern and facilitates the interpretation of sample analyses. I

The modified Stiff diagrams are based on a meq/L comparison of the major cations andanions of a given sample. The cation and anion equivalents are plotted to the left and to theright of a vertical axis, respectively. The horizontal scale is in meq/L, and similar species Isuch as sodium and potassium are grouped and labeled as such (Na + K, C1 + F, HCO3 +

C03). Graphically displayed comparisons of the chemical constituents dissolved in naturalwaters are an easy way to compare the gross chemical composition of waters.

After the points have been plotted on the graph, they are then joined together by straightlines forming a closed diagram. This closed pattern is the modified Stiff diagram.Modified Stiff diagrams can be calculated by hand or be computer derived. The diagrams Iin this report were computer derived. One of the main values of Stiff and modified Stiffdiagrams is they are visually recognizable "fingerprints" for major groundwater types. 3

As the composition of the dissolved constituents contained in a water sample changeover time, the shape of the modified Stiff diagram will change. Plotting the diagrams on amap in their respective sampling positions will show spatial variability in the gross water Icomposition, while a temporal comparison will show changes in composition over time.

IGROSS WATER CLASSIFICATION BY MAJOR IONS

Another method of classifying water is by gross composition. This method also usesthe meq/L values but compares the percentage of the major cations and anions and classifiesthe water based on the percentages of each constituent. If a certain cation or anion makesup over 20% of the total cations or anions, that ion is included in the naming of a water.The cation with the largest percentage of the total cations is named first in the water type,then the cation with the second largest percentage, with the naming continuing until thepercentage of the remaining largest cation drops below 20%. The anions are next, with thelargest percentage leading. The anions also continue to be named in lesser percentages untilthe percentage of the remaining largest anion also drops below 20%. This listing of cationsby lessening percentage followed by anions by lessening percentage makes up the water- Utype name. For example, a water could be of a sodium-chloride (Na-Cl) type, a sodium-calcium-chloride (Na-Ca-Cl) type, or a sodium-calcium-magnesium-chloride-bicarbonate-sulfate (Na-Ca-Mg-Cl-HCO3-S04) type. 3

1I

18 B

ISI NWC TP 7019, Volume 1

CONDUCTIVITY VERSUS TOTAL DISSOLVED SOLIDS

Estimates of TDS (mg/L) in a water sample can be obtained by using specificconductance, eliminating the need to send the sample to a laboratory. Specific conductancemeasures the ability of the sample to conduct electricity at a specific temperature andthrough a unit distance. Plotting calculated TDS against specific conductance allows theestablishment of a curve relating one variable to the other. If specific conductance for aparticular water type is measured and compared against an established relational graph ofspecific conductance versus TDS, then the TDS content for the sample can be estimated.

An attempt was made to correlate specific conductance with TDS using water analysesfrom the USGS records and those samples collected specifically for this study. Many ofthe USGS analyses did not include both TDS and specific conductance. Both of theseparameters are necessary to construct the relational curve mentioned above. Because sofew analyses were complete, graphs for all water types and areas were not reliable.However, relationships for TDS versus conductivity for specific water types werecalculated.

Using a computed TDS (sum of major components measured in mg/L) andconductivity, a linear regression line was fitted to the data. A correlation coefficient "R"was computed for the line. If R = -1.00 or +1.00, there is a perfect correlation between theindependent and dependent variables. If R = 0, there is no correlation. Using the datafrom all analyses, R = 0.30, which is unsatisfactory. We decided to attempt correlationagain using the computer-derived water types. Curve fitting was attempted only if therewere three or more samples of a water type (two samples always give a straight line withperfect correlation). In general, linear regression lines fit well. The resulting curves ofcomputed TDS versus conductivity are shown in Appendix B. By determining the watertype (by the method described in the next section) and by taking the conductivity of aIsample, you can determine the TDS using the appropriate curve.

I DETERMINATION OF GROUNDWATERFLOW SYSTEM CELLS

Figure 3 is a plot of areas where various types of groundwater are found, areasdescribed as groundwater flow system cells. This map was prepared from three sets of3 data, all maps.

In the first map, waters that gave similar modified Stiff diagrams were plotted, andareas where a given water type dominated were outlined on a map of the Indian WellsValley (Naval Weapons Center map, 1982).

In the second map, computer-generated water types were plotted using color codes foreach ion in the classification. In general, this map and the first map were in goodagreement.

A Utah State computer agency made contour maps of the analyses for sulfate, boron,pH, and TDS. In general these maps confirmed the assignment of areas made on the basisof the above methods.

I19

NWOTP 7019, Volume 1 3I

T 20 s ,

__ IT 21 S I

T 22 S

T 23S SSEE DETAIL 1 w

z

T 24 S <

SESEE DETAIL 3

SEE DETAIL2 3I IT 26 S

T 27S

R37E R38E R39E R40E R41E R42E R43E

a. Overall map. 3FIGURE 3. Water Types at the Naval Weapons Center and in theIndian Wells Valley. 3

20

I

3 NWC TP 7019, Volume I

6 - 46

7 8 9 10 11 12ALPINE

16 15 14 13

z

COOJUNCTIONSDU

ALPIN2~__CHLORIDE

I NCOSO HOT.SPRINGS

3 _3

6 5 4 LITTLE LAKE TYPE WVATERS __b

9 SOMEWHAT VARIABLE7 8 SODIUM-CALCIUM-MAGNESIUMI BICARBONATE -SULFATE -CH LOR IDE

3T 23 -

3~~3 FIUR 3.(C3i

15171I51


SODIUMBICARBONATE

S OIUM BICARBON ATE \3\ 2\\ \5 /4 3 *21

T 2 5S -19W 'C2 0 21 19 20, 21' 2 3 24

26 25 30 2930 9 8 2/ 5

36\ C 36 z 31 32 33 '34 35 36'

7 B 10 1 ~I2 7 12 7 9 "io SODIUMIU

CALCIUIUM

T26S SODIM 23 24 1 20 1 22 23 2. 19 20 1S22 23 U2

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126 2~ 30 12 928 27 26 2 302 22 26 25

3 36, 1 32 3113 /

6 A 1 54U

T ~10 1 12 1778 SDU

SODIUM CARBONATE 36\ 14I---BCALRBONE1

T 27S-- SODIUM .4 -SULFATE

201 22 23 BICARBONATE

7 .~ SULFA E K8, 27

R 37 E R 38E R39

.Detail 2.1

FIGUR 3. (Contd.)5

221

II NWC TP 7019, Volume I

T 24 3

ac0; U

, ~z -

c/I T 25 S

n _j

SODIUMCHLORIDE'II ,~soDUMI 7 8

SCHLORIDE----

-7 2 7 S

T26 19__ _ _ _ 20_ 21_ 22_23 _2

30 29 28 2 26 25 - --

R40E R41 E R42E R43E

d. Detail 3.

3 FIGURE 3. (Contd.)

i 23I


We wanted to determine what kind of rocks the various types of water had been incontact with. Doing so would allow us to identify "bedrock" inflows. Dr. T. Cerling,Assistant Professor of Geology, University of Utah, noted that one of his students in 1985 Ihad considerable success relating the rocks of a drainage basin to water chemistry using a

trilinear plot of silica, alkalinity, and sulfate plus chloride.* The scheme was developed byStallard and Edmond (1983). To use it, one computes the milliequivalent of the silicon, Ialkalinity (bicarbonate plus carbonate), and chloride plus sulfate, and sums them. Theindividual milliequivalents and the sum are used to compute percentages for their plotting.

Stallard and Edmond's study was of the Amazon Basin. We were doubtful that the Ischeme would work in the Mojave Desert because of the great difference in climaticconditions, which affects rock weathering. Also, the scheme was developed for surfacewaters, not groundwater. Pederson's study was in the bighorn basin of Wyoming. Allanalyses with the appropriate components analyzed were calculated and plotted (Figure 4).As one would expect, most sample sites were in a plutonic and volcanic area because of theproximity of the Sierra and Coso volcanics. Some sites were plotted in the limestone area, ashale area, evaporate (playa) area, and geothermal area. The geothermal area was added tothe plot by Whelan (Figure 4). Trends of water types as determined by the scheme wereplotted on another copy of the referenced map. The trends were in general agreement withthe trends of water types as determined by the other methods.

Unfortunately, the fact that some waters appear to have a limestone affinity and othershave a shale affinity does not prove or disprove the presence of Paleozoic metasediments in Ithe basement. The Indian Wells Valley has been occupied by Holocene and Pleistocenelakes, which affects the results significantly. Stallard and Edmond (1983) also proposed atrilinear plot of milliequivalent of alkalinity, calcium plus magnesium, and sulfaterecalculated to 100% to relate water compositions to the sedimentary rock environment. All Iapplicable water analyses were plotted on this diagram (Figure 5). It appears that thisdiagram, developed for surface waters in the tropics, is not applicable to the groundwaterenvironment of the desert in Indian Wells Valley as the majority of the points show a Isedimentary relationship (Figure 4). Because much of the alluvium is composed of SierranRocks, which are granitic with lesser metamorphic rocks, one would expect the waters tohave exhibited an igneous association.

Figure 3 is considered the most important product of this investigation. However, onemust be cautioned on its use because of certain limitations. Dashed lines are used toseparate water types. They are dashed because in general the boundaries are very Iapproximate, this because of the lack of sufficient data points in large areas. When wells ofmoderate depth produce reasonable amounts of water, of good quality, many wells aredrilled. Where the aquifer is very deep, the yield poor, or the quality poor, few wells are Udrilled and control for plotting deteriorates.

Another factor is depth control. Of 375 wells sampled through the years by the USGS, 3total depths are available for only 150, or 42%. Of the sites sampled specifically for thisstudy, depths were available for 7 of 12 wells, or only 58%. Only rarely were depths ofthe aquifer available. Very few deep wells are in this Valley. In the China Lake Playa, forinstance, only very shallow wells were available for sampling; therefore, any freshwaterunderflows were ignored.

Pederson, B. L. 1985. Geochemical Studies in the Bighorn Basin, Wyoming.Unpublished Master's Thesis, University of Utah, pp. 37-45.

24 !


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26


Figure 3 contains some personal interpretation. For instance, sodium-calcium-chlorideand calcium-sodium-chloride waters were lumped together in areas of mixing. If one wellhad a different water type than most others in an area or was much different in depthcompared to the others, it was not used.

We acknowledge that Figure 3 is a preliminary map but believe that it will be useful insubsequent investigations. We expect that future workers will improve upon it.

N THRUSTING AND LISTRIC FAULTING COULDPROVIDE MAJOR WATER COLLECTORS

The growing realization of probable thrusting with associated listric faulting in LheSierra, the Coso Range, and the Argus Range has many implications on in-erpretation ofthe groundwater geochemistry. The hanging wall of a thrust sheet would probably be anaquitard-a barrier to groundwater flow. The footwall is probably badly sheared. Thecrushed footwall of a thrust in the Oquirrh Mountains or Utah is known to the operatinggeologists of the Bingham Canyon Copper Mine as the "chaotic area." Thus the footwall ofa thrust could well be a major aquifer. while listric faults and dish-shaped thrusts couldserve as major water collectors in the hanging wall system (Silver, 1986). Fracturepermeability can be very high. As examples, in driving the San Jacinto tunnel in granites,flows of up to 16,200 gpm occurred when major faults were crossed (Procter, White, andTerzoghi, 1946), and a geothermal well (54-3) in the Roosevelt Geothermal Field nearMilford, Utah, producing from the dome fault zone with a diameter of just over 9 inches,had an initial mass flow of 1,500,000 pounds of steam and water per hour (approximately3,000 gpm).* Thus water could be entering the Indian Wells Valley from beneath thrustplates of the Sierra.

Another aspect of possible thrusting in this region is that the lower plates are believed tobe sediments.** Also, the basement under Indian Wells Valley could be sediments.Mifflin (1968) shows that there are large interbasin flows of groundwater under mountainranges in Nevada. The Naval Weapons Center Rocketeer (18 March 1988) noted thatsprings at the Onyx Mine in the Panamint Valley can produce 60,000 gallons of water perday or 70 acre-feet per year. These springs may be an example of interbasin underflowbeneath the ranges. It is highly probable that there is interbasin leakage from Indian WellsValley through the Poison Canyon area and under the Argus Range as a whole into SearlesValley, and south through the Paleozoics of the El Paso Mountains into Freemont Valley.

II

R __po c u an t r AW a 1R. Lenzir, personal communication with Dr. . A. Whelan, 1976.

2 M. Erskine, personal communication with Dr. J. A. Whelan, 1988.27

I

INWC TP 7019, Volume I 3

WATER TYPES IWATER TYPES DEFINED BY THIS STUDY

Alpine Waters 3The least-modified water in the region would be meteoric water derived from the

granitic terrain of the Sierra. These waters are of the calcium-magnesium-sodium-bicarbonate-sulfate-chloride type (Figure 6). These waters are normally of low TDS. Asthese waters work theiz wa, to the Valley they are modified by evapotranspiration,reactions with soils and rocks, and mixing with other waters. 3

U

Na+K CI+F II

Mg S04

Ca HC03+C03 !

5 -5

FIGURE 6. Grumpy Bear Well in 22S/36E-21. ISodium-Chloride Waters I

Two sources of sodium-chloride brines are in the Indian Wells Valley region:geothermal brines and playa brines.

The analyses of a typical geothermal brine (Coso Geothermal Exploration Hole(CGEH)-1, Coso Geothermal Field) given by Fournier and Thompson (1980) togetherwith an analysis of a sodium-chloride playa brine are given in Table 4. Salt Wells andSearles Lake waters are also of this type. A modified Stiff diagram is shown in Figure 7.

IU

28 I


TABLE 4. Analyses of Sodium-Chloride Type Brines.

IItem CGEH-I, sampled at China Lake, 253140Eapproximately 360 ft 25HI (USGS data)

Temperature 1950C ...pH 5.40 7.3

SiO 2 119 ...

Ca 55 26

Mg 1 71

N 1,510 26,000

K 132 320

Li 13 ...

HCO3 119 570

SO 4 53 130

CI 2,330 40,000

F 3.3 ...

B 49 912

Calculated TDS 4,384.43 ...

TDS measured ... 66,400I

3Na+K i C+

I Mg S04

Ca HC03+C03

*II3 480 -480

FIGURE 7. Sodium-Chloride Waters.

1 29I


Sodium-Carbonate and Sodium-Bicarbonate Waters

The location of these waters is shown in Figure 3. Most are sodium-bicarbonate Iwaters. Of special interest are waters from 27S/37E-31B and 26S/35E-35L. These aresodium-carbonate waters with low TDS. A similar water is present in the 103-foot well bythe old house at the south end of the Coso Hot Springs area. This is not to imply that thereis any communication between these areas, but to note that there may be an inflow ofgeothermal waters into the southwest corner of the Indian Wells Valley. It is ourexperience that sodium-carbonate and sodium-bicarbonate geothermal waters generallyindicate low-temperature systems. A modified Stiff diagram of these waters is shown inFigure 8. ISulfate Waters

There are several occurrences of sulfate waters in the area. One is Walker Well, a 3calcium-sulfate-bicarbonate type water. A sulfide-type mineralization exists near WalkerWell.

Waters from the Tungsten Peak Mine (Figure 9) and a shallow well at 38E/26S-15Q are Iof the calcium-sodium-sulfate type. It is believed that the sulfate is from sulfides found incontact metamorphic mineralization (minerals formed where an igneous rock has intruded asedimentary rock). When the mine was in operation, it made 110 gallons per minute orabout 180 acre feet per year.

II

Na+K CI+F 3

Mg S04

Ca HC03+C03

3 -3 IFIGURE 8. Sodiur-Carbonate and Sodium-Bicarbonatc Waters.

3I

30 I


I

3Na+K C1+F

IMg S04

Ca HC03+C03

* 5

3 FIGURE 9. Tungsten Peak Mine in 26S/38E-1OH, on 9-16-86.

I

I Na+K CI+F

IMg S043

I Ca HC03+C

1 88 -i88

1 FIGURE 10. "Sewage Water," in 26S/40E-22H2, on 6-8-82.

I31

I

U

NWC TP 7019, Volume 1 3A shallow seepage from the sewage ponds is a very peculiar sodium-magnesium-

sulfate water (sodium sulfate has replaced phosphates in detergents (Figure 10)). 3Red Hill/Little Lake/Lumber Mill Waters

A complex but interesting set of waters is called Red Hill/Little Lake/Lumber Millwaters. These waters are found in sampling sites from east of Red Hill in Rose Valley tothe area where Brown Road turns from north to west at the site of the former village ofBrown in Indian Wells Valley. The waters are of somewhat varying types. Theexpleration hole at Red Hill was of the sodium-calcium-bicarbonate type. Well 22S/38E-8C is of the sodium-calcium-magresium-bicarbonate type; Little Lake Spring is a calcium-bicarbonate-chloride type. The Lumber Mill site is of the sodium-bicarbonate-chloride- Isulfate type, and a well in 39E/25S-1 IP is a sodium-bicarbonate-chloride-sulfate water.However, the modified Stiff diagrams indicate that the waters are of all of one family. Thevarious cations and anions (except bicarbonate, which dominates the anions) hover around I20% of the milliequivalents, so they drop in and out of the computer classification. Amodified Stiff diagram of the Little Lake Spring is shown as Figure 11.

Mixing models did not work well on Little Lake/Lumber Mill site waters. We believe Ithat the calcium and bicarbonate ions are a contribution from alpine waters. The sodium isprobably geothermal, and that the magnesium is probably leached from the basalts. Webelieve very strongly that the chloride represents a Coso geothermal component. The Isulfate is more difficult to evaluate. Its source could be geothermal (Coso) or deep RoseValley waters. Isotope data confirm the presence of a geothermal component in thenorthwestern Indian Wells Valley.

GROUNDWATERS OF THE INYOKERN INTERMEDIATEAND RIDGECREST WELL FIELDS

The groundwaters of the Inyokern intermediate and Ridgecrest well fields are complexwaters. ElectricakV, sodium is usually the dominant cation, although calcium occasionally Iis. Magnesium contents are low. Bicarbonate is almost always the dominant anion.Chloride is usually the next dominant anion. Sulfate may or may not be present in amountslarge enough to appear in the computer classification. 3

Only order of magnitude results can be determined by mixing models because ofreactions of groundwaters with enclosing rocks (solution of mineral, deposition ofminerals, ion exchange), transpiration (loss of water from plants), evaporation, and mixingof two or more waters with or without chemical reactions. In using mixing modelschloride is often weighted heavily because it is the ion least reactive to surrounding rocks.It appears that the waters of the Inyokern well field could result from the concentration of Ualpine waters by evaporation and transpiration and mixing with a few percent geothermalbrines. The intermediate field would have less geothermal leakage or other sodium-chloride water leakage. To create the waters of the Ridgecrest field would require a largergeothermal component than to create the usual waters of the intermediate field, but a smallergeothermal component than to create the waters of the Inyokern field.

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NWC TP 7019, Volume I

Na+K C2+F

M Mg S04

Ca HC03+C03

I ~~11 1 1I1I I jT r l-r TT-1- 1 -- r-

* 13 -13

FIGURE 11. Little Lake Spring, in 23S/28E-17, on 9-18-86.

1 WATER TYPES ACCORDING TO TOWNSHIP

Refer to Figure 3 for location of the townships discussed here.

Township 22 South, Range 37 East (T22S/R37E). Chemical analyses ofgroundwater samples from wells and springs in T22S/R37E along the Sierra front and atCoso Junction reveal those waters to be similar to groundwater typically found on the crestof the Sierra Nevada, located west of Indian Wells Valley. T22S/R37E includes thesouthern part of Rose Valley and a portion of the east slope of the Sierra range. All of theanalyses used from this section came from within Rose Valley itself. This area wasincluded in the study because of its close proximity to Indian Wells Valley and previousstudies that suggest water movement from Rose Valley into Indian Wells Valley throughthe Little Lake area. The shallow waters found in Rose Valley are typically a calcium-sodium-magnesium-bicarbonate type based on the 20% water classification scheme and area result of direct recharge from the Sierra to the west.

3 Waters from the Rose Valley Ranch house well and irrigation well to the north of CosoJunction are of the calcium-sodium-sulfate-bicarbonate-chloride type. The house well is675 feet deep and the irrigation well 724 feet deep. The irrigation well is capable ofproducing 2,000 gpm without measurable drawdown.*

Township 22 South, Range 38 East (T22S/R38E). Only one water samplewas obtained from T22S/R38E. This sample was taken from an exploration drill hole justeast of Red Hill (22S/38E-30K1) and is very similar to water from the Little Lake samplingsites. The TDS content of the water from this well was 875 mg/L, and the water was asodium-calcium-bicarbonate type. The water taken from the Red Hill site had a high silicacontent (82 mg/L) implying some connection with geothermal activity.

5 * Phil Hennis, personal communication with Dr. J. A. Whelan, 1979.

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Township 22 South, Range 39 East (T22S/R39E). T22S/R39E includes theCoso Geothermal Field in the northwest and part of the Coso Range to the southeast, andcontains a wide range of water types. The array of differences between the waters can be Iattributed to geothermal activity, various drilling depths, and structural differencesthroughout the area. The principal geothermal brine is of the sodium-chloride type withabout 5,000 mg/L TDS. This area is located to the immediate north of Indian Wells Valley Iand may be affecting the quality of water in Indian Wells Valley itself via both Coso Valleyand Coso Basin. There is some evidence that geothermal waters are entering Indian WellsValley in the area around Little Lake and the basalt flows. Two observation holes havebeen drilled in Section 10 (22S/39E-1OD1 and 1OC1). The waters encountered in theseholes are mixtures of sodium-chloride type geothermal brines and valley underflow, whichis similar to the alpine waters of Haiwee spring at the head of the valley to the north(21S/39E-10P). The westernmost well water is about 90% geothermal leakage and 10% Ivalley underftow, the well to the east is 60% geothermal water and 40% underflow. Theholes are a quarter of a mile apart. The amounts were calculated by a chloride mixingmodel and checked with mixing models of the other major ions.

Township 23 South, Range 38 East (T23S/R38E). The water samples thatwere collected from T23S/R38E-8C, Little Lake Spring, and the well at the site of thelumber mill (now removed) include the well in 8C, which is 150 feet deep. All arecomplex multi-cation and anion waters that we have designated the Red Hill/LittleLake/Lumber Mill multi-cation type.

The northwest comer of Indian Wells Valley lies in T23S/R38E and includes the areasboth north and south of the Little Lake surface-water divide. Groundwaters north andsouth of the divide are very similar in composition with only a slight increase in TDS to thesouth. Pumping records from the lumber mill at the bottom of Nine Mile Canyon showvirtually no drawdown over the past years even though over 1,000 acre feet of water havebeen removed from the area annually. The recharge rate to the area affected by thepumping must logically be equal to the amount of water being removed from the aquifer by Uthat pumping. Water from the area of the lumber mill is high in TDS and appears to beaffected by contributions from geothermal waters. Water to the west of the lumber millsite, towards the alpine waters, quality can be expected to improve as one leaves the lowervalley fill and moves up gradient towards the mountains.

Township 23 South, Range 39 East (T23S/R39E). T23S/R39E lies towardsthe center of NWC and includes Airport Lake and, in its southwest corner, part of thebasalt flows. No water samples have been analyzed from this area. However, because thistownship lies directly south of the Coso Geothermal Field there is a strong possibility thatany groundwater found in this area will contain a significant geothermal component.

Township 23 South, Range 40 East (T23S/R40E). T23S/R40E lies east-northeast of Airport Lake and down gradient from Mountain Springs Canyon andRenegade Canyon. This township is also located within the NWC boundary. No wateranalyses fom the township have been performed.

Township 23 South, Range 41 East (T23S/R41E). The Mountain Springs ICanyon area in the Argus Range lies within T23S/R41E and is located to the northeast ofIndian Wells Valley. This township includes Mountain Springs Canyon waters, several ofwhich have been analyzed. The water of the spring itself is of the calcium-sodium- Imagnesium-bicarbonate-chloride type. Water from the Wild Rose Mine is of the calcium-sodium-magnesium-bicarbonate type.

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INWC TP 7019, Volume 1

Township 24 South, Range 38 East (T24S/R38E). T24S/R38E lies directlysouth of the township containing the Little Lake divide and rests along the Sierra on thewestern side of Indian Wells Valley. In the northeast and eastern sections of the township,the waters are of the Red Hill/Little Lake/Lumber Mill area type. In the southwest corner ofthe township the water quality is similar to an alpine type water.

I Township 24 South, Range 39 East (T24S/R39E). T24S/R39E is locatednorthwest of China Lake Playa and south of the Coso Geothermal Field and includes thesoutheast section of the basalt flow and a portion of the White Hills. The chemicalcomposition of the waters in this area are mainly sodium-bicarbonate. Waters from thisarea have a high TDS content. Drilling has been limited in this area because of the qualityof water encountered and the location of the township within the confines of NWC. It ispossible that the water from this township has been affected by inflow from the geothermalarea; however, there is insufficient data to evaluate this idea.

Township 24 South, Range 40 East (T24S/R40E). T24S/R40E includes thesoutheast portion of the White Hills and Paxton Ranch to the southeast. The township liesentirely within the confines of NWC and contains only a few scattered wells. Thetownship seems to be an area of water mixing with many complex types-sodium-chloride-bicarbonate (6A1, White Hills), sodium-magnesium-calcium-chloride (20J1),calcium-sodium-chloride (24E1), and sodium-calcium-magnesium-chloride (36 Ml,Paxton Ranch).

I Township 24 Sojuti-, Range 41 East (T24S/R41E). T24S/R41E includes partof the Argus Range on the east side of Indian Wells Valley. Fournier (1979) sampled aspring in Wilson Canyon (section 13F). The water is of the calcium-magnesium-bicarbonate type.

Township 25 South, Range 38 East (T25S/R38E). T25S/R38E is locatedalong the western edge of Indian Wells Valley and includes the area northwest of Leliter.Water types vary both with depth and location within this township. Water from wells insections 13, 14, 23, and 24 are similar to waters from the Los Angeles aqueduct. Thewaters differ slightly from alpine waters by an increase in magnesium and a decrease incalcium. However, the changes are minor, and positive differentiation of water typebetween alpine and aqueduct waters is very difficult, if not impossible. These alpinewaters probably represent recharge from the Sierra Nevada.

Sand Canyon surface water was sampled from a short stretch of stream in section 7 on21 August 1986. This water was an alpine type water. Because the chemical compositionof water may change drastically upon removal from the ground, this sample was not usedin the overall investigation of water quality in Indian Wells Valley. However, the streamwas reabsorbed into the ground just below the sampling site, thus providing recharge to thegroundwater system in the valley.

A water sample from a deep well in the northeast corner of the township (section 11)has the characteristics of Red Hill/Little Lake/Lumber Mill type water. Although this welllies in the middle of the aforementioned alpine water plume, the deep well probablysamples from a lower aquifer influenced by the higher-density Red Hill/Little Lake/LumberMill type water. This sampling site was the furthest southern extent of the pure Red3 Hill/Little Lake/Lumber Mill type water signature.

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In section 36 of this township, samples were collected from one well at differentdepths. There was an overall increase in TDS and a great increase in sulfate with depth.There are no data from the SW corner of this section.

Township 25 South, Range 39 East (T25S/R39E). T25S/R39E is locatedtowards the center of Indian Wells Valley and lies northeast of Leliter. This township lies Ualmost entirely within the confines of NWC and contains a few scattered wells. Many ofthe wells were sampled in 1946 with no recent samples taken (Bailey, 1946). There seemsto be both Little Lake type waters and alpine waters in this township. Because of limiteddepth data, it is not possible to interpret the groundwater system in this township.

Township 25 South, Range 40 East (T25S/R40E). T25S/R40E lies to thenorth of Armitage Field, includes much of China Lake Playa, and is located entirely within Ithe boundaries of NWC. Depth control for this section is also very poor, yet there appearsto be a specific pattern in the quality of the water within this township. The south andsoutheast edges of the township contain water of a distinctly higher TDS and are of a msodium-chloride or sodium-bicarbonate type. The western part of the section appears to beinfluenced by alpine type waters. Yearly samples from a well in section 20, from 1974-1976 (depth 174 feet), show an alpine type water. Water from section 18 also is stronglyinfluenced by alpine water. Perhaps water is coming from the west and forming a plumeinto this section.

Township 25 South, Range 41 East (T25S/R41E). T25S/R41E includes 3portions of the Argus Range and the southeast section of China Lake Playa. There are fewsamples from this township and all of them are from the China Lake Playa area. This wateris a sodium-chloride type with high TDS and is probably directly related to evaporationnear and in the playa area.

Township 26 South, Range 38 East (T26S/R38E). T26S/R38E lies to thesouthwest of Leliter and contains water samples from a well located in 15Q, the Tungsten IPeak Mine (formerly the Hi-Peak Mine), Indian Wells Canyon, and sites further east in thevalley alluvium. 3

Water from the northern half of the township is primarily a sodium-calcium-sulfatewater. This water type extends all the way across the township and into the next townshipto the east. The water-sample collection from the Tungsten Peak Mine came from the thirdlevel from a pipe driven into the bedrock in that area. The wells to the south and east ofthis area are probably getting some recharge from the bedrock.

A deep well in section 27 (723 feet), which was sampled in 1974, had a TDS content of 3approximately 300 mg/L, a field pH of 6.3, and a sample temperature of 29.5°C. The hightemperature and abnormally low pH indicate that this water may have been affected bygeothermal activity. 3

Another indication of geothermal activity in the area comes from a well in the southeastcorner of the township. This well had a TDS of less than 200 mg/L, a field temperature of27.5*C, and a pH of 9.36. The water is of the sodium-carbonate type. Alpine water lies tothe west in section 33.

Township 26 South, Range 39 East (T26S/R39E). T26S/R39E includes the 3town of Inyokern and the western end of Inyokern Road. Sections 23 and 24 display twodistinct water bodies above and below an indicated break line around 300 to 350 feet.Perhaps this is a separating clay layer. In sections 29 and 30 the water bodies are basically 3

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UNWC TP 7019, Volume 1

all the same. The waters from the shallower wells are calcium-sodium-bicarbonate-sulfate-chloride waters, while waters from the deeper wells are of the sodium-bicarbonate type.

Township 26 South, Range 40 East (T26S/R40E). T26S/R40E encompassesthe communities of China Lake and Ridgecrest, the eastern half of Inyokern Road, andArmitage Field. Samples from this township indicate the presence of two aquifers. Theshallow aquifer, generally less than 50 feet, has been sampled extensively throughout thearea and contains over 40 years of records. In the last 10 years or so, there has been anoverall increase in TDS. This increase seems to be related both spatially and chemically todirect seepage from the sewage-treatment ponds located in sections 13, 14, and 14a, and tousing sewage effluent to water the NWC golf course in sections 23 and 24. A limitedamount of data is available on the deep aquifer (generally greater than 500 feet), but thewater quality seems to be relatively constant over time except in the case of one deep well.The two aquifers are probably separated by a structural control, such as a clay layer, thatprohibits or inhibits movement of water between the aquifers.

I An influx of sodium-sulfate water causes the water quality of the shallow aquifer tovary greatly. The spatiai relationship between the sewage ponds and the contaminantplume and the fact that the sewage effluent is sodium-sulfate water points to the sewagelagoons and the watering of the golf course as the principal contributors to the increase inTDS in the very shallow aquifer. This plume of contaminated water runs NE to SW andcan be seen most dramatically on the sulfate contour map generated by computer.

I A limited amount of data is available for the deep aquifer in this area; however, itappears that thr, quality of water has not changed significantly over time.

Water samples obtained from the north and northeast sections of the township, in thevicinity of China Lake Playa, show an increase in sodiam-chloride content probablybecause of the proximity of China Lake.

Township 26 South, Range 41 East (T26S/R41E). T26S/R41E lies to theeast of China Lake and includes Lone Butte and Salt Wells Valley. Water samples fromthis township are of a high-TDS, sodium-chloride type and are not suitable for domestic orirrigation use. These waters are very similar to those found just to the northwest of thetownship in the China Lake playa area and to waters pumped from the Leslie Salt Companywells located in 26S/43E- 17D.

Township 27 South, Range 38 East (T27S/R38E). T27S/R38E lies in thesouthwest corner of Indian Wells Valley and includes Freeman Junction and Armistead.Few wells are located in this township, but those with water quality analysis in the westernSierran portion indicate that the water is of the alpine type. Water from section 3 ID is ofthe sodium-carbonate type with a TDS of 196 mg/L and a fluoride content of 4.6 mg/L.These characteristics could represent condensate from a geothermal system.

Township 27 South, Range 39 East (T27S/R39E). T27S/R39E is located justnorth of the El Paso Mountains. Many of the wells in 27S/40E have waters of the sodium-chloride type although there are wells with other types of water (such as well 27S/40E- ID,which has sodium-chloride-bicarbonate water with 452 nig/L TDS). Both of these types ofwater could represent geothermal leakage. The second type could be a mixture of asodium-chloride and a sodium-sulfate geothermal brine. Haystack Peak, to the east,exhibits snowmelt. That is, after a light to moderate snow, Haystack Peak will be snowfree while the surrounding areas are snow covered. This phenomenon is an indication ofgeothermal leakage. Well-defined snowmelt areas occur at Coso and Roosevelt

37I


Geothermal Fields. (Roosevelt is near Milford, Utah.) The waters of 27S/41E may beleakage from the Haystack system entering the township over clay layers in the alluvium.

CHANGES OF WATER QUALITY 3CHANGES WITH DEPTH 3

Water quality is a relative term. What is good quality depends upon the use. Whatwould be excellent culinary (drinking, domestic use) water would indeed be poor qualitywater for the producer of salt. High-quality water in a hot-water-type geothermal reservoir Iwould have a high temperature and low TDS. Feed water for the boilers should have lowTDS. However, most people consider water quality in terms of culinary waters, irrigationwater, and water for livestock. For these purposes, the gross measure of quality is TDS,but certain trace elements, such as arsenic in culinary water or boron in irrigation water, arealso important. Hem (1985, pp. 210-15) cites EPA standards for culinary waters and givesa good discussion of water quality in relation to use including industrial uses. In thissection of this report, water quality is referred to in the gross sense-amount of TDS.

Water quality may increase, decrease, or remain constant with depth. Some examplesof water quality increasing slightly with depth include the Red Hill/Little Lake/Lumber Mill Iwaters. The spring at Little Lake has a TDS content of 1,084 mg/L, while the Lumber Millsite well with a depth of 611 feet has water with a TDS of 1,228 mg/L. A deep well justinside the NWC boundary (26S/39E-21N) near the Inyokern substation had a dissolvedsolids content of only 215 mg/L (residue at 180'C) and calculated TDS of 221 mg/L.Figure 12 shows the dissolved solids content of this deep but very pure water and theshallower wells around it. Figures 13 and 14 show variations of water quality in somewells of varying depth within specific sections.

CHANGES WITH TIME UThere are two schools of thought on the groundwater system of the Indian Wells

Valley. One school, whose strongest proponent is Dr. Pierre St. Amand (1986), hnds Ithat the groundwater system is a closed basin and that losses from it are limited toconsumptive use, evapotranspiration, and evaporation from China Lake Playa. By makingthe assumption that the values of the losses at the playa equals the recharge, one can thenpresent strong arguments that the users of water in Indian Wells Valley are "mining" waterand that the future of the Valley is indeed quite bleak.

The second school, whose most vocal proponent is Dr. C. F. Austin, acknowledges Ithe surficial losses given above but makes considerably different assumptions onsubsurface recharge and losses. He believes that the groundwater system is open, thatrecharge exceeds the surface losses, and that Indian Wells Valley is actually contributing Iwater to both Searles Valley to the east through the underflow beneath the Argus Range andto the Koehn Lake/Cantil area to the south through underflow beneath the El PasoMountains and Black Hills.

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0

200

0-18 K1

19 30 C1

400 1--m 30 F1

30 J1-*~ k 19 P1

30 F3

19 K1 1902

m 0600

I3 800

m *k21 N

1000 21_N

0 200 400 600 800 1000

TOTAL DISSOLVED SOLIDS. mg/L

3 FIGURE 12. TDS at Well 26S/39E-21N and Closest Sunounding Wells.

III

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III

200

01 07-31-78

0. 400

P1 03-29-80

02 10-25-73

600 ; 3K1 03-29-80

800 o0 200 400 600 800 10003


FIGURE 13. TDS Versus Depth in Wells in 26S/39E-19.

II

I

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0

I

3 200

K1 05-04-7901 09-19-57

E- 400oo _____

3 Ri 09-18-58

600

3 M1 09-18-85 P1 05-04-79

800 1L0 200 400 600

TOTAL DISSOLVED SOLIDS. mgL

a. Section 26S/39E-24.

FIGURE 14. TDS Versus Depth in Wells in the Sections Noted.

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200 3Y F1 05-12-76 30 C1 05-01-75I.-w.,' J1 4-17-6

i 4F3 10-25-73400 I

0 200 400 600

TOTAL DISSOLVED SOLIDS, mg/L

b. Section 26S/39E-30. 3FIGURE 14. (Contd.)

I0 101 10-25-73 I

1A2-10-27-77 3- 200

400

0 200 400 600


c. Section 24S/40E-01.

FIGURE 14. (Contd.)

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Our evaluation of what geochemical data contributes to the solution of the abovedilemma, both factual and hypothetical, will be given in the Summary.

The closed-basin school is very concerned that high usage will cause significant lateralmigration of water from areas of possibly poor water quality, hence degrading waterswhere deep pumping depressions occur. Of special concern is the possible migration ofsodium-chloride waters into the Ridgecrest well field from the southern and southeasternparts of the city.

In 1975, Warner stated "in 1972 the dissolved solids concentration in the groundwaterin some areas is increasing slightly, but where this has occurred, it is not yet serious."

In 1987, the USGS made a proposal for funding to the Indian Wells Valley CooperatorMeeting on the basis of water-level decline and water-quality degradation. Theydocumented their proposal with five graphs.

We had computer printouts made of the various ion concentrations of all sample sitesused by the USGS with serial print outs. We tried to estimate changes of quality with timevisually, but this approach did not prove satisfactory.

The approach finally taken was to convert the time intervals to days and to calculateTDS by summing the major components-those with concentrations reported in mg/L, notgig/L. There is considerable scatter, probably because of normal variance of analyses,slight variation in the components, mistakes in analyses or reporting. Regression lines(best-fitting lines mathematically) were then calculated for the data. If the fit was good(goodness-of-fit can be calculated) and if the slope is positive, the quality of water wasdecreasing; if negative, increasing (which is doubtful); and if zero, remaining constant.This approach was partially successful; the times when it was not are attributable to poorcurve fits because of the scatter noted above.

Except for a few wells in the Ridgecrest area, and the shallow waters of "area R" onNWC being contaminated by seepage from the sewage ponds, we believe that the quality ofwater in the Indian Wells Valley is changing little, if any, at most wells.

GEOTHERMOMETERS

The Geothermal Program Office at NWC is the Navy's lead laboratory for geothermalexploration. The Program Office has long believed that the Indian Wells Valley contained alow- to moderate-temperature geothermal resource that could be tapped for space-heatingpurposes. Indirect evidence for a resource within the Valley was seen in elevated watertemperatures pumped from wells, old hot springs deposits, and unusual snowmelt patterns.Now, however, a more direct method of determining geothermal resources is available bythe use of chemical geothermometry. Chemical geothermometry uses water analysis resultsin estimating the geothermal reservoir location and temperatures. The two main families ofchemical geothermometers are the silica geothernometers and the alkali geothermometers.

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Silica Geothermometers

Several silica chemical geothermometers are available: quartz-conductive-cooling (also Icalled quartz-no-steam-loss), quartz-steam-flashing (also called quartz-maximum-steam-loss), chalcedony-conductive-cooling, alpha-cristobalite, B-cristobalite, and amorphoussilica (Fournier, 1981). All silica geothermometers use the general formula I

T = [x/(y- log A)] - 273.15whereI

T = the reservoir temperature (0C)x = a number from 784 to 1309, depending on the type of silica I

geothermometery = a number from 4.51 to 5.75, depending on the type of silica

geothermometerA = the concentration of SiO2 in parts per million (or mg/L)

During the course of this study, all the silica geothermometers were calculated fromavailable water analyses. Our experience with the alpha-cristobalite, B-cristobalite, andamorphous silica geothermometers indicate that they sometimes give unsatisfactory results;in this study they gave numerous temperatures below freezing. These results are thereforenot reported. Results for the quartz-conductive-cooling, quartz-steam-flashing, and Ichalcedony-conductive-cooling are given in Appendix A.

Waters derived from geothermal resources are enriched in dissolved silica. Therefore,excluding mistakes in analysis, all sample collection errors tend to lower calculated results;for example, precipitation of silica after sample collection but before analysis and dilutionof geothermal waters by cold, low-silica waters. Hence, silica geothermometers representminimum resource temperatures. Also, the silica geothermometers generally apply in the Itemperature range of 0 to 250*C (Fournier, 1981). Above 250'C, the quartz solubilitycurves depart drastically from experimental curves, making reasonable calculatedtemperatures impossible. Because all silica geothermometers have the same type formula, Ithe general form of contoured results should be the same. Therefore, only the quartz-conductive-cooling geothermometer was contoured (Figure 15).

The highest temperatures calculated in the Indian Wells Valley with the quartz- Iconductive-cooling geothermometer are east of Armitage Field at NWC and exceed 1400C.These higher temperatures are part of a larger area of warm calculated temperatures(>1200C) trended north-northeast that cuts between the mainside area of NWC and the nairfield. The most striking feature on Figure 15 is the plume of colder water (<40*C)emerging in the vicinity of the intermediate wellfield. This plume spreads out and appearsto trend north-northwest, paralleling the hotter water to the southwest. One other area ofcold water (<600C) is seen along the eastern boundary of the map, just east of the area ofhighest temperatures.

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I 8080 60 40 )

( 100120

1000

80

74- 140

+ -h +I 8060 ARMITAGE60CO

760LESS

I' 6808

I 100

1IS 04

FIGURE 15. Tempemwtre Contour Lines as CalculatedI Fromn the Quartz-Conductive-Cooling Geothermoineter.

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Alkali Geothermometers

The most commonly used alkali geothermometer is the sodium-potassium (Na-K) type. ITruesdell (1976) initially developed the Na-K geothermometer, which was later modifiedby Fournier (1979). Where waters come from high-temperature environments (>180 to220°C) the Na-K geothermometer generally gives excellent results. The main advantage ofthe Na-K geothermometer is that it is less affected by dilution and steam separation thanother commonly used geothermometers, provided that there are few positive ions ofsodium or potassium (Na+ or K+) in the diluting waters relative to the reservoir water. Itappears, however, that the Na-K method generally fails to give reliable results for watersfrom environments below 100*C. In particular, low-temperature waters rich in calciumgive anomalous results by the Na-K method (Fournier, 1981).

The sodium-potassium-calcium (Na-K-Ca) geothermometer of Fournier and Truesdell(1973) was developed specifically to address calcium-rich waters that give anomalouslyhigh calculated temperatures by the Na-K method (Fournier, 1981). The effect of dilutionon the Na-K-Ca geothermometer is generally negligible if the high-temperature geothermalwater is much more saline than the diluting water and the geothermal water contains morethan 20 to 30% geothermal brine. Fournier and Potter (1979) showed that the Na-K-Cageothermometer gives anomalously high results when applied to waters rich in the Imagnesium ion. To address this problem they devised a magnesium correction, which isapplied when appropriate.

The Na-K, Na-K-Ca, and the Na-K-Ca-Mg calculated reservoir temperatures are given Iin Appendix A. The Na-K-Ca values are contoured in Figure 16.

The Na-K-Ca geothermometers indicate a high temperature (>200'C) anomaly justsouth of Armitage Field (Figure 16). This anomaly trends west-northwest with smallerspurs from it trending southwest. Other small anomalies of >2000 C temperatures lie to thenorthwest, north, and northeast of this main anomaly, although the anomalies to thenorthwest and northeast could be extensions of the main anomaly. There is a largemoderate-temperature (>1400C) anomaly emerging north of Armitage Field trending north-northwest completely across the Indian Wells Valley. However, this anomaly is based ononly a few data points and will need more data control to characterize. Areas of cooler Uwaters (<1000 C) are seen northeast of the airfield (two anomalies), and along the easternboundary of the study area, immediately east of the airfield.

Discussion

Comparison of the quartz-conductive-cooling and the Na-K-Ca geothermometers(Figures 15 and 16 respectively) show few similarities. The greatest similarity is in thearea of cooler waters located along the eastern boundary just east of the airfield. However,just west of this lies the north-northeast trending high-temperature anomaly, which is seenclearly by the silica geothermometer, but only as a spur from a larger anomaly by the alkaligeotheriometer.

We think that this area is a prime target for further geothermal exploration because of its iproximity to large Navy laboratories. Space-heating costs can be dramatically cut in thesebuildings if a moderate-temperature resource exists. Toward this end, three thermal-gradient drill sites have been located within these anomalies (Figure 17) with drilling of twoof the wells expected to conclude before January 1990. Results of this drilling will providethe next step in the exploration process for geothermal resources within the Indian WellsValley.

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I 100

I 395

I 140

100 FIEL200 14

3 140

100

FIGURE 16. Temperature Contour Lines as CalculatedFrom the NA-K-Ca Geothermometer.

47

I

NWC TP 7019, Volume 1 1

N~I

I ,

396II

'7

ARMITAGE710 FIELD 0

BOUNDARY 5AI

44 31II

I

FIGURE 17. Approximate Locations of Three Thermal-Gradient Drill Sites at NWC.

48


SUMMARY AND RECOMMENDATIONS

The obvious conclusion one can draw from this study is that the geochemistry ofgroundwaters in Indian Wells Valley is complex. Using a computer classification of watersby principal cations and anions, of 254 water types possible under the classificationscheme, some 55 occur in the Indian Wells Valley, Rose Valley, the Sierra, the Coso andArgus Ranges, the Coso Geothermal Field, Salt Wells, and Poison Canyon.

Groundwater Flow Cells

By lumping similar waters together, the following major groundwater flow cells can bedelineated.

Sodium-Chloride Waters. These waters are found in the Coso Geothermal Field,China Lake Playa, southeastern Ridgecrest, Salt Wells, and Poison Canyon.

Sodium-Carbonate Waters. These waters are found in the Coso Geothermal Field(one site). In southwest Indian Wells Valley, two sites are noted. The presence ofsodium-carbonate waters in these areas very possibly indicates geothermal inflow into thesouthwest part of the valley.

Sodium-Bicarbonate Waters. These waters occur in a horseshoe-shaped areafrom Inyokern up to the dividing line between T24S and T25S and back down toMichelson Laboratory at NWC. On the east side of the horseshoe area, an area of mixedwaters-sodium-bicarbonate-chloride--occurs between the sodium-chloride brines ofChina Lake Playa and the sodium-bicarbonate waters, indicating mixing around the Playa.

Sulfate Waters of Various Types. The sulfate waters occur in Walker Well inthe Sierra, the Tungsten Peak Mine, a well in 26S/38E- 15, some wells about 2 miles northof Inyokern, and deep Rose Valley waters. The source of the sulfate may be oxidation ofsulfides that are formed by mineralization or that occur in lake sediments (the Walker Welland Tungsten Peak Mine), or geothermal activity. The very shallow waters in "area R" atNWC are contaminated with sodium-sulfate-rich waters from the sewage ponds.

3 Alpine Waters. These waters are characteristic of the mountainous regions, and arecalcium-sodium-magnesium-bicarbonate waters with low TDS.

Red Hill/Little Lake/Lumber Mill Site Waters. These waters are of somewhatvariable classification by computer, but generally give similar modified Stiff diagrams.These are calcium-(sodium-magnesium)-bicarbonate-chloride-(sulfate) waters, and areprobably a mixture of alpine, deep Rose Valley, and geothermal waters.

Groundwaters of the Inyokern Intermediate and Ridgecrest Well Fields.In these waters, sodium is usually the dominant cation, although sometimes calcium is.The magnesium content is usually low. Bicarbonate and chloride are the important anions.These waters could be formed by concentrating alpine waters by transpiration andevaporation and mixing with small amounts of geothermal waters.

I Argus Range Waters. The waters of the Argus Range are sodium-calcium-magnesium-bicarbonate waters.

349

INWC TP 7019, Volume I 3

Variations in Water Quality

Water quality may degrade, improve, or remain constant with depth. In most cases Iwater quality has changed too little with time to be identifiable. Exceptions are a few wellsin the Ridgecrest area. Degradation may represent vertical leakage from low-temperaturegeothermal reservoirs in bedrock. Other possible areas of geothermal inflow are the Isouthwest comer of the Valley and the Haystack Peak area of the Spangler Hills.

Geothermal Leakage Into Indian Wells Valley IIt is highly probable that waters are entering Indian Wells Valley from the bedrock

basement. There are good indications-measured temperatures, pseudo-temperature Igradients, and chemical geothermometers-that there is geothermal leakage into the Valleywest and just north and south of the main gate of NWC. Haystack Peak, which exhibits avery anomalous snowmelt pattern, may represent another source of geothermal leakage into 1the valley. These geothermal plumes may be a partial cause of some loss of water quality.

Water chemistry indicates probable geothermal leakage into the southwestern portion ofthe Valley, recognizing that the Little Dixie wash area of the El Paso Mountains is a deepcircular sub-basin, separate from the Indian Wells Valley. The fact that a complex wateroccurs all the way from Red Hill in Rose Valley to the Brown Road turn in Indian WellsValley indicates a major flow of groundwater from Rose Valley into Indian Wells Valley.

Further grounds for this belief are provided by the conditions at the lumber mill onCalifornia State Highway 395. When in operation, the lumber mill used about 1,000 acre-feet of water per year.* When collecting a sample there, millworkers told Baskin that there Iwas very little drawdown. Lower Little Lake Spring flows about 1 cubic foot per secondor over 700 acre-feet per year. Most of this flow infiltrates. These facts indicate that theestimate of 45 acre-feet a year entering Indian Wells Valley from Rose Valley by Bloyd andRobson (1971) is absurd. The 10,000 acre-feet estimate of Thompson (1929) seems morereasonable (and could be conservative).

Another source of recharge that has been neglected is leakage from the old aqueduct;Austin estimates this leakage to be about 4,000 acre-feet in the Indian Wells and RoseValleys.** Another source of recharge not usually considered is water from the Sierran 3granites and metamorphic rocks. Volcanic rocks may have permeability because offaulting, jointing, vesicles, or rubble areas between flows. Faults, joints, and even micro-fractures all contribute to permeability. The Tungsten Peak Mine, when last in operation(and never completely dewatered), made 110 gpm of water or 180 acre-feet per year.***Another source of this type of calcium-sodium-sulfate water is a shallow well in 26S/38E-22D. 3

We believe that enough usable chemical data are now available to enable interaction offlow data with structural data. After the geochemical data have been integrated with thestructural and other data there may they be additional critical sites that should be sampled.It might also be desirable to obtain Tritium ages on some of the fundamental water types.

Dr. C. F. Austin, personal communication with Dr. J. A. Whelan, June 1988. 1** Dr. C. F. Austin, personal communication with Dr. J. A. Whelan. June 1988.* Dr. C. F. Austin, personal communication with Dr. J. A. Whelan, June

1958. 150 I

Ij NWC TP 7019, Volume 1

iREFERENCES

U Austin, C. F. 1987. A Comment on Modeling of Geologic Processes. China Lake,Calif., Naval Weapons Center, 29 July 1987. (NWC Reg Memo 2606/201, document5UNCLASSIFIED.)

. 1988. Hydrology of Indian Wells Valley. China Lake, Calif., Naval WeaponsCenter, 10 June 1988. (NWC Reg Memo 2606/103, document UN-CLASSIFIED.)

Austin, C. F. and J. L. Moore. 1987. Structural Interpretation of the Coso GeothermalField. China Lake, Calif., Naval Weapons Ceniter, September 1987. 34 pp. (NWC3 TP 6841, publication UNCLASSIFIED.)

Austin, C. F. and J. K. Pringle. 1970. Geologic Investigations at the Coso Thermal Area.China Lake, Calif., Naval Weapons Center, June 1970. 40 pp. (NWC TP 4878,publication UNCLASSIFIED.)

Bailey, P. 1946. Report on water supply of Indian Wells Valley, Kern County,California, to the Lands Division, Department of Justice; United States v. 529, 533acres of land in the Counties of Inyo, Kern, and San Bernardino, no. 3472-H civil.

Banta, R. L. 1972. Groundwater Conditions During 1971 in Indian Wells Valley,California. USGS Open-File Report, Water Resources Division, Menlo Park,California. 22 June 1972. 9 pp.

__ 1974. Groundwater Data, 1973, Indian Wells Valley, California USGS, Open--File Report. 9 pp.

Berenbrock, C. 1987. Groundwater Data for Indian Wells Valley, Kcrn, Inyo, and SanBernardino Counties, California, 1977-84. USGS Open-File Report 86-315,Sacramento, California. 56 pp.

Bloyd, R. M., Jr., and S. G. Robson. 1971. Mathematical Ground-Water Model ofIndian Wells Valley. USGS Open-File Report. 36 pp.

Bureau of Land Management. 1980. Final Environmental Impact Statement, ProposedLeasing Within the Coso Known Geothermal Resource Area, Inyo County, California,prepared by the Department of the Interior, Bureau of Land Management, September1980. Pp. 2-1 through 2-7.

Duffield, W. A. and C. R. Bacon. 1981. Geologic Man of the Coso Volcanic Field andAdjacent Areas, Inyo County, California. USGS Miscellaneous GeologicInvestigations Map 1-1200.

Dutcher, L. C. 1959. Data on Water Wells in the Freemont Valley Area, Kern County,3 California. USGS Open-File Report. 125 pp.

Dutcher, L. C. and W. R. Moyle, Jr. 1973. Geologic and Hydrologic Features of IndianWells Valley, California. USGS Water-Supply Paper 2007. 30 pp.

51I


Fournier, R. 0. 1979. "A Revised Equation for the Na/K Geothermometer," inExpanding the Geothermal Frontier, Transactions Volume 3, Geothermal ResourcesCouncil Annual Meeting, 24-27 September 1979, Reno, Nevada. Davis, Calif.,Geothermal Resources Council. Pp. 221-24.

____ 1981. "Application of Water Geochemistry to Geothermal Exploration andReservoir Engineering," in Geothermal Systems: Principles and Case Histories, ed. byL. Rybach and L. J. p. Muffler. Chichester, England, John Wiley & Sons, Ltd. Pp.113-22 and 109-143.

Fournier, R. 0. and R. W. Potter II. 1979. "Magnesium Correction to the Na-K-CaChemical Geothermometer," Geochimica et Cosmochimica Acta, 43, pp. 1543-50.

Fournier, R. 0. and J. M. Thompson. 1980. The Recharge Area for the Coso, California,Geothermal System Deduced From dD and d18 0 in Thermal and Non-Thermal Watersin the Region. USGS Open-File Report 80-454, Menlo Park, California. 24 pp.

Fournier, R. 0., and A. H. Truesdell. 1973. "An Empirical Na-K-Ca Geothermometerfor Natural Waters," Geochimica et Cosmochimica Acta, 37, pp. 1255-75. I

Hem, J. D. 1985. Study and Interpretation of the Chemical Characteristics of NaturalWater. USGS Water-Supply Paper 2254, U.S. Government Printing Office, IAlexandria, Virginia. 263 pp.

Jenkins, 0. P. 1962. Geology Map of California, Trona Sheet. California Division of fMines and Geology.

Koehler, J. H. 1971. Ground-Water Conditions During 1970 in Indian Wells Valley,California. USGS Open-File Report, Water Resources Division, Menlo Park,California. 26 November 1971. 19 pp.

Kunkel, Fred, and G. H. Chase. 1955. Geology and Ground Water of the Inyokern Naval IOrdnance Test Station and Vicinity, China Lake, California. USGS Report, preparedby Ground Water Branch, Long Beach, California, 1955. 166 pp.

_ 1969. Geology and Groundwater in Indian Wells Valley, California. USGSOpen-File Report, Water Resources Division, Menlo Park, California. 23 January1969. 84 pp.

Kunkel, Fred, G. H. Chase, and W. J. Hiltgen. 1954. Open-File Appendix, Tables ofSelected Data to Accompany U.S. Geological Survey Closed-File Report Geology andGroundwater of the Inyokern Naval Ordnance Test Station and Vicinity. USGS, Iprepared by Ground Water Branch, Long Beach, California. July 1954. 115 pp.

Lamb, C. E. and D. J. Downing. 1978. Ground-Water Data, 1974-76, Indian WellsValley, Kern, Inyo, and San Bernardino Counties, California. USGS Open-File Report I78-335, Water Resources Division, Menlo Park, California. July 1978. 42 pp.

Lee, C. H. 1913. Ground-Water Resources of Indian Wells Valley, California. CaliforniaState Conservation Commission Report, pp. 403-29.

I52

I

II NWC TP 7019, Volume 1

Lipinski, Paul and Darwin D. Knochenmus. 1981. A 10-Year Plan to Study the AquiferSystem of Indian Wells Valley, California. USGS Open-File Report 81-404, Menlo5 Park, California. June 1981. 16 pp.

McKee, J. E. and H. W. Wolfe. 1963. Water Quality Criteria. California State WaterI Quality Board Publication 3-A. 548 pp.

Mifflin, M. D. 1968. Delineation of Groundwater Systems in Nevada. Center for WaterResources Research, Desert Research Institute, University of Nevada, Reno. TechnicalReport Series H-W, Hydrology and Water Resources Publication No. 4. 53 pp., plusappendixes.

Moyle, W. R., Jr. 1963. Data on Water Wells in Indian Wells Valley Area, Inyo, Kern,and San Bernardino Counties, California. California Department of Water ResourcesBulletin 91-9. 243 pp.

3 . 1977. Summary of Basic Hydrologic Data Collected at Coso Hot Springs, InyoCounty, California. USGS Open-File Report 77-485, Menlo Park, California.September 1977. 93 pp.

INaval Weapons Center. 1982. Map of Naval Weapons Center, N3530-W1 1715/45X45.

Nilsen, T. H. and R. H. Chapman. 1971. Bouguer Gravity Map of California, TronaSheets. California Division of Mines and Geology.

Norris, Robert M. and Robert W. Webb. 1976. Geology of California. New York, N.Y.,John Wiley and Sons, Inc. 365 pp.

Procter, R. V., T. L. White, and Karl Terzoghi. 1946. Rock Tunneling With Steel3Supports. Commercial Shearing and Stamping Co., Youngston, Ohio, pp. 27-28.

Silver, Leon T. 1986. Evidence for Paleogene Low-Angle Detachment of the SouthernSierra Nevada. Pasadena, Calif., Division of Geological and Planetary Sciences,California Institute of Technology.

Spane, F. A., Jr. 1978. Hydrogeologic Investigation of Coso Hot Springs, Inyo County,California. China Lake, Calif., Naval Weapons Center, May 1978, 56 pp. (NWC TP6025, publication UNCLASSIFIED.)

St.-Amand, P. 1986. Water Supply of Indian Wells Valley, California. China Lake, Calif.,Naval Weapons Center, April 1986. 71 pp. (NWC TP 6404, publicationUNCLASSIFIED.)

3 Stallard, R. S. and J. M. Edmond. 1983. "Geochemistry of the Amazon 2. The Influenceof Geology and Weathering Environment on the Dissolved Load," Journal ofGeophysical Research, Vol. 88, pp. 9671-88.

IStiff, H. A., Jr. 1951. "The Interpretation of Chemical Water Analysis by Means ofPatterns," Journal of Petroleum Technology, Vol. 3, No. 10. Pp. 15-17.

3 Thompson, David G. 1929. The Mojave Desert Region, California. USGS Water-SupplyPaper 578. Pp. 144-85.

£ 53I

NWC TP 7019, Volume I 3Truesdell, A. H. 1976. "Summary of Section IIl-Geochemical Techniques in

Exploration," in Proceedings, Second United Nations Symposium on the Developmentand Use of Geothermal Resources, San Francisco, California, 20-29 May, 1975,Volume 1. Washington, D.C., U.S. Government Printing Office, pp. liii-lxxix.

U.S. Geological Survey. 1987. Project Proposal for Evaluation of Groundwater Quality in 3Indian Wells Valley, California. 11 pp.

Warner, J. W. 1975. Groundwater Quality in Indian Wells Valley, California. USGSWater Resources Investigations 8-75. 59 pp.

Whistler, J. T. 1923. Report on Indian Wells Valley and Freemont Valley, California.California State Division of Water Rights. Mimeographed report. 83 pp.

Wilcox, L. V., J. T. Hatcher, and G. Y. Blair. 1951. Quality of Water of the Indian WellsValley. U.S. Salinity Lab Report, No. 45. 33 pp. 1

Zbur, R. T. 1963. A Geophysical Investigation of Indian Wells Valley, California. ChinaLake, Calif., Naval Ordnance Test Station, July 1963. 98 pp. (NOTS TP 2795,publication UNCLASSIED.)

IIIIIIIII

54

I

INWC TP 7019, Volume II

IIAI5 Appendix A

INDIAN WELLS VALLEY GEOTHERMOMETRY31920 TO 1986

AIIIII!III5 A-I

INWC TP 7019, Volume. 1 I

TABLE A-1. Indian Wells Valley Geothermometry 1920 to 1986.All temperatures in °C. 5

Type of geothermometer

I rn ILocation

Az-.! I

011

3-M - 3 ' &-S-S3 - - - 6-2751386- 31DOI 61 57 19 qq 6 -

8ae.- Ztot 3-2-q. 74 -73 '42, 130 23 -

'3-21-4O! q 7 "4 37 N I Z? 21.7

z'i/,o.-'o 'f.lt-zT-. '~ '7. q4 '5 9 bq - :244i1

&-2A-72.: 5 q7 6 ,'I1 &i - 30. oZI/ - -SI4 o

.3--7-74 14 q(. 43 )(-4 72.

z7S).4oe- I'Moa /o-.-q ' 97 ,,. - - - - I• t-24-7o0 - - - ' , - -

2"/4] Co - oq#oj j o-,o-j . . . . . . - I4- r..,:3 - - - ' q 77 - -

/-2q-72. /05 /o0 7(a INP - 30.0 32Tko/- 07o1 9-/cO-10 113 //Z 34 /2 ( - 30.o

27&/4qo- 9.02. --. 4 q -q . . . I

ZS/4/06- /OO g-- - - -3 jq 70 -

?S7/ gl - o7eo 3-2-% q2.. Tq zi ) 33 -I

3-lq-. - - - 1S2 3 - -

3-2.-4* 21 94 4) (*,3 32 - Z1.o

ZTVo6- /0201 3-7-74 3-q 47 7 7-2 158 13f -

41-7 q 2;. - .50 /0 170 15S 1314 Z5.o a

&-97 9 41 IL 174 ISJ J35 4.o

(-- 42. 1 /(oz. 153 133 2.oS-z"- n" 36, -(a 1'74 1,. /35 Z7#.5

2S/,/oe - IOA,, &-if.-&L /05 /o5 -S ",3 9-f - 21.q I

ZIA-2e- al)0O1 421 - 9 7q 37 /12.

A-2 5

NWC TI' 7019, Volume 1

TABLE A-1. (Contd.)


Locadon

2Sou/OcOI 9U7s-ip//a IO A0lq 7

3-fb? - 7-

2~s/qe - ICo?. q-,Ly-(& /0! /03. -7( 11 / 7 .-

/00 -11-W. /99 '7 65 /OS 7( -6

'He-SI- - 4 q-;- 23- -j U- /4jb9 -

q-9-164 /02 /13 (073. 'I~ 1 Z .

3 q-'5q -7 (. -0

-7Vqe -Mot Y-3( -4o

3~oe 1/CO3ZO 3-*- 7 /03 (o9Z / (62. -

I.-Z.. 7 /07 /o3 72. /IO 7/ ~ 2.

I -~7z /02. 4S 4'2 /1-5 -73 -P

3 A-3

UNWC TP 7019, Volume 1

UTABLE A-1. (Contd.)

Type of geothermrnometer 3

LocationI

4,-,6--M /q1 b &q' I 71 6o Z4.o

5-27-90 /0/ /07- 71 2? - I3-s ,o7 /o? 7 /1 (q -

Z731Y- 6P~ v- 5-. 32. 41 /y 78 (

-- - - - /0( 70 --

_ - - - q8 . - -

Zr,/k... o.o I q -zT. , 4S G3 13 13L. /34, 32. -

r--)Vco - oz.ro1 27f- (.-9 /05 /06 7(p //3 tp 2. - -

4- - PS, /0(0 7(a 173 (Os - - 54-17-7Z. /04 /ui ? //0 (,(4 - 24.o

3 - - 7 4, Ol o / 09 4 O 0 ?2. 1 .q - - I3-!-7T /03 /o3 "3 IZt (q - 27.'s

1-74 /08 10 ?9 /19 G ?. - 2/,

tl-2-78 /Os /06. '7. (a I(. -ft - ,.)

e,-I- 7 /05 1O 7(4 13 71 - Zr. 0

S-Z3 -to ca1 Jos 7q 017 -7b - .s m

Z5)9c6-,imol 5-l-Yfs q3 +6 (.2 , - (9 ,

9 q2-q 99 17 51 73 o(--3 -- - /12 161 ( 244

.271 - 61k01 q-3-Z1 /if 110 g1 - - - -

I,--t-.O:I-Z - - - qg "7 -- 27.

-l. - - - IIIbf TI - 3a-J-'i -- - - //3 I$ a2 -,

6,- - - - ; q - ; - ic&/4 -#oI . -- i - - - q 3 -

A4

NWC TP 7019, Volumne. 1

TABLE A-1. (Contd.)

5 Type of geothermnometer

Location

&-8- 10/'oo4o 104 ?- 0I4e -

S-I-v-- 3 48 /C6 -7'q

27be ~~i2-p*-7L - - -9 (0

17SiO- OZ4, 4-15-7Z /040 1046 77 Y6 (01 73. o

I7YE 0C~O4.. I -31-b N9- '172- (.3 -

& -0:09 13-+ So 5!5 -

I V~~-o~3 -Z2-77 14 6 - - -

-XW- 040 -- IS16 S-i -

-iz-4 1114 Sid -

7 -1+4.7 101f /0-4 71~ - -

7.7 - WD I -22- 4A - - - 1'q (6-3

5 3-31-70 - (03 sq

44b-1Ps -AO-/(/ 40S - -

5 36j'A-3so2. 46-iv.-72. r 17 It-4- qo 19q 'IS -71 Z4~.

/~3R,'a3- - - ISZ 172. 5z.

- -' 5z~ '4 3?

5 3~77- -213 130 -

I -I-S3 q q (a (03 393 -48 2 4.4

2&S 06/1f -7 S 00 /01 11 /1 51 - -

3-j7:- - - 0O4 &a0 -

5lui.Sd*- 3qC0i S-i-Y6 q-4 to &4 2(4 t.o-O. t 101/0 71 '20Qi W3 -

5 A-5


TABLE A-1. (Contd.)

Type of geothermometer I

Location

COYI

Z~~qW- .3p34-0,, a +

, '! I

'I-2s- R, 91 .o, 1"78 SO - - 37--6-7 qv q - 4,0 - - I

2. . E-',99 .lg .- /,@' 1 l9i!z. ( - --

-Z'-q o7. o3 -12 242. (&,S - -

Li6g - - - rr (.75 2S. 0I'l~ ~ ~ Ia 6.1. L 0

-- - -0 -Z- 247- -

la- - _ -1(63

,?-I0I- lo 0 1 70 its

-93 /47 s - i" 3 I 42 . I - -

395 4 2. 47 Z. - -

q?5 9,7 (OS zS 64

q-7.-45 & Z i . (2.

- 1 I ?.f . 63 -- -

'17 lo S( I a CS -0

II'-' Z. 94 - 6 18 -1 -

/o-D--t '. q7 (. I27(0(0 & -- - i/2-b43 '15 (2 Z q4 S6 - -

Z3 'S 91 S% 4 -2A2. &0o

6 3 40 2o0--.7L~ 7-+ 37 20q -

A-63


U ~TABLE A-I. (Contd.) - - -

3 Type of geothermorneter

I Location

/0-25-73. 70 . .2 - W 58 -

(-wr- 7z 77 4Co 19q + ? -

s-z ' j /0o G9 12Z S

;-i.-T4, q,? (.7h - -4

34I3-ZKj II- 41-77 '33 1Z~

giz--- Is'I 7

LA.-/oog 3zIi '7 -453 19 7 -

&S4i- Zo, -r-9 7 7' 1 45 19zjj 44. - 27.

ZIjj6 34-0 /0.i0 3 - 70'4 15 z

;-1.-74q 1 Z4 M 33 -q 2 ( O -

3-6LZSt 1 -08 /y/ 22.- -O

U 1 ~-(- 3 - - (,- 191 77- 7

t'O .-3Ai.-21-S - N. ; - ' 1 1. ( IS M-

I11 3/..UJ( -- RZ 92 1. S? 1- q Z3,0

(0-n-as /Oz /05 7 2 133 &go7.

26sj-?q /07o /z 7 33 - q 24 0 73~I --2-5'1 Z34 fl I ip

35 6 A-179S3 -W

NWC TP 7019, Volume I

TABLE A-1. (Contd.)

Type of geodhermometer5

Location

I-to-*. icig lo ?q 331 q 78 24,o3

a,5/06 3oo3 /P-2'-W /t -51 -

- - ?z /UTS - -3

3-z3-7-7 -- (' j

-i' 300 /(0S3 4Sq -

Z(/o- 304ol 3 -3 -b, / 3j :8

2(s-e 26Ho 137-s 22 1--oZo

-6jO- -qO It -2- 7b WO3

2&5j~qOE 31bKO?. 3-3/- b - --

Z- 78 -7, S4 -

9~/~o~ -v-(,7 3q 47 7L 32.(. 215 -4

2-/46 2D~-r-- Z3 t- - 24. t

2& - (.FOI -u-2(v3- 4411 17 17( 9,q (o U.-

4,o-!6 -N-82 1-7 -1 1- 1. (o -? 5! Z-4

&Wq30Fb~-I 7S V'3 43 IS:; 41 - -

6,-7- (. 71.. 77 4a Isq, 44

&21-4 72 12.. 47 150 -is

IS~ 82 S9l 158 -98 - -

A-83


TABLE A-1. (Contd.)

3 Type of geolliermometer

Locafion L

(.4-03-74 (03 09 31 IZ8 i

5- 1- 7 4-7 72 3S 13o .413 -r2-3r. '4 Sgq 12 'zi42. - -

2t5/X -,03 5---6: 1 .1I IS'S 43 - -

11i-q-49 *78 8 Z 471 qz 10 -

9(d- 2q S5 /3&, 40 -3R 4- 1 24 ~ 4 'q 1313 3,9 - -

/0-20-;b 91 Pq '49 13S 36 -34-23-11 9( 9' ,Y9 42- -

/O-Z7-71 -7-7 a 4 q Ie~s .403t4-6-72. - - - /k8 -41

/0 -ZS -73 (, -74 -33:7. 133 38- -

243ie- 2&.O 1-2(,U2 q4 'T~ (03 - - - -

3 25B'~'-- 3ow:l S-I-7S -7- 93 48 Iqafaoe-.o 7-8-53 - Sz. (a0 23.

I(SA 2C--3-/L e vuZO/'7 ?. 323 a-(

Z'43VCe28ZO 0 OV4 - - - 204 OZ.3Z(.St- 2oa (.1. /00 /01 vo 327 TI3 78e 2&..0

2'qSfe- 28&110-7--l - - 1(02- 35 - -

3 2&1/ae- ZeA*3 6 -1-53 - Z 02 173 90O

3.5/qoe- ZAoi (--1-2- -53' 1-73 80

g 2 bs)J/6 -3W 219CI -3 - - Z4 74~ - -

26SE- SCI0Z ~ /94 3q - 2.

3-Sly*E-ZWO1 3--S4 - - 2Y .-

5 A-9

1NWC TP 7019, Volume 1



UU I I2"E- Zvo2_ (a -'7/2.q ? 12 1 %~ 23.q ' 43 Z4.(3

'5-3-83 /ZS I2Z 9? 248 9 7- -33

9-8-84 )2.4 IZI '70 24(o 'q(, 3(, 7A. 0

-Io-SS /Z o /2.4 'M9 24 95 37 24,. Q

2t/406 ZzIl Z-O--4 94 1 64 /l? IZS 11o 3Z.Z(9-0-L- 7' 7 3 -'. l 9/ 19 W a /09 Z7, 0

6-22--S 14 ZA -I 9U I1,0 1I zq. s

5-29 -78 82 4 10- / 7 Z7. 0

2-o,4ot I 7 i 6 1 24(o 4,4 - - 3-I- S 2So 5. -

S3-4o 71f 78 4 2 8 S3-

.6-I-isl 3 11-2 5q £S3 3'1 2'7.81-I-L 175 797 43 IS? 39 - -

4--a 79 23 48 )1o3 43 I-b-3gs g9 S4 *i .

-6 5t _ 13q 33 -

4 -)at 6Z82 41 1$. 4o - -

S1 4 Iq I163 4s -

'-'I?-~ SS :5) /J 3S - -

/O-Z3 (4 %&I gq 49 /36 37 - -

&-S-4.u 3q '12- q. I 3z, 3( -

/a-q-f 1,5 :1 42 1o 3(o - - 5A-10


I TABLE A-1. (Contd.)

5 Type of geothermometer

0

UU

ILocation

~ '~ ~ 7 13(a 3S5 4-,-7, s 75 q 43 131 3q - -

. 3 '9 0 56 16 ,q 5 --

/o-27-71 7' 78 42. 132 34 6 - -

4-b-Z4n -33 t - -

:?0 - 7s X 24"7)

5..< Is- s : ,. 2-q 34 - -

"7-31- 77 7 I I 1'3 31 - -

C-4-749 9 o 5( a -is- - -

3-N'-8o7 8 82, 1 - q 32 -8

q-18-a q 5 1 /q 3 - 27.,

i 3 - z -- -4- 9 ISz 4- Z7. Z.P -t4s I! w 31 2(.,:?3O-I~3- - - - Z-e 3 -

-- - - ? - -

/o.f~-q.-35 - - - ZC4 , - - ,i2t&SIIF--2Z Q0 I'1q3 40 Zn2 48 -2tI

o-s - - ,Z04 4 z -

a ,5- - - - .07-

* I

/,* (*1, 7-1 21 4s /f.2. 32

I3 A-Il


TABLE A-1. (Contd.)

Type of geothermnometer£

Location ~ 3-

b U

-4-jq -2? po - -a 3S156 S o(

4s so 33.q

- - FKz 45

~-+s :M ~ 43 11-1 ss?,..2,7 9 3 48 (, C3 - -

104-,3 - 21 4s j(.~ 32 - -I

,5-00-4.4*2I 4 4-7 151 41 - -

915'<44 ? 7 12 48 N-9 48 - -I

e,-Zi- : -72 77? 4a IS(O - -

-4q 48 1'+ C.0 - - 3- 78 4-. /(fl, S?*- -

4= Z 3S 1 28 S1

I4 I - 436 0 :S 3 s

(-g2g-71 '79e 78 4 2 118 qf. - -

A'-,Z7-'7f 7LN 78 4 z. /q-7 So -3

o-i4-U! S-S too 2-1 1-28 TI - -

/O-lS-73' 77 91 .4s /3? -44 - -3

(r(-oo-'78 -(-4 )I2. qj -

-A -543 13q 50) -

eq ss Ia~ z~ oq 7.

)46 I I L -3L. 13q 154 /? z.'-'5- 63 /1 /0'? ISO t~q 2o4 - -

A- 12


3 TABLE A-1. (Contd.)

3 Type of geodiermomnetr

LocationW

I 2~~t 7-4-S3 jq V( ~i ". ~

1 - i33 )37 27 23.17

4-zB-72. /as /o(. It'., 210 31 31Y zs o33-to-74 /0 /01 ?0 US~ 2? 31 -

5 -Iq-76o/7 /0-7 78 2.L4 20 -40 sD4-70-a 02 /a?-13 7zZ* g3o 39 Z3. o55-31-7q, /09 IOq~ 74 241 9z, 31 ?S1.

TZ-e SS Sj 11-21 /2Z2. 3 Zz. 0

4-3-q../O~ /(o a Zb 4. - -0I lI-o.a - Zgo U 4 433 .9- 130 .(

5 a 31- 24 w !9-q-q 71 12. 51? 12 4 -

2b5/3L--241MO1 -- 7S 79 43 1- 'I (a

/0-I'I.3 7q* -78 q 7- 3oo lazo ?S5 -00-1-4 g3 S Z . csz I -

71 I'? S 5) 1-7z. 4ot -3et..7q '13 qa 1-74 4S

A-23-7 79 8Z14-1 /7S 42. - -3 --. (A' 74 31*P NS 43 - -

-n37 21 -qs / IY 44 - -

e.i 78 S2- 4-+ IRO '46 -

JO24 31 q I q(. 38 - -

'31 /a 177 '48-

3 A-13

1NWC TP 7019, Volume 1 I

TABLE A-1. (Contd.)

Type of geothermometer 3

Locaton y

z

/o-Z7-7 75 " -71 43 1co 48 " '

4-P-72L (al (q '2) /(, 41 - -

/o-s. &(, 27 1-73 42q - 1

'-i-7S o3 ( 9 3/ /Y(, a - -

S1-;6 1- /Wo bq /Y2- 951 - -1

7-31-;6 'q 71 37- 2A 4 - -

- 24 4q 1"7q <13 -" -

3-2r,-& -7-L -7-7 -40 Zoq SC -

2-8s I I(a 57- 20, '43 - I,/0-9-3 /O? /6-4 7G 2.3 /7o - -

?-1 IO / 2, 71 2-- 17?2. 21 2o

41I2-8S 101 /01 qu 2io q0 IN 23(0,13,q6. IQI oO-w-d 2S Z2 r4 11q 3

/o-q 70 75 31 /04 ZS - -

c-5- 164 '91 4 '141 ISo 3 - -

1-10-t6 72 77 .,0 /34 44, - 31- -~ ,-77 '91 4 173 53 -

-i-6! 7q 13 4'8 123 54 - -

4-45 78 4z, A7 3-7

9S(-4(g 92 541 1(: 3'9 - Iq-7L~t 72 12. 4z 141 36, -

4-2-6? 1.3 36e ., /Y3 3(6 -

10-M-. 22. ZC 51 ' /4 34 - -3

4-5-1. 74 79 4. P /41 33 -

83 t o 2 / Yq 36 - - 3A-14 3


TABLE A-1. (Contd.)

3 Type of geothermometer

UU

4 0 ,

3 4-t- 21 84 qs /.2. 3q -

&-23- / '' S-4 170 31

/o -Z-7/ 79 32. 47 / ,4 3S - -

(,-a-?z 70 76 -31 /63 3,5 -

3 -w- 4 70 75 3 /'33 3(. -

S-1-75 (:S, 71 33 13to 3(a

3 -1z-?, 4& S5 15 'cit - -

7-31-7 -,3 G 3/ 17S 35I -y'-2 g'. g qt ,-M" 32. - -

2N.S/,E- 23o 1 -27- Av, -7 3 2o 2 9 -q-

2(.S/6E- 23Z-o 5-Y- -n /17 f(. zq /ZS /39 4 22.o

9-q-gq /o /O1 '7q 331 q 7 78 -

3 ZSA2t6--2.41.01 (-a-7z. /10- /07 79 1q3 172 S-t- zz.o

2.5/4a- 2ZO t.-- - 11- 7 /i s a 21q 170 -*'

/0-3-13 /IS //I % Zoq /-72 -

9-1-4 1-7 (a 9 :l 3 '7(a - M o

6-1-8S /27 /24 'Tq 27 17 - .o

2,,/31fe- 24601 q27-%, g% 24 4? IRS .4 -

2613% - U ?0I /c)a-- R 2 S4 20'. '? -q-

'4--1,3 27- is 5 12( ize s -

1 0N-1-3 ? I S1 b4 22. - -

I 9 54 1 o 44A-15

3 A- 15

!NWC TP 7019, Volume 1

TABLE A-1. (Contd.)


LocationL

~I

q-7- 4 1- 41. 2J4 4(a - -

S32., 3 ; 57 21 - 4-7 - -3

-- ,7q '3 4 / a - --

) 114 -,9 / q-, 39- -75 79 43 17o 38 - -

-- 7-7 91 4S 11 1 3 q - -

A,-3m- 4 .a'7 10 S t "Y - -

&-I-7o ) . 3S j4, - '-

/a -o-. 7q P 48 2o 4b -- 5/0-27--71 79 3 Y8 Zo 44 - -

-- (a ' 33 20(o 3 -

:? 12 -q8 1293 41? -

-Oo- : 74 ;- It 43 - -

-I-7 70 75 317 1I 35

~-qs- Sie )5 /&? 38-

7-31-6 775 7q 43 22q 30 - --

5--) SS 8 S4 /23 34 - -

11 66 52. 111 27 24.o

2440F- 2p-1 OS7L /O ?Of, 2 y . 202. q1 24,o

1-7-84 /00 l1o :7o Z78 oo ?0 1

303- - - 3o 3 2 % 24

S,s/W.3of /-1/ /0 91 q /8 33 22.o

%-7-84 /too log 20 103 12's - Z, o

, -i- qZ 4 to1 104 127 - 27.o

2./40E-ZJ4o1 &-nl III I/; o 2,6 111 - 24.o a44--a /ZZ 12o q4 224 16, - 0

Si- 12-o III 12, 237 I' - 0

-". -- - Z%1 Iaq' - Z

A-16 3


TABLE A-i1. (Contd.)

3 Type of geothermomneter

Location j I1

2 -v4. q 12.2IZ %a 274 178 723 27-5

,f28 1230 12(o qa1,, 24 I8 2.3 '24.

2c.s/4oE-22HoZl (-rz-7z /j 10-L 7,1 119 132,. - 50

414-~ -Z % ] '9 S? IZ? /45 - 25

S-Is--,M all e 43 120 /4,/ 23.

W-2 q1 '94 e41 /1( /Z? -

/0 -/V --3 qqj q7. Il~ i /o30

c&-,-azs q 7 qe1 11 u~Izz -

32,S/4OC- 2LHO3 6,-I3V2- /OS 105 '75 /42Z /q7 n 240

4- 19-Z /01 /oz.. 71 IS(, AY - 25,0

6-115-, A/67 /07 75 ~ /,5 M - 4

I 2~ 1" 110 21 '&O 150 24.0

-.. 'l o/o0 l oi Is0 /V 3q 2z3-794 11-7 //(a 19' 213 n7 to-

V-4f'cJ 113 /12 94 iyeq /bjc. Z4

3 -. ~ / is 18 Ii / Y( i9(. .!5,'

q-(1-x M / /7 1/ 0 ;c q? /39 Z'Z

1~/'.ob -15-64 -3 9 (o 2 S- I71& 32 9

S-tf -- 23 4 -

2,S/qae- 23Aci$-r--z /13 /1. 84 /y~/ /,Yt% 53 22. 0

~-~ los /Oo 7c q 2, /' S3 24.o

S-r1-7q /0(0 /Ob /yj JqS 0'3 (c S

35-71~-go /10 /0,9 To i39 /Ya 151 2cs

f~v/11. 1l i ~. 33 /39 S/ 2 4. s

3 A- 17

INWC TP 7019, Volume 1 I

TABLE A-1. (Contd.)

Type of geothermometer 3

Location ------- 4 j 32165/W - Z A62- 5-74-77,: IZI Illq 13 1'4:5 /, (al 22.5

e,Nt?)B 1/0' 1(q ?'O /Y'3 N8~ S Z3"5

-57- M /1 II 7 12. 5 2. 1o 43 15. <

u-OQ /1% //:7 10 t32 N'3 :58 2q.

Z'.f/',iE- ?IDO /o-7/43 77 81 4S q . /2 - Igig.3s qq .3 'Is 1,2? qq 23.a

qc-? oA-71-gi 22 5-0-7 I3 /3, (6-

1-4-26' 1(6 7 SS /34 N5. ZZ.

5/~~-2/f -- z 1 S'4 Iq 1 ,, 3 "q7 37-7.-4 III fla /10 /so I yto nq 0

4--S/.. 11.4 /o3 IS4 Ado /s¢/ 270. ,-o,. in /7o Itgq o l 1 j. -8 3.,

, -S/4/0-I2 COi 7-4-Q 4 -- 4, ).

I(1-2ir -B, 48 C' S I S is ' 5 8 3-.5-z, -gc 3s 44 3 :?r /CD~ ; 2o.o

A-/O18. 3 6 3 (a I - IXS4E- 2MIa -IS-A jo't J09 I -q - 5a

E-444 I I 'S 1 /3s N'3 - Z?.o 54-a26~,Z 1 20~ tit I 1 15 - Z S4.

)(,S/qaC-j'Ej q-zl 24 3 - /6q ('74 - -1

19, - 5 4 24..1

A-183



- Type of geotherineter

LocationC sU

-./W r741 b(-S i-U4 z t

U xs/va- 9 7Zo 10 S(

3-~ 367 /03 1( (.7i~ -

-I Fq 43~ 2-'3 Soa /2j 4

,Uk n riq 4-t'- ;04 104 74 Zza bo - 2.3 1-7-tq 104 104 '7 ZZI S-4 - -.

0o-6' 10(. o( I? zq ~b - 24.o

5 2&jsE.-s-o'S3: - - 152- 32Z ZO..

7A~J-13A.401 &~f-Z 6q (( Z? /I(~ SO 1 0

-2tosjqqoE psiqo- .- ,q-g2.- 74 72 41. /2S 17 - ZS. 0

9- -14 /Oq IN~ 7q '9 1 ?2. S9 2,3.0

6-11 1oq /09 30 /04 13(4 5. 2So

leU~ 5-e3-b - - - 120 4)

3 -20o-a /0? i 10; - /33 130 53 24,o

5 -10-10 lcn. /03 77- /S4. /Y-1 -93 21.S

2&/t&130 -,6-lz 'Iit 13 /51 134 t, -

3q-, 7 -,4 q4 % (-3 23 153 72(,t-yg- 99 /6Zo (q 20? 52.- 4

326O/Jg-8i /ol /o2. -1 118 /-?1

2'/3~-,vo ~f.~. . 2q4 - 2417

3 A- 19


TABLE A-I. (Contd.)


a ILocation N. ~C

- - - " 118 (N3 22.. 33-5-7 q3 q5 42. ' /24 /70 -

W' qZ 56 1t 24 /2Z 2o.:

q-3-;6 3q 4,3 I ( 2, /.4 -1 24. o

-2o- /0. /03 . 71 I C? - Z.5

5.22-0 q 5- qq. < -. /24 - 23. 02(,s /oc- is6oI d/-28-* Mv I /13 7 f4 I 2. - -

7-3 - - - : ?q 7 21. I/02- - /4o 44 21,

- i 111 /60 ( 1 q i

1.4--/4 G I /Y 13(o a .<

q-I- 19 (0 10( 7e, 91 22.0lq~2- z 94 (01 /01 Tq ss ZA

5-9 q 4 4/ IC I f4 q0 2".o

&40-13, S- (0 - 3 94 3 24.1 IsAe-/76oi 1-a-s - - - 174 37 -

2&Vft - 13C~t o-/v-n ( ' 7-H 33 17 0 - zC

S-24-so 4a 56 I1 is 8 1 8 a9, 12(,-I 1-z 5 ? (4 8 12 32. c) -

6 4'-;e/1 /09 1 1-3 '1 4 Z I

0- Oq sCY ,o S1 i - 2..0 I1-)q /Z- no 94 j'zs 91. 90 20,.a

A-20 3


TABLE A-1. (Contd.)

Type of geothermomneter

0>

Location

6+2 /70 /i 2 /24 817 (2, o

I 6-g-s /04 /04 ~-4 124 10 -78 2-4,o

I ~ ~~2qcF,-7?&j 1-2&za '.o

4 4 -4q-q6g 8V S? 1'77 :3q-

X!Vwe - go .1-6-9, 69 Z , A03 (e'1 - -5 ?.s-//-No j. %--4 117 /1 r 9 / 13S 58 A 2o

II~sfr4. '&7 /03 /03 7 9( 6 - -3 .S/3qe6- /o'4o1 /-9-( S3 (a 174 '37 - -

2r.S/4AX-/wof 4-12-q4(a q /b 64f 7.4 7Z.~7-Ce-S3 - - - %( 112. 3? .21-iI32(-.S(3qe-7&~g4oi .' 25 89 :54 /5! .41 - 72. a

q-z(,-4q' (3 (61 1/ - - -

'3.9-V-9, 77 31 -is -

23-SIWM- 21O&--- - -3 -q 119 ? 27.

4 _tc-j o_ 7, - -5 - 1'3 - - 2

f-27-8 -is -3 -cIS 3q 13~*(. 5 20.

36 0-/Y-20bI W-7 -21 -I -3 /37 13&, (4 210

35-15-A -SI 1Y2, PA' / (. z f.

(-nz-IS Z -I -'S3 /37 ,/V3 9-7 -

3 A-21


TABLE A-1. (Contd.)


Location ,.

3"7O4 f 2 -I q I, /.t 0 ' -

2&--qoe. JITOI -74-r i' /'i g 2,o n

265/ -/ 8-'j-1 /Y /3 z '4 1-35 aq4 / 27.o

4-It-SS 104 /04 74 2 11(s 5 - 3Z(-S/3-e'O1 -- 27-41 6 ~ ( - 131 40 - -

2T¢5/3q-/26'I i-22- . - - -- 22) Z4. 32 -ln

)-2-1, 34 4i -I Z6 ?.21 -

2s,,s/3 q -// o .~-3-( z e. q4 ,/ , - C9 I

7- -s3 - - /69g 37 a

(,-- ?o :?o ?S 39 1(04 4z2i 3!-4-41. 77 21 IS 1(2. 41

, .. 2.. IS S) /33 31 32-~ IS. S1 / Vq 32-

.--'-.e, 77 3) es /qs o 39 3/O-7,o.6i. 7 ?o 5 'VR ?q - -

,-7oR " 2.. .47 /9' 3? -I

-' , - -

/o-7-) 73 2s . 4 7- 1S8 , " - 3/v-2s.7 13 1 ; SZ, /2.8 3" --

4-00-74 Wf ?4 31 124 7 - -

A-22 3

.INWC TP 7019, Volume 1I

TABLE A-1. (Contd.)


Location " "Iz

U S-f-75 (a7 ?. 3 -

3 S-gz-"),, 37 ?o 56. 124 3? - -

7-3).-B 77 91 45 15/4 43 - -

n-Lj7 ?~ S S1 jig 34 - -

3 -q'b va is' 5! 1 , 41

2%56- oEIOCe 1-24-A) 21 -4 4 9

I q/3'E-~io~~ -77 vo 11 1"

243 225 S1 366 -'

I 4.- 7 - --. -7o - - - 2s

IS ZS -18 It8 13 - ,

2Z. 3 ( ( t 1(. - Z3.!5

I - ;-4. 4 , z, I /1t q2 - zo.5

24.5/c- /oot 7-4-53 -- - IS.- Lv'z. 46, 21, 1

I 4-rl-'- o /10 28 /28 q 2,o

3-(-7 3S 43 2. /3o 21 I3 3-21- 57 .4 25 )qt 74 - 2, 0

I- iI-% ?0 ?S 39 / Z, 4f - Z.o

( ,- 3- 39 47 7- 13 -5 210

.--l /01 /2. /oz I7 9. S - 2.o

S-ZO-8o 114 % 13 /-f (AO 9 - S

(.--82. 47 72 :3S /23 ?2. - z 0Z.

IS-11-7 2' 43 - qq - g0,

-2-50 42 so /o 132- 35 1-2. 24.5

3 2Gae - IAOI 7-(. . 3 - //0 Zaa 2o3 -.8.3

2t6/'//E-7&1 "4- '-5-3 --- I3 S - 20

3 (-29' 5' 1 7 /7" ?? 22.0

3-0-7y, 5q A ? -21 313 I -2.0

I A-23


TABLE A-1. (Contd.)

Type of geothermometer III

Location qo,

w? :z 3s (4 /o0 &

(-Zo-& 69 74 2- 0 )24 0 ZZO

?.'/38 4qg~-7(.-q4 (' -7 7'3 - Is 41? -

2r-S) OE - ( 0 7--r3 - - - &S-7 21. 3S3 -t o (00 z -11 21, 0- 2- / 4 .q 12. I

2tS/1ss- osan 9-q- S3 - A6-7M 74 - h

-4 - /Ze - Z.

4-14-u- q-5 17 (!S 13 (

q-, - qI, q? 4,(- -

I-q--.8 3'7 90 S, o 17 2. 35J -2,o /%?5. 0 8) 4T

4-I-',, 46 9o c bC 133o ( -

-o ?.'. < Z1 IZ4 4- I(.ZI77: /D9 1o4 74 123 : - -

7V 72, 414 09 43 - -

1- IS 42 q-5 34. - -

1 3n.- I % , 5 . zz .53

5. 1- 7S; t 9 133 48 /-a (,. - -

o. /o- 3 /0

2~44'E-5~o3S 3 (.o 2-4 /'~I'Z. /V04 -

I, ?-2A--, q3 S-1 13 /72 /31 - I

A-24i


Type of geothermometerITT -I>I>

,Z 5/412 -QO 4-2- 3 Izq 74 203 6-ts-, 7,1 14 -30 q4 13q Z. -,

-r,- 45(0 $3 5~ 74 8 1/3 3z3-Z4'11 2 -2s 24 /'1?~ -2.

2GS/*ae- I .Z77,I I -Z4 /aDj /71 0- -Sq- 130 "S 15S- 20.o

S-20-go 8z. 8S 130 1!: 111 22.025 iloi 7-8-53 - - I(A I'3 SI 2i,1

&d-13-7-z 42z- SO /0 t13 /'S S 21,o(,- -27a 39 47- 7 /01 /64 S4 ZTo3S-4-7q (6S 71 '33 /o4 I Sq 44 2.

6-p-aL 48a SS I's /O2Z IS :5z2 24'a

,1,,q~ q1VO - ' ? /A4 8 42. -3 ~2o 2e/ 366 -) CIO 1~z- - - s S(O -

23-l 10-1. 1 -2u--n - - (,0

& Sj -Fb 1 '-&44$ q- qp o7 r,,5 ?~*-3 73 - -53o S6. Z1-

2, 29 Ss 213-~74 '78 42. /s o 0

6 .21 qI1 7 /44 52- -3q-(A6 &a j .5S 11(4 qa

46/O-wwr gl. 2q ss (365 Y. --

1-'y-te /00O lb /33 4s --

3 A-25

NWC TP 7019, Volume* 1


Type of geothermomneter3

Location

zz

j~2~*4~ ~7 '1.0 4 /30 a -

-- 2'7 S&,( /30 4-7- -3

SS 92 5 /37 .4!5 -

-771 TS S, '2 48 o

6-O-~~az 47 IZj 43 - -

,5-1-75 60's to9 31 /2s 4(0

Y- 1-7 S7 &q Zs 127 4(D -

-7-31-78 -77 e1 qcj /32 44 -

3--- 7(o 3q 55 1~33 -4~?

2&-!qoE- JAc. - - - - --

-4B.33 42. 7a 134 - 7

3 Doi q(. 47 1- 2-4 -5~3 -

XS40s'-I.4o -M-Z - - 40 1-3;7 ZO, 0

2&5/* - 2cot q -z-4% i 99 ,2 /(o3 44 -3

255/4qoVr- L.71-4-53 66 ~S 114 38 21.

16~7 /03 103 73 5 I /2. - 5 0'

2~SS3qe- 354 4.3>q( /Oz~ 103 ?Z 1 4$ 8

4.0~ !52-- Za.o a

-1(-6/4 (P2 -a

W~?-'~ 90 15 124 48 - -

4-~'Iqs 9,- &S /3(. -4- 1

/0? 37 s 82 S4 134 4s

/0-5-737'S -7q 43 /Ir 46 - -

A-263

NWC TP 7019, Volume. I

TABLE A-1. (Contd.)


LocationJ cu

3-1-.q 3 q5 (-Z /0: 4 - -

-7- 31-78 S~ 1 4 4'? 13o 4(, -

ZS)% -3 ol?-7-74 6-7 -71. 35 &15 151 /14

3 7--x S3 4o 21 !:3 (155 24,5(.-ZI-79 Itt 1/0 91 (v /So

SWe!-31 -18 -63 19 Z89

25- v& 331-2 3--74o1 9 - /4 4 2- 2.

I4-Zi-- 2to 3s -7 1 S-f i(7 34. Z3. o

5-3t-R) -2i -8 -153 /.C, /168 3-3 21.0

"u'-82- 34 4? 1 p4"? / O -33 z?.

3255/34- 31 M Q3 6S27.(Lq: - - - /1 Z15 40 -

ZSSL Zf-35M oe 1 -S-S3 - - - Iss &( - -

5 5S/31E- 3iE0I zq2i' CS 6L 23 111 - 44

2'SS/31,- ?I DOI IZ? sq 21.0?2SI)sbe 3GS13o 44-6 1 q 3 0 11 -

2551396 ap0i 4-2j-r%~ loq go 171 44 - -

32SS/4AE-3/6ol 7-- q(-,. - -

3 A-27


TABLE A-I1. (Contd.)

Type of geothermrneterI

CUUUb

Location ba

2SS/396- 24hj bl ~ C q2, 14 (0/ I/00~ 4!5 -

q.4 26 'Y? -S 10 /15 - -

10-270.- 14 ito (a3 III IG 4

(,-23-11 /05 /o5 :75 Al 24 38

/O-7--71: q% r~t 41 /0:7 /15 '33 -

,--7..(P' ;i1 33 /34. 95 34 -

2Z-5/it-r- 27Col 7-4-43 - - - 191 /(*a 38 .(

4,-,'-72 1,/1 Il 81 190 13 4Z Z?.o

24s/3qe6- Wq4'1 4-5-5 - - )SS5 41 3c), a

A-*-9 - - 59 4 1 - 30,(.--q,7 - l*d 43 36.

+ -s - - 14 4. -

9--6 C9 74 21? (4S 4 . - I

&-7-61L '7? 81 4s ~. 41. -

3-i3 3 48 3df / O - I/"-q-43 21 B4 49 f19 17 -

9-f- 31S q9~ MY /~ 37"-46!4 4 3? 1 sea - F

-,~w Iq 13 48 IS3 .3117W 78 82. 4'; 19 '23 -3

(s~7.(01 6 29 /4(0 4 -ea

w--~ 9 2q /31~ 3 -

S-i-7s to 67 29 130 4. z

A-28I



Type of geodiermnometer

4)4

-I-.78 '8Z43 -i- I*q 7q 37 15(.*4 - -

-q 77 61 4s /Vq7 9

5-?f-vo 78 e Z 4? 141 3 -

ZX53%-Iz2 -48 74 78 '42 139 3. -

It-q-4s IS 43 I/W3 %

tva:-- -7 -n v -S ivq'13? -

3 jO-o-n 7 81 45 )(o 35 - -

lb01 2 4 J$9 40 - -

O-25-?3 7S ~-'l 43 13 - -I 2M/4W-2,AA 78-Sl - - V7 752s)a,-w -s,3-L 41 -1 Itc%: 1W

ZSsI31E -19k'Oi 4- S4 q &,& Z7 Z20 f1. 32 -

25- 3M--* 1'7I '92 L30 &2- -- 1.3 25/ioE~~ I-z,~ - - - 23(. % - i.

--- 74 /04 104 -74 24a 39 1 0 -

s-ZO-W 2.4 3 1 -12. 2Wo6 173 91 11105-6- 310 45 3 115 5 - 20-a

5-20-80.3 Le 21 2j '78 48 i'3 482. 77 81 4s 21 q3 4S ~2.8

2S51fle-f'i~i -7-q-53 - - - 103 /ab - 2.

3zss/3w- mat. 4-atq. -1- -n7 4o A14 &Z - -

ts/j*if-24NsI S-s-3: I S IS-4 3932ss)3q%-24qi 4-25"f. - 223 30 q -

3 A-29




Location -

/0.2--b IN i ( "rU -6 ,

jO-Z--7'5 ql IS 11 IZ3q 7S z (,

-- X- --- q T --- --- - -- I-zs s -Z-8 48 - sq 233 ( aS-126-4; /0. v~ I2 /it 11 9

I

- 1 33 / 22 ,(, - 7Z.o I

I

A3f 2Z13 111 22.S

Tr48 1 74 qq Z AIi 4z -z. a7.

2%S3,LOI (.-IS-8i -78 8L 4- 2o3 &2.. - .0I

255/23a- CCO1 1-25-4r. d07 /10- 24q 9(o 32.

2S5 /X- 17Wofd+z-' 3(1 49 .3 21. -?. -S

2%1l3&- ImDsI 4-2t.-'. 1Z. 23 -alZI VS 2o - -

2?S/3%-.IZOO 2-3-S3 - - - 71-. 1-71 -

-73-7 IS S4 94 '1?,. 38 -

-4 - z . 3 12d 9'4 ze

2%M 9Sq zz.r~~

A-303



Type of gohermometer

L-----I4)

zz

I25S& 2oZ 4-2-Z*- -

-71-2 /01 -q3 1 ( /&Z. §1I-M-.18 4M / /(. '59 -

q--. z 94 e.g 1gg /6z 4o -

i -S-'8 Se 12, 6q 14q ?1 48 -

3tY~ 1is& 1~'7 &15 Zss 14 34

/0-20-W /7v X7 b 121, q, 13 -

6,-1-70 113 //2~. 8-4 1975 ?8 ?.

I/0-26-70 q?3 is 4 2o ?8 49

4- 19 q 9(a 163 /141 55 - -

A30 I 6h 93 (0 24ts /(, 22 -

/CO-2s-73q '? 5 3 i 4z 12 INj ' 44 -

1. '3 48 Iqs 171 33 -

~ 1231I 97 3,3 -

2S3e-1M ~-S32 )2 YS /._ 0

-5A -I 17 1 -vsa14 q qIR15 -14.)/ 4i) t9 1% 0

A4 /13 21% 11 A

"W/~ 211 22. 3(6I q-w.1 , 01 102. R/19j3 Wv -

I A-31


TABLE A-1. (Contd.)


9

Location

It- io3 /10 93 jq3 S3 -

0 0 -0.6 3 1 04 / 64 "-74 l 7 7 7 2- 3 S -

Co-(:v-(-s //1Y /13 gS j'94 77 4 -

6-:5-(v8 Ica /ol 70 2oq Aq 44 -

- - - 24s qS 30 -

lI7 /1 .3 2! . 1I

00<X-'7 q1 011 4" 2.0 r -

00-00-?.. I N S. 11 W 5Z

-Z- 73 /z /1 7I 2?D 2 72 -L ? - I(0-60-?4/~Z M~ /q -2 2a. '77 S. -

S-'-Z 61Z q4 to 1 215 94 34 5<-rz-. 10 /o4 7.4 2os -73 Z, -

73- /05 /o 75 2(x. 77 39 -

191 (.2 )9 w9 -

/os /0? ?q 2oq 22. 41 -

2'5SJ32C-I/keo2 191-~ - - 1 IZ1~9-5-S - - - 200 &- - -

2!/; -o 7 o1 4-3-4* -32. 41 -1 /3o /,5 - -

2S51396-a~ +ii-s. /2, Z? -21 20q /91 34ZS 40C- CA0 1 -- 6.3 - - 2Z'r4 I " - I

3-74 /04 /O4 "77 222. 1,2. 3

3-24-75 /03 /0 73 244 203 39 11-o

/--, 11 82. ZZZ 1q2. "1 20.o

A-32


TABLE A-1. (Contd.)___


>

U

2SS 14.X 43 Z14 I 0 1Z5S - ?z 3

AD-0-a.qf7 918 &1 2j. -4 91

21 2'4 41 ISO 1/ 33 -

9--f~. 26. 21 _e 195 'P 47 -32C4- 92 11 S? 2o '3 - -

11b-a9 q3 (, -9 ?q

92-i~ I'S SI ,'% -7 -I6 J- 9 4 15 200 19 -3

c>Q-)78 92- 4: 212 z 15 33 -

n2-)-7 11 5l 2 2. 45 - -

S7z. 77 40 0510 204i -

/o-ZS-73 '316 'I S-;- i1'q 99 q

6-,%-4 77 8( 45 21?- 123 -2. -

S -17S W2 7 4o 1194 11 - -

5~r~7qq ~ 43 1q1 157-31-18 NO' C S ZOS qj- 30

3-2q-~ S9 N 24 aZ 1161 27.

31~w nho 7-4,43 - 11-L IeS 121 24o

2Y//3-33Y*I -2-zrT-Y4P 44 3 241 19 --

s/e?3 oo-7, - - 323 <q

3 A-33

NWC rP 7019, Volume I

TABLE A-1. (Contd.)

Type of geochermrneterI

13Locationzzz

;24q,',We-q8, -7-6-53 - - -C -4 7 -.

2q)e -W 3 q-ui-'& 42- 50 /0 1-77 f 5 15

210f-33WI Z-5~-ZO qq % (3 - - - -

4 -Z,, V,, 78 31T 214 q S 11 1 -&

2S/36-7aol Z" I :k -

zqS~qx26 -( - q3 2j.2 o

zislq'f- tOAo1 4-X-K 1?% 29 - is (7? 117-

23Sji--r-17ta I-rl- SS - - - ZOq'? 321--

Z25/38-ao20* 7-iv-- a -2 - 4 37 -3

2~~- 7-3-SS -q 9~'1 34 -

'7-30-6 i- /0' 1 7 -0 A.- 1! 113

A-34