Figure I Generalized map of the Wilbur Mining ... - University of Utah

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Thompson T OC pH SIO2 Al Fe Mn Ca Mg Sr Ba Na K Ll NHi| HCO 3 CO3 so^ Cl F Br I B H2S Na-K-•Ca Mg corr SIO2 Na-K-Ca Adlabatic Conductive Ânalyses,in mg/L Table 1. Averaged concentrations for spring and well water in the Wilbur mining district' Wilbur Hot Spring 52 7.5 176 1.8 0.17 O.Of 2.5 15 3.6 3.1 8700 ^08 11.6 29'* 6900 — 356(H) 9980 2.1 19 12 233 165 236 8it 218 _—_ Jones' Fountain of Life 60 7.7 89 0.35 0.05 2.6 31 1.6 3.0 9880 it 32 10.7 120 57IO — 71 11,700 3.5 31 23 2H0 232 118 223 to Wilbur Hot Springs (see Table 1) Wilbur ffl geothennal well contains (1) a higher chloride content (11,100 vs. 10,000 mg/L), (2) a lower sulfate content (260 vs. 36O mg/L) and (3) a much lower magnesium content (2 vs. 15 mg/L). The magnesium corrected Na-K-Ca geothermometer (Fournier and Potter, 1978) indicates temperatures ranging from 10 to 160°C. However, because the country rock around Wilbur Hot Springs is principally serpentinite, the high magnesium in Wilbur Hot Spring is probably due to serpentine dissolution. The uncorrected Na-K-Ca (Fournier and Truesdell, 1973) temperatures, which range from 220 to 218°C, may be more reasonable. Water from Wilbur ff 1 geothermal well has a Na-K-Ca temperature of 2IIOC (Table 1) and very little magnesium; a correction of only 1°C is calculated. Due to possible silica addition from serpentine dissolution, severe difficulties are encountered when using dissolved silica Blanck's Spring 12 7.8 121 0.19 0.05 3.5 69 1.1 1.5 7220 360 6.9 125 6390 — 180 8050 2.3 21 18 150 730 232 16 198 —— Elgin Mine Springs 61 198 0.17 1.0 1.8 28 3.7 9330 510 11 213 7270 — 86 11,550 3.2 30 25 210 170 211 118 208 — •'— Wilbur fi Geothermal well 110 8.8 133 — 1 2 10,000 110 — 275 5170 1170 263 11,100 16 — • — 118 211 213 201 Meteoric water 19.5 6.8 21 — 3.1 182 — — 132 1.1 0.16 — 1020 0 185 83 .37 — — conoencration in estimating thermal reservoir temperatures. The difficulties include the following: (1) the silica may have already polymerized or precipitated so that direct application of the silica geothermometer (Fournier and Rowe, 1966) will indicate a low reservoir temperature; (2) the thermal water is probably mixed with dilute meteoric water giving rise to the observed spring water compositions and temperatures; and (3) the.diluting water or the warm mixed water may contain some silica originating from low-temperature serpentine dissolution. For comparison, the conductive and adiabatic (with assumed subsurface steam loss at lOQOC) silica-mixing-model temperatures (Truesdell and Fournier, 1977) of the warm springs are shown in Table 1. Despite all of the possible problems using silica concentrations in springs from this area, the adiabatic mixed-water temperatures are in moderate to good agreement with the Na-K-Ca temperatures. Fournier (1979)' indicated that silica reequilibratlon is more likely to occur than Na-K-Ca reequilibratlon. The —
silica concentration in a water sample from Wilbur ffl geothermal well is below that expected in a 220° to 210OC water; however, It may be in approximate equilibrium with quartz at 150°C or chalcedony at 13OOC (Truesdell, 1976). The quartz equilibrium temperatures at 150OC and the Na-K-Ca equilibrium temperatures at 230°C in Wilbur ffl are inferred to represent high initial water tanperature (230°C) and slow rate of water movement. Ultimately, little confidence can be placed in the temperatures estimated from the dissolved silica concentrations of the springs because of the numerous possible complications. In an attempt to calculate a third independent reservoir temperature, gas samples were collected and analyzed. Franco D'Amore and A. H. Truesdell (written communication, 1979) have devised a system of equations for geothermal steam wells which quantitatively relate the concentrations of CHi) and CO2 and of H2S and CO2 measured at the surface to the temperature in the producing zone. Using their equations the reservoir temperatures in Table 2 were calculated for Wilbur Hot Springs. These temperatures are in excellent agreement with the uncorrected Na-K-Ca tanperatures from the spring waters. Table 2.—Gas Analyses of Wilbur Hot Springs ^ Date 12-11- -77 Collect or AHT CO2 H2S NH3 H2 Ar 02 N2 CHi) C2H6 TOTAL T 51.2 2.66 0.622 9.36X 0.319 U.71 29.0 2.36 0.00 93.87 2120C Wilb ur Hot Springs 0-" 12-11-77 AHT 69-3 2.91 0.00 2.66x10" 0.217 1.26 18.8 3.33 0.00 95.85 237°C 8-15-78 JMT 76.7 2.92 , 0.0323 •^ 1.08x10 0.188 0.635 15.1 3.28 0.00 98.22 227 °c Ânalyses in mole percent. Analyses by Nancy L. Nehring, U.S. Geological Survey. The Wilbur Hot Springs water composition may result if one part diluting water such as that in Table 1 mixes with two or three parts of thennal water such as that from the Wilbur ffl geothermal well. This diluting water may be unusual because it contains a high magnesium content from dissolved serpentine. Alternatively, the magnesium from serpentine dissolution may not enter the system until after mixing. Another possible scheme is that 230°C water mixes with connate water similar to that described by White and others (1973) to form the J'ISOOC water in 731 Thompson Wilbur ffl geothermal well. This water then mixes with cold meteoric water in different proportions producing the various spring water compositions. This model Is not favored because it requires three different water types. Presently, the time at which the magnesium enters the system cannot be determined. The additional sulfate (115 mg/L) probably arises from oxidation of H2S in the near surface region. CONCLUSIONS The brine in the Wilbur ffl geothermal well result from the mixing of deep thennal water of unknown composition at a temperature near 230^0 and connate water such as that described by White and others (1973). Alternatively, the connate water may have been heated to near 230°C and then mixed with meteoric water in proportions of 2:1 or 3:1. This diluting meteoric water may contain as much as I80 mg/L Mg. This mixed v/ater may then slowly rise to the surface without appreciable residence in a large reservoir where Na-K-Ca reequilibratlon could occur. The depth to the 230°C water is unknown. REFERENCES journier, R. 0., 1979, Geochemical and hydrologic considerations and the use of enthalpy-chloride diagrams in the prediction of underground conditions in hot-spring systems: Journal of Volcanology and Geothermal Research, v. 5, - 1-I6. Fournier, R. 0., and Potter, R. W., II, 1978, A magnesium correction for the Na-K-Ca chemical geothermometer: U.S. Geological Survey Open-File Report 78-986, 2i| p. Fournier, R. 0., and Rowe, J. J., 1966, Estimation of underground temperatures from the silica content of water from hot springs and wet-steam wells: American Journal Science 261,- p. 685-697. • Fournier, R. 0., and Truesdell, A. H., 1973, An empirical Na-K-Ca geothermometer for natural water: Geochlmica et Cosmochimica Acta, 37, p. 1255-1275. Truesdell, 1976, Summary of Section III Geochemical and Geophysical Techniques in Exploration: Proceedings 2nd U. N. Symposium on the Development and use of Geothermal Resources, San Francisco, 19875, v. 1 p Ixxiii. Truesdell, A. H., and Fournier, R. 0., 1977, Procedure for estimating the temperature of hot-water component in a mexlco water by using a plot of dissolved silica versus enthalpy: Journal Reaearch U.S. Geological Survey, v. 5, p. 19-52. White, D. E., 1957, Magmatic, connate, and metamorphic waters: Geological Society of America Bulletin, v. 68(12) pt. 1, p. 1659-1682. White, D. E., Barnes, Ivan, and O'Neil, J. R., 1973, Thermal and mineral waters of nonmeteoric origin, California Coast Ranges: Geological Society of America Bulletin v. 81, p. 517-560.
Page 1: Geolêrtnal Resources Council, TRAN
Page 5 and 6: Morgan, et at. holes over the anoma
Page 7 and 8: Morgan, et al. point the gradient b
Page 9 and 10: Olson, et al of a theoretically gen
Page 11 and 12: Olson, et al Isherwood, W. F., 1977
Page 13 and 14: Sun and Ershaghi history matching p
Page 15 and 16: Sun and Ershaghi eg S o "^ lii z >o
Page 17 and 18: « •'t Lund. et. al. In general,
Page 19 and 20: Lund. et. al. FIGURE 3 Production F
Page 21 and 22: W.:-- Lund, et. al. Since the heat
Page 23 and 24: Lund, et. al, and temperature in th
Page 25 and 26: Lund. et. al. of the well with cont
Page 27 and 28: Lund, et, al. special heat resistan
Page 29 and 30: Lund, et. al. Ste«) in {«) Tunne\
Page 31 and 32: Lund, et al. 3. 4. References TABLE
Page 33 and 34: •Edmis-tjon period of time buried
Page 35 and 36: Edmiston VININI FM (SILICEOUS ASSEM
Page 37 and 38: Table I. Chemical analyses and calc
Page 39 and 40: Satkln et al. GEOTHERMOMETRY The te
Page 41 and 42: Denlinger We modeled the gravity da
Page 43 and 44: TABLE 3. RESULTS OF MODELING RESERV
Page 45 and 46: Knirsch Table 1. Continued Location
Page 47 and 48: Knirsch Spring/Well Edgemont Burlin
Page 50: Mariner et al. MomfflatI Min H>0^ 1
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Mariner et al. KjRiti/Locit Ion T:i
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Mariner et al. T.ibU' I. CftL'iBlr;
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Mariner et al. Table 2. CoioposltLo
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Mariner et. al. Table 3. Geotherrao
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Mariner et al. Table 3. Geotherraom
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Mariner et al. Table 5. Expected an
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Mariner et al. Table 6. Isotopic da
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Mariner et al. Table 6. Isotopic da
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Mariner et al. 9 K O Figure 10. 10
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Mariner, et al. hot springs and sha
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Mariner et al. Mariner, R. H., Pres
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BOREHOLE GEOPHYSICAL TECHHIQUES FOR
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Thick-Body Studies ^ Prior to 1982,
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J-. - (l.ti.od. Co' FIGURE 4c Downh
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' X • , methods; and, the anomali
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Geolhermal Resources Council TRANSA
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Figure 2. Index map of MCAGCC, Twen
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SMPERATURE GRADIENTS Temperature gr
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EOTHEFttVlAL RESERVOIR— FLUID TEM
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Geolhermal Resources Council TRANSA
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Geology ((aJMG) within the Napa Val
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^C Bomw of (tw VaAmf Figure 4. Tril
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Geolhermal Resources Council. TRANS
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Geophysical studies by Youngs and o
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feothermal aquifer into a zone of i
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INTRODUCTION Geothermal Resources C
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do not become isothermal or have ne
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the heat flow anomaly predicted fro
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INTRODUCTION In our experience, all
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The bo'rehDle" eiectricai, techniqu
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T1ie Cascades Region For the past t
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which is the rociprpGal pE resistiy
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of the .deefjer thermal regime .in
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Wright et al. vide basic data about
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training and experience in each of
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Thermai genesis of dissGlution cave
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JEWEL CAVE THERMAL GENESIS OF DISSO
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the Soviet Union), however, where K
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SiKiype THERMAL GENESIS OF DISSOLUT
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sed onto a longer term lowering are
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Ceothermal Resources Council RADON
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^H—^ ^ * I SAN IGNACtO O o V ' o
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GUTIERREZ-NEGRIN This geothermal zo
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GOSNOLD TEMPEiRAVURc (Doq. C) FIGUR
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GOSfJCLD bas(?raent. radioactivity
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GOSNOLD Sass, J.H., and Galanis, S.
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Corbaley and Oquita 50 sos+cr 4. -f
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Ctorbaley and Oquita "The combined
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JANIK ct al. Old Fort Road valley,
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JANIK et al. with a cold water at a
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JANIK et al. — Pilncipal hot-w«l
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DIRECT HEAT APPLICATION PROGRAM SUm
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TABLE OF CONTENTS Special Session A
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Special Session/Agenda (continued)
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DIRECT HEAT APPLICATION PROJECTS Th
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Institutional Heating Systems 1 Nav
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00 t Agribusiness 1 Utah Roses —
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DIRECT HEAT APPLICATIONS PROJECT DE
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Commercial Prawn Farm Project Page
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Boise City Project Page 2 Project D
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Project Title: City of El Centro Ge
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City of El Centro Project Page 3 St
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Elko Heat Company Project Page 2 Sy
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Philip School Project . Page 2 Proj
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Project Title: Geothermal Energy fo
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INJ EAST - WEST DIAGRAMMATIC CROSS
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.TO CC> ;i'iLjS^" •
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o EXISTING FACTORY A UNION aoiiER I
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Kelley Hot Springs Agricultural Cen
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Project Title: Klamath Falls YMCA 1
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Project Title: Klamath Falls Geothe
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Klamath Falls Project Page 3 Status
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Madison County Project Page 2 Statu
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Monroe City Project Page 2 Status:
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Navarro College and Memorial Hospit
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Ore-Ida Foods Project Page 2 A seis
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Pagosa Springs Geothermal Project P
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Moana KGRA Project Page 2 Fracture
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Project Title: Geothermal Applicati
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'4 ]^ W^^ '!-/..-'
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Project Title: Susanville Energy Pr
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Susanville Energy Project Page 3 Th
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] ^ ITffl^SSH '(gSPW-
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THS Memorial Hospital Project Page
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Utah Roses Project Page 2 Project D
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Utah State Prison Project Page 2 On
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Warm Springs State Hospital Project
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Appendix 1 (continued) Industrial P
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Appendix I (continued) Industrial P
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Appendix 1 (continued) industrial P
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^ Appendix 1 (continued) Industrial
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1. PROJECT SUMMARY - JUNE 1987 1.1
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1. k. 1. m. Name Date Nature Gib Co
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Name Date Nature m. Kevin Fisher 6/
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3. GEOTHERMAL PROGRESS MOMITOR 3.1
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g. If a new or amended Geothermal D
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Figure I Generalized map of the Wilbur Mining ... - University of Utah

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