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J. M. Thompson

Publications and source records attributed to J. M. Thompson.

34 records · Page 2Linked to original sources
USGS1983

SELECTED CHEMICAL ANALYSES AND GEOTHERMOMETRY OF HOT SPRING WATERS FROM THE CALABOZOS CALDERA, CENTRAL CHILE.

Hot springs discharging from the active hydrothermal system associated with the Calabozos caldera, Chile, have measured orifice temperatures as high as 98. 5 degree C and calculated geothermometer temperatures as high as 250 degree C. Three types of spring waters can be identified from the chemical analyses: a Na-Cl type, a Na-HCO//3 type and a Na-mixed anion type. Chloride-enthalpy relations indicate that the hydrothermal reservoir water may attain temperatures near 342 degree C and that most spring waters are mixed with cold meteoric water. Despite the proximity of Mesozoic marine gypsum deposits, the Cl/Br weight ratio of the Calabozos spring waters does not appear to indicate that these waters have a significant 'marine' signature. Refs.

Conference Paper↗
USGS1982

Evolution of geothermal fluids deduced from chemistry plots: Yellowstone National Park (U.S.A.)

Large amounts of chemical data, obtained in geothermal fields, may readily be sorted-out by the aid of a simple set of graphs that provide a clear over-all picture and facilitate the understanding of geochemical processes taking place. As a case study, data from several hundred samples of the thermal springs at the well-known Yellowstone National Park are discussed. The pattern obtained seems to indicate: (1) geochemical similarity between the spring groups of Heart Lake, Shoshone, Upper, Midway, Lower and Norris Geyser Basins, i.e., a geochemical uniformity of major spring groups located over 40 km apart; (2) these groups may be described as originating from a common fluid, most resembling the composition of Norris waters, accompanied by CO2, and other volatiles, that react with igneous rocks, forming local variations; (3) the secondary reactions occur at (medium) depth, before the ascent to the surface; (4) extensive concentration-dilution processes occur during the ascent to the surface. The water of the Mammoth group may be described as originating from the same Norris-like fluid that has been diluted (low Na and Cl contents) and intensively reacted with carbonaceous rocks, thus gaining in Ca, Mg, SO4, and HCO3. ?? 1982.

Journal of Volcanology and Geothermal Research↗
USGS1981

The origin of the Cerro Prieto geothermal brine

The Cerro Prieto geothermal brine may have originated from mixing of Colorado River water with seawater evaporated to about six times its normal salinity. This mixture circulated deeply and was heated by magmatic processes. During deep circulation, Li, K, Ca, B, SiO 2 and rare alkalis were transferred from rock minerals to the water, and Mg, SO 4 , and a minor quantity of Na were transferred to the rock. Similar alteration of seawater salt chemistry has been observed in coastal geothermal systems and produced in laboratory experiments. After heating and alteration the brine was further diluted to its present range of composition. Oxygen isotopes in the fluid are in equilibrium with reservoir calcite and have been affected by exploitation-induced boiling and dilution.

Geothermics↗
USGS1979

Arsenic and fluoride in the upper madison river system: Firehole and gibbon rivers and their tributaries, yellowstone national park, wyoming, and southeast montana

Chemical analyses of 21 water samples from the Firehole and Gibbon Rivers, which combine to form the Madison River, gave arsenic and fluoride values above the Environmental Protection Agency Interim Primary Drinking Water maximum contaminant levels (0.05 mg/l arsenic and 2.0 mg/l fluoride). On 18 October, 1975, during a period of moderate flow (16,600 l/s), the Madison River at West Yellowstone contained 0.23 mg/l arsenic and 6.2 mg/l fluoride. Below Hebgen Lake the Madison River during periods of high flow (56,000 liter/s at West Yellowstone and 708,000 liter/s below Hebgen Lake) would contain 0.05 mg/l arsenic at both stations and 1.5 and 4.0 mg/l fluoride at West Yellowstone and below Hebgen Lake, respectively. The strong correlations of arsenic and fluoride with other chemical constituents of the river water at the sampling sites demonstrate the conservative nature of each element after it reaches the Madison River system. Calculations indicate that water from three sampling sites is above saturation with respect to fluorite. ?? 1979 Springer-Verlag New York Inc.

Environmental Geology↗
USGS1979

Chemical composition of water and gas from five nearshore subaqueous springs in Clear Lake, Northern California

In 1971 The Geysers-Clear Lake area was selected by the U.S. Geological Survey geothermal research program as a region for extensive investigation. Under this program thermal water samples were first collected in December, 1974 during a winter of normal rainfall; the last samples were collected in February, 1977 during a period of drought. The drought exposed many springs which normally are submerged by Clear Lake. The collection and analysis of these springs is reported in Thompson and others (this vol.).

California↗
USGS1979

Chemical analyses of waters from geysers, hot springs, and pools in Yellowstone National Park, Wyoming, from 1974 to 1978

Waters from geysers, hot springs, and pools of Yellowstone National Park have been analyzed by numerous investigators extending back nearly ten decades. Large compilations of complete major ion analyses of the thermal waters have been reported by Gooch and Whitfield (1888) 38 analyses; Allen and Day (1935) 94 complete and 127 partial major ion analyses, Rowe and others (1973) 166 analyses including many previous chemical analyses of the same feature; and Thompson and others (1975) 242 complete and 299 partial major ion analyses. Smaller compilations of the thermal water chemistry have been reported by Douglass (1939) 12 analyses; White and others (1963) 6 analyses; and Scott (1964) 10 analyses. Partial chemical analyses have been reported by White and others (1956) and by Morey and others (1961) for dissolved silica; Noguichi and Nix (1963) for dissolved silica and major anions; Araki and Noguichi (1969) for dissolved silica, molybdenum, vanadium, and major anions. Here we report 422 complete major ion analyses from 330 different locations of geysers, hot springs, and pools, collected from 1974 to 1978. Many of the analyses from Upper, Midway, Lower, and Norris Geyser Basin are recollections of features previously reported.

Wyoming↗
USGS1978

Determination of dissolved boron in fresh, estuarine, and geothermal waters by d.c. argon-plasma emission spectrometry

A d.c. argon-plasma emission spectrometer is used to determine dissolved boron in natural (fresh and estuarine) water samples. Concentrations ranged from 0.02 to 250 mg l -1 . The emission—concentration function is linear from 0.02 to 1000 mg l -1 . Achievement of a relative standard deviation of ⩽ 3% requires frequent restandardization to offset sensitivity changes. Dilution may be necessary to overcome high and variable electron density caused by differences in alkali-metal content and to avoid quenching of the plasma by high solute concentrations of sodium and other easily ionized elements. The proposed method was tested against a reference method and found to be more sensitive, equally or more precise and accurate, less subject to interferences, with a wider linear analytical range than the carmine method. Analyses of standard reference samples yielded results in all cases within one standard deviation of the means.

Analytica Chimica Acta↗
USGS1978

Phosphorus in hydrothermal waters of Yellowstone National Park, Wyoming

Ninety-seven hot-spring and geyser samples (field acidified to pH<1.4 with HCl or HNO 3 ) from Yellowstone National Park, Wyo., were analyzed for PO 4 -P using reduced molybdenum-blue and the selective arsenate reducing agent, metabisulfite-thiosulfate. The PO 4 -P concentrations ranged from below detection limit (~1-73 micrograms per liter). Twenty-five springs had PO 4 -P concentrations exceeding 6.8 &mu; g/L; seven spring samples exceeded 20 &mu;g/L. Elevated PO 4 -P contents were invariably associated with mixed springs, as evidenced by diluted chloride concentrations and, commonly, subboiling temperatures, low pH's, and elevated calcium concentrations. Alkaline high-chloride (>400 milligrams per liter) hydrothermal waters from Upper and Norris Geyser Basins had PO 4 -P concentrations below 2 &mu;g/L and represent the low end of the range of PO 4 -P contents in natural waters.

Wyoming↗
USGS1975

Chemical analysis of the waters of the Yellowstone National Park, Wyoming from 1965 to 1973

Analyses of Yellowstone Park thermal waters have been reported by many investigators extending back almost one hundred years. The first detailed analyses were reported by Gooch and Whitfield (1888). Allen and Day (1935) were second. White, Brannock, and Murata (1956) and Morey, Fournier, Hemley, and Rowe (1961) reported field analyses of dissolved silica content of hot springs. White, Hem, and Waring (1963) reported six new chemical analyses. Noguchi and Nix (1963) reported partial analyses of five geysers. Rowe, Fournier, and Morey (1973) published the analyses of 166 samples from 89 different locations and the previous analyses of the same hot springs and geysers from 1888 to their study. The analyses compiled here are from 541 samples from 405 different locations of streams, rivers, cold springs, warm springs, hot springs, pools, and geysers. We are indebted to many colleagues at the Survey who have contributed to this report. These include Manuel Nathenson for his help in writing the computer program, E. E. Bell and H. S. Cortez for coding the analyses, R. O. Fournier, L. P. J. Muffler, A. H. Truesdell, and D. E. White for collecting and locating the water samples. We are also grateful to the U. S. National Park Service for their cooperation and assistance.

Wyoming↗