Abstract
Hot spring deposits in the Roosevelt thermal area consist of opaline sinter and sinter-cemented alluvium. Alluvium, plutonic rocks, and amphibolite-facies gneiss have been altered by acid-sulfate water to alunite and opal at the surface, and alunite, kaolinite, montmorillonite, and muscovite to a depth of 70 m. Marcasite, pyrite, chlorite, and calcite occur below the water table at about 30 m. The thermal water is dilute (ionic strength 0.1 to 0.2) sodium-chloride brine. The spring water now contains 10 times as much Ca, 100 times as much Mg, and up to 2.5 times as much SO/sub 4/ as the deep water. Although the present day spring temperature is 25/sup 0/C, the temperature was 85/sup 0/C in 1950. A model for development of the observed alteration is supported by observation and irreversible mass transfer calculations. Hydrothermal fluid convectively rises along major fractures. Water cools by conduction and steam separation, and the pH rises due to carbon dioxide escape. At the surface, hydrogen and sulfate ions are produced by oxidation of H/sub 2/S. The low pH water percolates downward and reacts with feldspar in the rocks to produce alunite, kaolinite, montmorillonite, and muscovite as hydrogen ion is consumed. 4 figures, 4 tables.
Citation Formats
Parry, W T, Ballantyne, J M, Bryant, N L, and Dedolph, R E.
Geochemistry of hydrothermal alteration at the Roosevelt Hot Springs thermal area, Utah.
United Kingdom: N. p.,
1980.
Web.
doi:10.1016/0016-7037(80)90179-9.
Parry, W T, Ballantyne, J M, Bryant, N L, & Dedolph, R E.
Geochemistry of hydrothermal alteration at the Roosevelt Hot Springs thermal area, Utah.
United Kingdom.
https://doi.org/10.1016/0016-7037(80)90179-9
Parry, W T, Ballantyne, J M, Bryant, N L, and Dedolph, R E.
1980.
"Geochemistry of hydrothermal alteration at the Roosevelt Hot Springs thermal area, Utah."
United Kingdom.
https://doi.org/10.1016/0016-7037(80)90179-9.
@misc{etde_5578585,
title = {Geochemistry of hydrothermal alteration at the Roosevelt Hot Springs thermal area, Utah}
author = {Parry, W T, Ballantyne, J M, Bryant, N L, and Dedolph, R E}
abstractNote = {Hot spring deposits in the Roosevelt thermal area consist of opaline sinter and sinter-cemented alluvium. Alluvium, plutonic rocks, and amphibolite-facies gneiss have been altered by acid-sulfate water to alunite and opal at the surface, and alunite, kaolinite, montmorillonite, and muscovite to a depth of 70 m. Marcasite, pyrite, chlorite, and calcite occur below the water table at about 30 m. The thermal water is dilute (ionic strength 0.1 to 0.2) sodium-chloride brine. The spring water now contains 10 times as much Ca, 100 times as much Mg, and up to 2.5 times as much SO/sub 4/ as the deep water. Although the present day spring temperature is 25/sup 0/C, the temperature was 85/sup 0/C in 1950. A model for development of the observed alteration is supported by observation and irreversible mass transfer calculations. Hydrothermal fluid convectively rises along major fractures. Water cools by conduction and steam separation, and the pH rises due to carbon dioxide escape. At the surface, hydrogen and sulfate ions are produced by oxidation of H/sub 2/S. The low pH water percolates downward and reacts with feldspar in the rocks to produce alunite, kaolinite, montmorillonite, and muscovite as hydrogen ion is consumed. 4 figures, 4 tables.}
doi = {10.1016/0016-7037(80)90179-9}
journal = []
volume = {44:1}
journal type = {AC}
place = {United Kingdom}
year = {1980}
month = {Jan}
}
title = {Geochemistry of hydrothermal alteration at the Roosevelt Hot Springs thermal area, Utah}
author = {Parry, W T, Ballantyne, J M, Bryant, N L, and Dedolph, R E}
abstractNote = {Hot spring deposits in the Roosevelt thermal area consist of opaline sinter and sinter-cemented alluvium. Alluvium, plutonic rocks, and amphibolite-facies gneiss have been altered by acid-sulfate water to alunite and opal at the surface, and alunite, kaolinite, montmorillonite, and muscovite to a depth of 70 m. Marcasite, pyrite, chlorite, and calcite occur below the water table at about 30 m. The thermal water is dilute (ionic strength 0.1 to 0.2) sodium-chloride brine. The spring water now contains 10 times as much Ca, 100 times as much Mg, and up to 2.5 times as much SO/sub 4/ as the deep water. Although the present day spring temperature is 25/sup 0/C, the temperature was 85/sup 0/C in 1950. A model for development of the observed alteration is supported by observation and irreversible mass transfer calculations. Hydrothermal fluid convectively rises along major fractures. Water cools by conduction and steam separation, and the pH rises due to carbon dioxide escape. At the surface, hydrogen and sulfate ions are produced by oxidation of H/sub 2/S. The low pH water percolates downward and reacts with feldspar in the rocks to produce alunite, kaolinite, montmorillonite, and muscovite as hydrogen ion is consumed. 4 figures, 4 tables.}
doi = {10.1016/0016-7037(80)90179-9}
journal = []
volume = {44:1}
journal type = {AC}
place = {United Kingdom}
year = {1980}
month = {Jan}
}