Abstract
The dominant reaction determining the chemistry of fluids in a geothermal system of the New Zealand type consists of the conversion of primary plagioclase by CO/sub 2/ to calcite and clays with log P/sub CO/sub 2// = 15.26 - 7850/(t + 273.2), temperature t in /sup 0/C. Subsequent reactions involving secondary minerals control relative CO/sub 2/-H/sub 2/S-contents. The distribution of mineral phases throughout a geothermal system reflects the stepwise conversion of thermodynamically unstable primary phases through a series of intermediate, metastable phases to a thermodynamically stable, secondary assemblage. The relative stabilities of these phases was evaluated on the basis of their solubilities, the least soluble aluminium-silicate representing the thermodynamically most stable phase under a given set of conditions. Observed assemblages of secondary minerals in geothermal systems represent indicators allowing mineral/fluid-interaction conditions to be evaluated on the basis of multi-component mineral stability diagrams.
Citation Formats
Giggenbach, W F.
Geothermal mineral equilibria.
United Kingdom: N. p.,
1981.
Web.
doi:10.1016/0016-7037(81)90248-9.
Giggenbach, W F.
Geothermal mineral equilibria.
United Kingdom.
https://doi.org/10.1016/0016-7037(81)90248-9
Giggenbach, W F.
1981.
"Geothermal mineral equilibria."
United Kingdom.
https://doi.org/10.1016/0016-7037(81)90248-9.
@misc{etde_6658242,
title = {Geothermal mineral equilibria}
author = {Giggenbach, W F}
abstractNote = {The dominant reaction determining the chemistry of fluids in a geothermal system of the New Zealand type consists of the conversion of primary plagioclase by CO/sub 2/ to calcite and clays with log P/sub CO/sub 2// = 15.26 - 7850/(t + 273.2), temperature t in /sup 0/C. Subsequent reactions involving secondary minerals control relative CO/sub 2/-H/sub 2/S-contents. The distribution of mineral phases throughout a geothermal system reflects the stepwise conversion of thermodynamically unstable primary phases through a series of intermediate, metastable phases to a thermodynamically stable, secondary assemblage. The relative stabilities of these phases was evaluated on the basis of their solubilities, the least soluble aluminium-silicate representing the thermodynamically most stable phase under a given set of conditions. Observed assemblages of secondary minerals in geothermal systems represent indicators allowing mineral/fluid-interaction conditions to be evaluated on the basis of multi-component mineral stability diagrams.}
doi = {10.1016/0016-7037(81)90248-9}
journal = []
volume = {45:3}
journal type = {AC}
place = {United Kingdom}
year = {1981}
month = {Mar}
}
title = {Geothermal mineral equilibria}
author = {Giggenbach, W F}
abstractNote = {The dominant reaction determining the chemistry of fluids in a geothermal system of the New Zealand type consists of the conversion of primary plagioclase by CO/sub 2/ to calcite and clays with log P/sub CO/sub 2// = 15.26 - 7850/(t + 273.2), temperature t in /sup 0/C. Subsequent reactions involving secondary minerals control relative CO/sub 2/-H/sub 2/S-contents. The distribution of mineral phases throughout a geothermal system reflects the stepwise conversion of thermodynamically unstable primary phases through a series of intermediate, metastable phases to a thermodynamically stable, secondary assemblage. The relative stabilities of these phases was evaluated on the basis of their solubilities, the least soluble aluminium-silicate representing the thermodynamically most stable phase under a given set of conditions. Observed assemblages of secondary minerals in geothermal systems represent indicators allowing mineral/fluid-interaction conditions to be evaluated on the basis of multi-component mineral stability diagrams.}
doi = {10.1016/0016-7037(81)90248-9}
journal = []
volume = {45:3}
journal type = {AC}
place = {United Kingdom}
year = {1981}
month = {Mar}
}