Other
Scientific paper
Oct 1976
adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=1976gecoa..40.1229s&link_type=abstract
Geochimica et Cosmochimica Acta, vol. 40, Issue 10, pp.1229-1240
Other
89
Scientific paper
Hydrogen isotope fractionation factors between hydroxyl-bearing minerals and water were determined at temperatures ranging between 400 and 850°C. The hydrogen isotope exchange rates for the mineral-water pairs examined were very slow. In most cases it was necessary to use an interpolation method for the determination of the hydrogen isotope equilibrium fractionation factor, e . For the temperature range of 450-850°C the hydrogen isotope fractionation factors for the mica-water and amphibole-water systems are simply expressed as a function of temperature and the molar fractions of the six-fold coordinated cations in the crystal, regardless of mineral species, as follows: 10 3 In e ( mineral - water ) = - 22.4 (10 6 T -2 ) + 28.2 + (2 X Al - 4 X Mg - 68 X Fe ), where X is the molar fraction of the cations. As the equation indicates, for any specific composition of the OH-bearing minerals, the change of e with temperature, over the temperature range investigated, is the same for all minerals studied. Thus for any specified values of X Al , X Mg , and X Fe for these minerals, the relationship between e and T is 10 3 In e = T -2 + k . Consequently, hydrogen isotope fractionation among coexisting minerals is temperature independent and cannot be used as a hydrogen isotope geothermometer. Some exceptions to the above general observations exist for minerals such as boehmite and kaolinite. In these minerals hydrogen bonding modifies the equilibrium hydrogen isotopic fractionation between mineral and water.
Epstein Samuel
Suzuoki Tetsuro
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