Sulfur isotopic fractionation among sphalerite, galena and sulfide ions

Sulfur Isotope Geochemistry of Sulfide Minerals

“…Ohmoto and Rye (1979) reviewed and critically evaluated the available experimental sulfur isotope fractionation data relative to H 2 S, which included temperaturedependent fractionation factors for sulfi tes, SO 2 , H 2 S gas, HS − , S 2− , and S, and the minerals pyrite (FeS 2 ), sphalerite (ZnS), pyrrhotite (Fe 1−x S), chalcopyrite (CuFeS 2 ), and galena (PbS). Their evaluation and compilation included experimental studies by Grootenboer and Schwarz (1969), Schiller et al (1969), Grinenko and Thode (1970), Kajiwara and Krouse (1971), Salomons (1971), , Kiyosu (1973), Robinson (1973), and Czamanske and Rye (1974), and estimates following Sakai (1968) and Bachinski (1969). Ohmoto and Lasaga (1982) re-evaluated experimental studies investigating sulfur-isotope fractionations between aqueous sulfate and sulfi de (Robinson 1973;Bahr 1976;Igumnov et al 1977;Sakai and Dickson 1978) and presented a revised equation describing SO 4 2− -H 2 S sulfur-isotope fractionation as a function of temperature.…”

Calculation of sulfur isotope fractionation in sulfides

“…Experimental measurements of sulfur isotopic fractionations among sulfides had been carried out by many researchers (Grootenboer and Schwarcz, 1969;Kajiwara et al, 1969;Rye and Czamanske, 1969;Schiller et al, 1970;Kajiwara and Krouse, 1971;Salomons, 1971;Kiyosu, 1973;Czamanske and Rye, 1974;Smith et al, 1977;Hubberten, 1980). Most of these studies have dealt with PbS, ZnS, FeS, FeS s , and CuFeS 2 .…”

Multiple sulfur isotope fractionation and mass transfer processes during pyrite precipitation and recrystallization: An experimental study at 300 and 350 °C

“…The S isotopic composition of starting native sulfur is 9.7, 18.8, and 0.038‰ for δ 33 S, 315 δ 34 S, and Δ 33 S, respectively, while the terminal S isotopic composition of the pyrite crystals used 316 for the exchange experiments ranged from -0.8 to 6.7, -1.5 to 13.1, and -0.068 to 0.002‰ for 317 δ 33 S, δ 34 S, and Δ 33 S, respectively ( [Czamanske and Rye, 1974;Kajiwara and Krouse, 1971;Kajiwara et 412 al., 1969;Robinson, 1973;Sakai and Dickson, 1978;Uyama et al, 1985]. A few experimental 413 studies [Kiyosu, 1973;Nakai, 1970] serve as an independent means of tracing equilibration of the mineral-fluid system (Fig. 7) …”