δ³⁴S

Of the 25 known isotopes of sulfur, four are stable.^[1] In order of their abundance, those isotopes are ³²S (94.93%), ³⁴S (4.29%), ³³S (0.76%), and ³⁶S (0.02%).^[2] The δ³⁴S value refers to a measure of the ratio of the two most common stable sulfur isotopes, ³⁴S:³²S, as measured in a sample against that same ratio as measured in a known reference standard. The lowercase delta character is used by convention, to be consistent with use in other areas of stable isotope chemistry.^[3] That value can be calculated in per mil (‰, parts per thousand) as:^[4]

${\displaystyle \delta {\ce {^{34}S}}=\left({\frac {\left({\frac {{\ce {^{34}S}}}{{\ce {^{32}S}}}}\right)_{\mathrm {sample} }}{\left({\frac {{\ce {^{34}S}}}{{\ce {^{32}S}}}}\right)_{\mathrm {standard} }}}-1\right)\times 1000}$  ‰

Less commonly, if the appropriate isotope abundances are measured, similar formulae can be used to quantify ratio variations between ³³S and ³²S, and ³⁶S and ³²S, reported as δ³³S and δ³⁶S, respectively.^[5]

 

Sulfur from meteorites was determined in the early 1950s to be an adequate reference standard because it exhibited a small variability in isotopic ratios.^[6] It was also believed that because of their extraterrestrial provenances, meteors represented primordial terrestrial isotopic conditions.^[7] During a meeting of the National Science Foundation in April 1962, troilite from the Canyon Diablo meteorite found in Arizona, US, was established as the standard with which δ³⁴S values (and other sulfur stable isotopic ratios) could be calculated.^[6][8] Known as Canyon Diablo Troilite (CDT), the standard was established as having a ³²S:³⁴S ratio of 22.220 and was used for around three decades.^[6] In 1993, the International Atomic Energy Agency (IAEA) established a new standard, Vienna-CDT (VCDT), based on artificially prepared silver sulfide (IAEA-S-1) that was defined to have a δ³⁴S_VCDT value of −0.3‰.^[8] In 1994, the original CDT material was found not to be isotopically homogeneous, with internal variations as great as 0.4‰, confirming its unsuitability as a reference standard.^[6]

 

Two mechanisms of fractionation occur that alter sulfur stable isotope ratios: kinetic effects, especially due to the metabolism of sulfate-reducing bacteria, and isotope exchange reactions that occur between sulfide phases based on temperature.^[9] With VCDT as the reference standard, natural δ³⁴S value variations have been recorded between −72‰ and +147‰.^[10][11]

The presence of sulfate-reducing bacteria, which reduce sulfate (SO²⁻
₄) to hydrogen sulfide (H₂S), has played a significant role in the oceanic δ³⁴S value throughout the earth's history. Sulfate-reducing bacteria metabolize ³²S more readily than ³⁴S, resulting in an increase in the value of the δ³⁴S in the remaining sulfate in the seawater.^[7] Archean pyrite found in barite in the Warrawoona Group, Western Australia, with sulfur fractionations as great as 21.1‰ hint at the presence of sulfate-reducers as early as 3,470 million years ago.^[12]

It is now better known that the degree of isotope fractionation during microbial sulfate reduction depends on the cell-specific sulfate reduction rate of the sulfate-reducing microorganism.^[13][14] The relative extent of sulfur isotope fractionating activities, including sulfate reduction, sulfide reoxidation and disproportionation, determines the isotopic compositions of the minerals or fluid measured.^[15] Other than microbial activities and environmental conditions, isotopic compositions also change due to diffusion, accumulation and mixing after burial.^[16][17][15]

The δ³⁴S value, recorded by sulfate in marine evaporites, can be used to chart the sulfur cycle throughout earth's history.^[7][4] The Great Oxygenation Event around 2,400 million years ago altered the sulfur cycle radically, as increased atmospheric oxygen permitted an increase in the mechanisms that could fractionate sulfur isotopes, leading to an increase in the δ³⁴S value from ~0‰ pre-oxygenation. Approximately 700 million years ago, the δ³⁴S values in seawater sulfates began to vary more and those in sedimentary sulfates grew more negative. Researchers have interpreted this excursion as indicative of an increase in water column oxygenation with continued periods of anoxia in the deepest waters. Modern seawater sulfate δ³⁴S values are consistently 21.0 ± 0.2‰ across the world's oceans, while sedimentary sulfides vary widely. Seawater sulfate δ³⁴S and δ¹⁸O values exhibit similar trends not seen in sedimentary sulfide minerals.^[7]

• δ¹³C
• δ¹⁵N
• Isotopic signature
• Isotope analysis
• Isotope geochemistry

• Hoefs J (2009). Stable Isotope Geochemistry (6th ed.). Berlin: Springer-Verlag. doi:10.1007/978-3-540-70708-0. ISBN 978-3-540-70703-5.