Reactions of oxidation of sulfide to sulfate and elemental sulfur (incorrectly balanced). The electrons (e−) liberated from these oxidation reactions, which release chemical energy, are then used to fix carbon into organic molecules. The elements that become oxidized are shown in pink, those that become reduced in blue, and the electrons in purple.

Microbial oxidation of sulfur is the oxidation of sulfur by microorganisms to build their structural components. The oxidation of inorganic compounds is the strategy primarily used by chemolithotrophic microorganisms to obtain energy to survive, grow and reproduce. Some inorganic forms of reduced sulfur, mainly sulfide (H2S/HS−) and elemental sulfur (S0), can be oxidized by chemolithotrophic sulfur-oxidizing prokaryotes, usually coupled to the reduction of oxygen (O2) or nitrate (NO3−).[1][2] Anaerobic sulfur oxidizers include photolithoautotrophs that obtain their energy from sunlight, hydrogen from sulfide, and carbon from carbon dioxide (CO2).

Most of the sulfur oxidizers are autotrophs that can use reduced sulfur species as electron donors for CO2 fixation. The microbial oxidation of sulfur is an important link in the biogeochemical cycling of sulfur in environments hosting both abundant reduced sulfur species and low concentrations of oxygen, such as marine sediments, oxygen minimum zones (OMZs) and hydrothermal systems.[3]

Ecology

The oxidation of hydrogen sulfide has been considered one of the most important processes in the environment, given that the oceans have had very low oxygen and high sulfidic conditions over most of the Earth's history. The modern analog ecosystems are deep marine basins, for instance in the Black Sea, near the Cariaco trench and the Santa Barbara basin. Other zones of the ocean that experience periodic anoxic and sulfidic conditions are the upwelling zones off the coasts of Chile and Namibia, and hydrothermal vents, which are a key source of H2S to the ocean.[4] Sulfur oxidizing microorganisms (SOM) are thus restricted to upper sediment layers in these environments, where oxygen and nitrate are available. The SOM may play an important yet unconsidered role in carbon sequestration,[5] since some models[6] and experiments with Gammaproteobacteria[7][8] have suggested that sulfur-dependent carbon fixation in marine sediments could be responsible for almost half of total dark carbon fixation in the oceans. Besides, they may have been critical for the evolution of eukaryotic organisms, given that sulfur metabolism could have driven the formation of the symbiotic associations that sustained them[9] (see below).

Although the biological oxidation of reduced sulfur compounds competes with abiotic chemical reactions (e.g. the iron-mediated oxidation of sulfide to iron sulfide (FeS) or pyrite (FeS2)),[10] thermodynamic and kinetic considerations suggest that biological oxidation far exceeds the chemical oxidation of sulfide in most environments.[4] Experimental data from the anaerobic phototroph Chlorobaculum tepidum indicate that microorganisms enhance sulfide oxidation by three or more orders of magnitude.[4] However, the general contribution of microorganisms to total sulfur oxidation in marine sediments is still unknown. The SOM of Alphaproteobacteria, Gammaproteobacteria and Campylobacterota account for average cell abundances of 108 cells/m3 in organic-rich marine sediments.[11] Considering that these organisms have a very narrow range of habitats, as explained below, a major fraction of sulfur oxidation in many marine sediments may be accounted for by these groups.[12]

Given that the maximal concentrations of oxygen, nitrate and sulfide are usually separated in depth profiles, many SOM cannot directly access their hydrogen or electron sources (reduced sulfur species) and energy sources (O2 or nitrate) at the same time. This limitation has led SOM to develop different morphological adaptations.[12] The large sulfur bacteria (LSB) of the family Beggiatoaceae (Gammaproteobacteria) have been used as model organisms for benthic sulfur oxidation. They are known as 'gradient organisms' that are indicative of hypoxic (low oxygen) and sulfidic (rich in reduced sulfur species) conditions. They internally store large amounts of nitrate and elemental sulfur to overcome the spatial gap between oxygen and sulfide. Some of the Beggiatoaceae are filamentous and can thus glide between oxic/suboxic and sulfidic environments, while the non-motile ones rely on nutrient suspensions, fluxes, or attach themselves to bigger particles.[12] Some marine non-motile LSB are the only known free-living bacteria that have two carbon fixation pathways: the Calvin-Benson cycle (used by plants and other photosynthetic organisms) and the reverse tricarboxylic acid cycle.[13]

Another evolutionary strategy of SOM is to partner up with motile eukaryotic organisms. The symbiotic SOM provides carbon and, in some cases, bioavailable nitrogen to the host, and gets enhanced access to resources and shelter in return. This lifestyle has evolved independently in sediment-dwelling ciliates, oligochaetes, nematodes, flatworms and bivalves.[14] Recently, a new mechanism for sulfur oxidation was discovered in filamentous bacteria. It is called electrogenic sulfur oxidation (e-SOx), and involves the formation of multicellular bridges that connect the oxidation of sulfide in anoxic sediment layers with the reduction of oxygen or nitrate in oxic surface sediments, generating electric currents over centimeter distances. The so-called cable bacteria are widespread in shallow marine sediments,[15] and are believed to conduct electrons through structures inside a common periplasm of the multicellular filament,[16] a process that may influence the cycling of elements at aquatic sediment surfaces, for instance, by altering iron speciation.[17] The LSB and cable bacteria seem to be restricted to undisturbed sediment with stable hydrodynamic conditions,[18] while symbiotic SOM and their hosts have been mainly found in permeable coastal sediments.[12]

Microbial diversity

The oxidation of reduced sulfur compounds is performed exclusively by Bacteria and Archaea. All the Archaea involved in this process are aerobic and belong to the Order Sulfolobales,[19][20] characterized by acidophiles (extremophiles that require low pHs to grow) and thermophiles (extremophiles that require high temperatures to grow). The most studied have been the genera Sulfolobus, an aerobic Archaea, and Acidianus, a facultative anaerobe (i.e. an organism that can obtain energy either by aerobic or anaerobic respiration).

Sulfur oxidizing bacteria (SOB) are aerobic, anaerobic or facultative, and most of them are obligate or facultative autotrophs that can use either carbon dioxide or organic compounds as a source of carbon (mixotrophs).[3] The most abundant and studied SOB are in the family Thiobacilliaceae in terrestrial environments, and in the family Beggiatoaceae in aquatic environments.[3] Aerobic sulfur oxidizing bacteria are mainly mesophilic, growing at moderate ranges of temperature and pH, although some are thermophilic and/or acidophilic. Outside these families, other SOB described belong to the genera Acidithiobacillus,[21] Aquaspirillum,[22] Aquifex,[23] Bacillus,[24] Methylobacterium,[25] Paracoccus, Pseudomonas [22] Starkeya,[26] Thermithiobacillus,[21] and Xanthobacter.[22] On the other hand, the cable bacteria belong to the family Desulfobulbaceae of the Deltaproteobacteria and are currently represented by two candidate Genera, "Candidatus Electronema" and "Candidatus Electrothrix"[27].

Anaerobic SOB (AnSOB) are mainly neutrophilic/mesophilic photosynthetic autotrophs, obtaining energy from sunlight but using reduced sulfur compounds instead of water as hydrogen or electron donors for photosynthesis. AnSOB include some purple sulfur bacteria (Chromatiaceae)[28] such as Allochromatium,[29] and green sulfur bacteria (Chlorobiaceae), as well as the purple non-sulfur bacteria (Rhodospirillaceae)[30] and some Cyanobacteria.[3] The AnSOB Cyanobacteria are only able to oxidize sulfide to elemental sulfur and have been identified as Oscillatoria, Lyngbya, Aphanotece, Microcoleus, and Phormidium.[31][32] Some AnSOB, such as the facultative anaerobes Thiobacillus spp., and Thermothrix sp., are chemolithoautotrophs, meaning that they obtain energy from the oxidation of reduced sulfur species, which is then used to fix CO2. Others, such as some filamentous gliding green bacteria (Chloroflexaceae), are mixotrophs. From all of the SOB, the only group that directly oxidize sulfide to sulfate in abundance of oxygen without accumulating elemental sulfur are the Thiobacilli. The other groups accumulate elemental sulfur, which they may oxidize to sulfate when sulfide is limited or depleted.[3]

Biochemistry

Enzymatic pathways used by sulfide-oxidizing microorganisms. Left: SQR pathway. Right: Sox pathway. HS−: sulfide; S0: elemental sulfur; SO32-: sulfite; APS: adenosine-5'-phosphosulfate; SO42-: sulfate. Redrawn (adapted) with permission from Poser, A., Vogt, C., Knöller, K., Ahlheim, J., Weiss, H., Kleinsteuber, S., & Richnow, H. H. (2014). Stable sulfur and oxygen isotope fractionation of anoxic sulfide oxidation by two different enzymatic pathways. Environmental Science & Technology, 48(16), 9094–9102. Copyright 2008 American Chemical Society.

There are two described pathways for the microbial oxidation of sulfide:

Similarly, two pathways for the oxidation of sulfite (SO32-) have been identified:

On the other hand, at least three pathways exist for the oxidation of thiosulfate (S2O32-) :

In any of these pathways, oxygen is the preferred electron acceptor, but in oxygen-limited environments nitrate, oxidized forms of iron and even organic matter are used instead.[44]

Cyanobacteria normally perform oxygenic photosynthesis using water as electron donor. However, in the presence of sulfide, oxygenic photosynthesis is inhibited, and some cyanobacteria can perform anoxygenic photosynthesis by oxidation of sulfide to thiosulfate − using Photosystem I with sulfite− as a possible intermediate sulfur compound.[45][46]

Oxidation of sulfide

Sulfide oxidation can proceed under aerobic or anaerobic conditions. Aerobic sulfide-oxidizing bacteria usually oxidize sulfide to sulfate and are obligate or facultative chemolithoautotrophs. The latter can grow as heterotrophs, obtaining carbon from organic sources, or as autotrophs, using sulfide as the electron donor (energy source) for CO2 fixation.[3] The oxidation of sulfide can proceed aerobically by two different mechanisms: substrate-level phosphorylation, which is dependent on adenosine monophosphate (AMP), and oxidative phosphorylation independent of AMP,[47] which has been detected in several Thiobacilli (T. denitrificans, T. thioparus, T. novellus and T. neapolitanus), as well as in Acidithiobacillus ferrooxidans.[48] The archaeon Acidianus ambivalens appears to possess both an ADP-dependent and an ADP independent pathway for the oxidation of sulfide.[49] Similarly, both mechanisms operate in the chemoautotroph Thiobacillus denitrificans,[50] which can oxidize sulfide to sulfate anaerobically using nitrate as terminal electron acceptor [51] which is reduced to dinitrogen (N2).[52] Two other anaerobic strains that can perform a similar process were identified as similar to Thiomicrospira denitrificans and Arcobacter.[53]

Among the heterotrophic SOB are included species of Beggiatoa that can grow mixotrophically, using sulfide to obtain energy (autotrophic metabolism) or to eliminate metabolically formed hydrogen peroxide in the absence of catalase (heterotrophic metabolism).[54] Other organisms, such as the Bacteria Sphaerotilus natans [55] and the yeast Alternaria [56] are able to oxidize sulfide to elemental sulfur by means of the rDsr pathway.[57]

Oxidation of elemental sulfur

Some Bacteria and Archaea can aerobically oxidize elemental sulfur to sulfuric acid.[3] Acidithiobacillus ferrooxidans and Thiobacillus thioparus can oxidize sulfur to sulfite by means of an oxygenase enzyme, although it is thought that an oxidase could be used as well as an energy saving mechanism.[58] For the anaerobic oxidation of elemental sulfur, it is thought that the Sox pathway plays an important role, although this is not yet completely understood.[39] Thiobacillus denitrificans uses oxidized forms on nitrogen as energy source and terminal electron acceptor instead of oxygen.[59]

Oxidation of thiosulfate and tetrathionate

Most of the chemosynthetic autotrophic bacteria that can oxidize elemental sulfur to sulfate are also able to oxidize thiosulfate to sulfate as a source of reducing power for carbon dioxide assimilation. However, the mechanisms that they utilize may vary, since some of them, such as the photosynthetic purple bacteria, transiently accumulate extracellular elemental sulfur during the oxidation of tetrathionate before oxidizing it to sulfate, while the green sulfur bacteria do not.[3] A direct oxidation reaction (T. versutus [60]), as well as others that involve sulfite (T. denitrificans) and tetrathionate (A. ferrooxidans, A. thiooxidans and Acidiphilum acidophilum [61]) as intermediate compounds, have been proposed. Some mixotrophic bacteria only oxidize thiosulfate to tetrathionate.[3]

The mechanism of bacterial oxidation of tetrathionate is still unclear and may involve sulfur disproportionation, during which both sulfide and sulfate are produced from reduced sulfur species, and hydrolysis reactions.[3]

Isotope fractionations

The fractionation of sulfur and oxygen isotopes during microbial sulfide oxidation (MSO) has been studied to assess its potential as a proxy to differentiate it from the abiotic oxidation of sulfur.[62] The light isotopes of the elements that are most commonly found in organic molecules, such as 12C, 16O, 1H, 14N and 32S, form bonds that are broken slightly more easily than bonds between the corresponding heavy isotopes, 13C, 18O, 2H, 15N and 34S . Because there is a lower energetic cost associated with the use of light isotopes, enzymatic processes usually discriminate against the heavy isotopes, and, as a consequence, biological fractionations of isotopes are expected between the reactants and the products. A normal kinetic isotope effect is that in which the products are depleted in the heavy isotope relative to the reactants (low heavy isotope to light isotope ratio), and although this is not always the case, the study of isotope fractionations between enzymatic processes may allow tracing the source of the product.

Fractionation of oxygen isotopes

The formation of sulfate in aerobic conditions entails the incorporation of four oxygen atoms from water, and when coupled with dissimilatory nitrate reduction (DNR) -the preferential reduction pathway under anoxic conditions- can have a contribution of oxygen atoms from nitrate as well. The δ18O value of the newly formed sulfate thus depends on the δ18O value of the water, the isotopic fractionation associated with the incorporation of oxygen atoms from water to sulfate and a potential exchange of oxygen atoms between sulfur and nitrogen intermediates and water.[63] MSO has been found to produce small fractionations in 18O compared to water (~5‰). Given the very small fractionation of 18O that usually accompanies MSO, the relatively higher depletions in 18O of the sulfate produced by MSO coupled to DNR (-1.8 to -8.5 ‰) suggest a kinetic isotope effect in the incorporation of oxygen from water to sulfate and the role of nitrate as a potential alternative source of light oxygen.[63] The fractionations of oxygen produced by sulfur disproportionation from elemental sulfur have been found to be higher, with reported values from 8 to 18.4‰, which suggests a kinetic isotope effect in the pathways involved in oxidation of elemental sulfur to sulfate, although more studies are necessary to determine what are the specific steps and conditions that favor this fractionation. The table below summarizes the reported fractionations of oxygen isotopes from MSO in different organisms and conditions.

Starting compound (reactant) Intermediate or end compounds
(products) 		Organism Average 18O fractionation (product/reactant) Details Reference
Sulfide Sulfate A. ferrooxidans (chemolithotroph) 4.1‰ (30 °C) Aerobic Taylor et al. (1984)[64]
A. ferrooxidans (chemolithotroph) 6.4‰
3.8‰

(no temperature provided)

Aerobic

Anaerobic

Thurston et al. (2010)[65]
Thiomicrospira sp. strain CVO (chemolithotroph) 0‰

(no temperature provided)

Anaerobic, coupled to DNR Hubert et al. (2009)[66]
T. denitrificans (chemolithotroph)
Sulfurimonas denitrificans

(chemolithotroph)

−6 to −1.8‰ (30 °C)


−8.5 to −2.1‰ (21 °C)

Anaerobic, coupled to DNR, SQR pathway
Anaerobic, coupled to DNR, Sox pathway 		Poser et al. (2014)[63]
Elemental sulfur Sulfate Desulfocapsa thiozymogenes

(chemolithotroph; "cable bacteria")

Enrichment culture

11.0 to 18.4‰ (28 °C)

12.7 to 17.9‰ (28 °C)

Disproportionation, in the presence of iron scavengers Böttcher et al. (2001)[67]
Desulfocapsa thiozymogenes

(chemolithotroph; "cable bacteria") Enrichment culture

8 to 12 ‰ (28 °C) Disproportionation, attenuated isotope effect due to reoxidation by manganese oxides Böttcher & Thamdrup (2001)[68]

Fractionation of sulfur isotopes

Aerobic MSO generates depletions in the 34S of sulfate that have been found to be as small as −1.5‰ and as large as -18‰. For most microorganisms and oxidation conditions, only small fractionations accompany either the aerobic or anaerobic oxidation of sulfide, elemental sulfur, thiosulfate and sulfite to elemental sulfur or sulfate. The phototrophic oxidation of sulfide to thiosulfate under anoxic conditions also generates negligible fractionations. Although the change in sulfur isotopes is usually small during MSO, MSO oxidizes reduced forms of sulfur which are usually depleted in 34S compared to seawater sulfate. Therefore large-scale MSO can also significantly change the sulfur isotopes of a reservoir. It has been proposed that the observed global average S-isotope fractionation is around −50‰ instead of the theoretically predicted value -70‰ because of MSO.[69]

In the chemolithotrophs Thiobacillus denitrificans and Sulfurimonas denitrificans, MSO coupled to DNR has the effect of inducing the SQR and Sox pathways, respectively. In both cases, a small fractionation in the 34S of the sulfate, lower than -4.3‰, has been measured. Sulfate depletion in 34S from MSO could be used to trace sulfide oxidation processes in the environment, although it does not allow a discrimination between the SQR and Sox pathways.[63] The depletion produced by MSO coupled to DNR is similar to up to -5‰ depletion estimated for the 34S in the sulfide produced from rDsr.[70][71] In contrast, disproportionation under anaerobic conditions generates sulfate enriched in 34S up to 9‰ and ~34‰ from sulfide and elemental sulfur, respectively. The isotope effect of disproportionation is however limited by the rates of sulfate reduction and MSO.[72] Just like the fractionation of oxygen isotopes, the larger fractionations in sulfate from the disproportionation of elemental sulfur point to a key step or pathway critical for inducing this large kinetic isotope effect. The table below summarizes the reported fractionations of sulfur isotopes from MSO in different organisms and conditions.

Starting compound (reactant) Intermediate or end compounds
(products) 		Organism Average 34S fractionation

(product/reactant)

Details Oxidant Reference
Sulfide Sulfate T. neopolitanus, T. intermedius and T. ferrooxidans (chemolithotrophs) -2 to -5.5‰

(no temperature provided)

Aerobic
pH 5 to 6 		Carbon dioxide Toran (1986)[73]
Polythionates (SnO62-)
Elemental sulfur
Sulfate 		T. concretivorus (chemolithotroph) 0.6 to 19‰ (30 °C)
-2.5 to 1.2‰ (30 °C)
-18 to -10.5‰ (30 °C) 		Aerobic Carbon dioxide Kaplan & Rittenberg (1964)[74]
Sulfate A. ferrooxidans (chemolithotroph) −1.5‰
−4‰

(no temperature provided)

Aerobic

Anaerobic

Carbon dioxide Thurston et al. (2010)[65]
Sulfate T. denitrificans (chemolithotroph)
Sulfurimonas denitrificans (chemolithotroph) 		−4.3 to −1.3‰ (30 °C)

−2.9 to −1.6‰ (28 °C)

Anaerobic, coupled to DNR, SQR pathway
Anaerobic, coupled to DNR, Sox pathway 		Carbon dioxide Poser et al. (2014)[63]
Sulfate Thiomicrospira sp. strain CVO

(chemolithotroph)

1‰ (no temperature provided) Anaerobic, coupled to DNR, no intermediates in complete oxidation of sulfide to sulfate (potentially only uses Sox pathway) Carbon dioxide Hubert et al. (2009)[66]
Elemental sulfur Chlorobium thiosulphatophilum
(green sulfur bacteria) 		5‰ (no temperature provided) Anaerobic Carbon dioxide Kelly et al. (1979)[75]
Thiosulfate Oscillatoria sp. (Cyanobacteria)

Calothrix sp. (Cyanobacteria)

0‰ (30 °C) Anaerobic, anoxygenic photosynthesis Carbon dioxide Habicht et al.(1988)[76]
Elemental sulfur

Sulfate

Chromatium vinosum (purple sulfur bacteria) 0‰ (30-35 °C)

2‰ (30-35 °C)

Anaerobic, anoxygenic photosynthesis Fry et al. (1985)[77]
Elemental sulfur

Sulfate

Ectothiorhodospira shaposhnikovii (purple sulfur bacteria) ±5‰ (no temperature provided) Anaerobic, anoxygenic photosynthesis Ivanov et al. (1976)[78]
Polythionates (SnO62-)
Elemental sulfur
Sulfate 		Chromatium sp. (purple sulfur bacteria) 4.9 to 11.2‰ (30 °C)
-10 to -3.6‰ (30 °C)
-2.9 to -0.9‰ (30 °C) 		Anaerobic Kaplan & Rittenberg (1964)[74]
Thiosulfate Sulfate T. intermedius (chemolithotroph) -4.7‰ (no temperature provided) Aerobic Kelly et al. (1979)[75]
Sulfate T. versutus (chemolithotroph) 0‰ (28 °C) Aerobic Fry et al. (1986)[79]
Elemental sulfur + Sulfate Chromatium vinosum (purple sulfur bacteria) 0‰ (30-35 °C) Anaerobic Fry et al. (1985)[77]
Sulfate Desulfovibrio sulfodismutans

(chemolithotroph)

D. thiozymogenes (chemolithotroph; "cable bacteria")

For both bacteria:

0‰ (30 °C; compared to the sulfonate functional group); 2 to 4‰ (30 °C; compared to the sulfane functional group)

Anaerobic, disproportionation Habicht et al.(1988)[76]
Elemental sulfur Sulfate Desulfocapsa thiozymogenes

(chemolithotroph; "cable bacteria")

Enrichment culture

17.4‰ (28 °C)

16.6‰ (28 °C)

Anaerobic, disproportionation, in the presence of iron scavengers Böttcher et al. (2001)[67]
Desulfocapsa sulfoexigens

Desulfocapsa thiozymogenes

(chemolithotrophs; "cable bacteria")

Desulfobulbus propionicus (chemoorganotroph)

Marine enrichments and sediments

16.4‰ (30 °C)

17.4‰ (30 °C)

33.9‰ (35 °C)

17.1 to 20.6‰ (28 °C)

Anaerobic, disproportionation Canfield et al. (1998)[80]
Desulfocapsa thiozymogenes

(chemolithotroph; "cable bacteria")

Enrichment culture

−0.6 to 2.0‰ (28 °C)

−0.2 to 1.1‰ (28 °C)

Anaerobic, disproportionation, attenuated isotope effect due to reoxidation by manganese oxides Böttcher & Thamdrup (2001)[68]
Sulfite Sulfate Desulfovibrio sulfodismutans

(chemolithotroph)

D. thiozymogenes

(chemolithotroph; "cable bacteria")

9 to 12‰ (30 °C)

7 to 9‰ (30 °C)

Anaerobic, disproportionation Habicht et al.(1988)[76]

See also

References

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