Hydrocarbons in Hydrothermal Vent Fluids: The Role of Chromium-Bearing Catalysts

Foustoukos, Dionysis I.; Seyfried, William E.

doi:10.1126/science.1096033

Cited by 316 publications

(240 citation statements)

References 22 publications

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“…Chromite, Fe-Ni alloys, and magnetite have been shown to catalyze this reaction (Horita and Berndt, 1999;Foustoukos and Seyfried, 2004) and these and similar phases are abundant constituents of the CM chondrites (Brearley and Jones, 1998). At 200˚C (a temperature at which this reaction occurs over laboratory time scales), the CH 4 produced by this reaction is ca.…”

Section: Correlation Between δ 13 C Of the Carbonates And δ 18 O Of Tmentioning

confidence: 99%

Temperatures of aqueous alteration and evidence for methane generation on the parent bodies of the CM chondrites

Guo

Eiler

2007

Geochimica et Cosmochimica Acta

220

214

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Section: Correlation Between δ 13 C Of the Carbonates And δ 18 O Of Tmentioning

confidence: 99%

Temperatures of aqueous alteration and evidence for methane generation on the parent bodies of the CM chondrites

Guo

Eiler

2007

Geochimica et Cosmochimica Acta

220

214

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“…Thus, at least some role for inorganic methane seems inescapable unless net heating by water vapour and clouds was proportionally higher than currently assumed or a fourth factor is overlooked. Abiotic methane (Horita & Berndt 1999;Foustoukos & Seyfried 2004;Scott et al 2004a) is found, e.g. in deep mines in Canada and South Africa and in mid-oceanic rifts.…”

Section: Synthesis: How Microbial Quantum Evolution Changed the Worldmentioning

confidence: 99%

Cell evolution and Earth history: stasis and revolution

Cavalier‐Smith

2006

Phil. Trans. R. Soc. B

249

278

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This synthesis has three main parts. The first discusses the overall tree of life and nature of the last common ancestor (cenancestor). I emphasize key steps in cellular evolution important for ordering and timing the major evolutionary innovations in the history of the biosphere, explaining especially the origins of the eukaryote cell and of bacterial flagella and cell envelope novelties. Second, I map the tree onto the fossil record and discuss dates of key events and their biogeochemical impact. Finally, I present a broad synthesis, discussing evidence for a three-phase history of life. The first phase began perhaps ca 3.5 Gyr ago, when the origin of cells and anoxic photosynthesis generated the arguably most primitive prokaryote phylum, Chlorobacteria (ZChloroflexi), the first negibacteria with cells bounded by two acyl ester phospholipid membranes. After this 'chlorobacterial age' of benthic anaerobic evolution protected from UV radiation by mineral grains, two momentous quantum evolutionary episodes of cellular innovation and microbial radiation dramatically transformed the Earth's surface: the glycobacterial revolution initiated an oxygenic 'age of cyanobacteria' and, as the ozone layer grew, the rise of plankton; immensely later, probably as recently as ca 0.9 Gyr ago, the neomuran revolution ushered in the 'age of eukaryotes', Archaebacteria (arguably the youngest bacterial phylum), and morphological complexity. Diversification of glycobacteria ca 2.8 Gyr ago, predominantly inhabiting stratified benthic mats, I suggest caused serial depletion of 13 C by ribulose 1,5-bis-phosphate caboxylase/oxygenase (Rubisco) to yield ultralight late Archaean organic carbon formerly attributed to methanogenesis plus methanotrophy. The late origin of archaebacterial methanogenesis ca 720 Myr ago perhaps triggered snowball Earth episodes by slight global warming increasing weathering and reducing CO 2 levels, to yield runaway cooling; the origin of anaerobic methane oxidation ca 570 Myr ago reduced methane flux at source, stabilizing Phanerozoic climates. I argue that the major cellular innovations exhibit a pattern of quantum evolution followed by very rapid radiation and then substantial stasis, as described by Simpson. They yielded organisms that are a mosaic of extremely conservative and radically novel features, as characterized by De Beer's phrase 'mosaic evolution'. Evolution is not evenly paced and there are no real molecular clocks.

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“…Chromite (FeCr 2 O 4 ), a primary mineral common in serpentinization systems, has been shown to enhance FTT synthesis reactions (17). Additionally, secondary minerals such as magnetite (Fe 3 O 4 ) and/or awaruite (Ni 3 Fe) are produced during olivine hydrolysis, providing increased opportunities for FTT catalysis (13,15,(18)(19)(20)(21).…”

mentioning

confidence: 99%

Differentiating biotic from abiotic methane genesis in hydrothermally active planetary surfaces

Oze

Jones

Goldsmith

et al. 2012

Proc. Natl. Acad. Sci. U.S.A.

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Molecular hydrogen (H 2 ) is derived from the hydrothermal alteration of olivine-rich planetary crust. Abiotic and biotic processes consume H 2 to produce methane (CH 4 ); however, the extent of either process is unknown. Here, we assess the temporal dependence and limit of abiotic CH 4 related to the presence and formation of mineral catalysts during olivine hydrolysis (i.e., serpentinization) at 200°C and 0.03 gigapascal. Results indicate that the rate of CH 4 production increases to a maximum value related to magnetite catalyzation. By identifying the dynamics of CH 4 production, we kinetically model how the H 2 to CH 4 ratio may be used to assess the origin of CH 4 in deep subsurface serpentinization systems on Earth and Mars. Based on our model and available field data, low H 2 ∕CH 4 ratios (less than approximately 40) indicate that life is likely present and active.kinetics | molecular hydrogen | Fischer-Tropsch type reactions | methanogenesis O livine hydrolysis (i.e., serpentinization) is a major pathway related to the near-surface synthesis of molecular hydrogen (H 2 ) on Earth, Mars, and, potentially, other planets and satellites (1-4). Molecular hydrogen from serpentinization can chemically reduce carbon (e.g., HCO 3 − , HCOOH, CO, CO 2 ) to form CH 4 or can be converted to CH 4 via microbial processes (i.e., methanogenesis) (1, 3, 5-12). Although CH 4 formation is thermodynamically favorable over a range of pressure (P) and temperature (T) (13, 14), CH 4 production via Fischer-Tropsch type (FTT) reactions is slow without the aid of mineral catalysts (3,9,15,16). To understand the limits of abiotic CH 4 production, it is imperative to assess the role of mineral catalysts, both those initially present in the system and those formed during the process of serpentinization.Chromite (FeCr 2 O 4 ), a primary mineral common in serpentinization systems, has been shown to enhance FTT synthesis reactions (17). Additionally, secondary minerals such as magnetite (Fe 3 O 4 ) and/or awaruite (Ni 3 Fe) are produced during olivine hydrolysis, providing increased opportunities for FTT catalysis (13,15,(18)(19)(20)(21). Here, we evaluate the rate of abiotic CH 4 production for systems catalyzed both by chromite and secondary minerals (magnetite and awaruite) in experimental systems undergoing serpentinization at 200°C and 0.03 gigapascal (GPa), conditions similar to hydrothermally altered peridotite in midocean ridge environments on Earth or at approximately 5 km depth in the Martian subsurface. By measuring H 2 and CH 4 formed during olivine hydrolysis, mineral-catalyzed CH 4 production can be differentiated from biogenic CH 4 production through a consideration of the H 2 -CH 4 kinetic balance. Experimental ProceduresSerpentinization experiments were carried out in the WaterRock Interaction Laboratory (US Geological Survey, Menlo Park, CA) using the parameters listed in

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Hydrocarbons in Hydrothermal Vent Fluids: The Role of Chromium-Bearing Catalysts

Cited by 316 publications

References 22 publications

Temperatures of aqueous alteration and evidence for methane generation on the parent bodies of the CM chondrites

Temperatures of aqueous alteration and evidence for methane generation on the parent bodies of the CM chondrites

Cell evolution and Earth history: stasis and revolution

Differentiating biotic from abiotic methane genesis in hydrothermally active planetary surfaces

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