Multiple sulphur and iron isotope composition of detrital pyrite in Archaean sedimentary rocks: A new tool for provenance analysis

Hofmann, Axel; Bekker, Andrey; Rouxel, Olivier; Rumble, Douglas; Master, Sharad

doi:10.1016/j.epsl.2009.07.008

Cited by 115 publications

(53 citation statements)

References 71 publications

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“…• Sediment-hosted Stratiform Copper Deposits, which form in preexisting sediments by leaching of proximal volcanics with hypersaline (high salinity) oxidized fluids, also first appeared around 2.25 Ga (Kirkham and Roscoe 1993). • Well-rounded pebbles of the minerals uraninite (UO 2 ), pyrite (FeS 2 ), and siderite (FeCO 3 ), which are unstable in modern oxidized fluvial environments, are common only in conglomerates deposited in fluvial and shallowmarine settings before *2.3 Ga (Rasmussen and Buick 1999;Roscoe 1996;England et al 2002;Hofmann et al 2009). • Paleosols, ancient weathering horizons that form in contact with the atmosphere, are leached of iron when older than *2.4 Ga because Fe 2?…”

Section: Other Lithological Indicators Of Oxygenationmentioning

confidence: 99%

Geological constraints on the origin of oxygenic photosynthesis

2010

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This article examines the geological evidence for the rise of atmospheric oxygen and the origin of oxygenic photosynthesis. The evidence for the rise of atmospheric oxygen places a minimum time constraint before which oxygenic photosynthesis must have developed, and was subsequently established as the primary control on the atmospheric oxygen level. The geological evidence places the global rise of atmospheric oxygen, termed the Great Oxidation Event (GOE), between ~2.45 and ~2.32 Ga, and it is captured within the Duitschland Formation, which shows a transition from mass-independent to mass-dependent sulfur isotope fractionation. The rise of atmospheric oxygen during this interval is closely associated with a number of environmental changes, such as glaciations and intense continental weathering, and led to dramatic changes in the oxidation state of the ocean and the seawater inventory of transition elements. There are other features of the geologic record predating the GOE by as much as 200-300 million years, perhaps extending as far back as the Mesoarchean-Neoarchean boundary at 2.8 Ga, that suggest the presence of low level, transient or local, oxygenation. If verified, these features would not only imply an earlier origin for oxygenic photosynthesis, but also require a mechanism to decouple oxygen production from oxidation of Earth's surface environments. Most hypotheses for the GOE suggest that oxygen production by oxygenic photosynthesis is a precondition for the rise of oxygen, but that a synchronous change in atmospheric oxygen level is not required by the onset of this oxygen source. The potential lag-time in the response of Earth surface environments is related to the way that oxygen sinks, such as reduced Fe and sulfur compounds, respond to oxygen production. Changes in oxygen level imply an imbalance in the sources and sinks for oxygen. Changes in the cycling of oxygen have occurred at various times before and after the GOE, and do not appear to require corresponding changes in the intensity of oxygenic photosynthesis. The available geological constraints for these changes do not, however, disallow a direct role for this metabolism. The geological evidence for early oxygen and hypotheses for the controls on oxygen level are the basis for the interpretation of photosynthetic oxygen production as examined in this review.

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Section: Other Lithological Indicators Of Oxygenationmentioning

confidence: 99%

Geological constraints on the origin of oxygenic photosynthesis

2010

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“…Large variations in isotopic composition ( 56 Fe/ 54 Fe) among iron-bearing species in geological and biological systems at Earth-surface temperatures (from d 56 Fe = À3.6& (sedimentary pyrite) to 1.6& (Fe-oxide in banded-iron formation)) have been found in natural samples (e.g., Beard and Johnson, 2004, and references therein;Rouxel et al, 2005;Hofmann et al, 2009), laboratory experiments (e.g., Anbar et al, 2000;Johnson et al, 2002;Welch et al, 2003), and in theoretical models (e.g., Polyakov and Mineev, 2000;Schauble et al, 2001;Anbar et al, 2005;Hill and Schauble, 2008). Such variations have primarily been attributed to redox effects in the environment upon fractionations among iron-bearing species, suggesting that 56 Fe/ 54 Fe may be an indicator of past oxygen fugacity levels in the sedimentary record (e.g., Rouxel et al, 2005;Yamaguchi and Ohmoto, 2006;Yamaguchi et al, 2007) and/or of bacterial processes (e.g., Johnson et al, 2008, and references therein).…”

Section: Introductionmentioning

confidence: 97%

Effects of changing solution chemistry on Fe3+/Fe2+ isotope fractionation in aqueous Fe–Cl solutions

Hill

Schauble

Young

2010

Geochimica et Cosmochimica Acta

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“…In the rock record, this event is manifested by a number of changes (see Farquhar et al, 2011Farquhar et al, , 2014, for reviews), including (1) loss of easily oxidisable detrital uraninite, pyrite, and siderite from fluvial siliciclastic sediments at ca. 2.4 Ga (e.g., Rasmussen and Buick, 1999;England et al, 2002;Hofmann et al, 2009;Johnson et al, 2014); (2) loss of iron from ancient soil horizons (paleosols) older than ca. 2.4 Ga because of greater iron solubility under reducing conditions (e.g., Rye and Holland, 1998); (3) the appearance of red beds after ca.…”

Section: Neoarchaean-palaeoproterozoic Iron Formationsmentioning

confidence: 99%