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Volumn 307, Issue 5712, 2005, Pages 1088-1091

Iron isotope constraints on the Archean and Paleoproterozoic ocean redox state

Author keywords

[No Author keywords available]

Indexed keywords

ATMOSPHERIC CHEMISTRY; DEPOSITION; IRON OXIDES; ISOTOPES; PRECIPITATION (METEOROLOGY); REDOX REACTIONS;

EID: 13844310799     PISSN: 00368075     EISSN: None     Source Type: Journal    
DOI: 10.1126/science.1105692     Document Type: Article
Times cited : (441)

References (44)
  • 3
    • 0346457225 scopus 로고    scopus 로고
    • A. Bekker et al., Nature 427, 117 (2004).
    • (2004) Nature , vol.427 , pp. 117
    • Bekker, A.1
  • 4
    • 13844313003 scopus 로고    scopus 로고
    • note
    • The disappearance of BIFs after about 1.8 Ga had been initially thought to indicate the transition to the oxygenated ocean (1), but a growing body of evidence suggests that sultide, rather than oxygen, could have been responsible for removing Fe from deep ocean waters (13, 34-36).
  • 5
    • 13844311424 scopus 로고    scopus 로고
    • note
    • 56Fe values are estimated at 0.10‰ (2σ level). Analytical procedures, sample descriptions, and Fe isotope composition of various georeference materials, black shales, and BIF are available as supporting materials on Science Online.
  • 9
    • 13844314450 scopus 로고    scopus 로고
    • note
    • The range of Fe isotope composition of hydrogenic ferromanganese deposits in modern oceanic basins is large [between -0.8 and -0.1‰ (37)], but it is unclear whether the variability is caused by changes of Fe isotope composition in the water column or by secondary effects.
  • 17
    • 13844306894 scopus 로고    scopus 로고
    • note
    • Experimental studies suggest that Fe isotope fractionations during bacterial reduction of Fe oxides is dependent on reduction rates (6). At high reduction rates, rapid formation and sorption of Fe(II) to ferric oxide substrate produced fractionations as large as -2.3‰, but this value corresponds to an extreme case and fractionation of -1.3‰ between biogenic Fe(II) and ferric oxide is more representative (6).
  • 20
    • 13844322294 scopus 로고    scopus 로고
    • note
    • 8) produces a kinetic isotope fractionation of 0.3‰ (38), suggesting that the fractionation of pyrite is poorly constrained from -0.3 to 1.0‰ relative to dissolved Fe(II).
  • 21
    • 13844313004 scopus 로고    scopus 로고
    • note
    • 56Fe value for each sample. For comparison and to evaluate heterogeneity, we also analyzed several individual sulfide nodules from the same samples (table S2).
  • 26
    • 13844320914 scopus 로고    scopus 로고
    • note
    • 2. Alternatively, a direct mechanism for Fe oxidation by anoxygenic phototrophic bacteria has been suggested (40), and abiotic photochemical oxidation may have also contributed to Fe oxidation in the Archean (41).
  • 27
    • 13844308305 scopus 로고    scopus 로고
    • note
    • A magnetite-Fe(II) fractionation factor of about 2.4‰ has been inferred from BIFs data (12), which is slightly less than the equilibrium Fe(III)-Fe(II) fractionation factor of 2.9‰ at 22°C (42). The fractionation between ferrihydrite and Fe(II) of 1.5‰ measured during anaerobic photosynthetic Fe(II) oxidation by bacteria (43) is slightly larger than the 0.9‰ fractionation measured during abiotic oxidation of Fe(II) to ferrihydrite (25).
  • 29
    • 13844320096 scopus 로고    scopus 로고
    • note
    • BIF is the fractionation factor during Fe oxidation and Fe oxide precipitation, ranging between 1.0015 and 1.0023 (6).
  • 40
    • 0027246589 scopus 로고
    • F. Widdel et al., Nature 362, 834 (1993).
    • (1993) Nature , vol.362 , pp. 834
    • Widdel, F.1
  • 44
    • 13844306885 scopus 로고    scopus 로고
    • note
    • We gratefully acknowledge B. Krapež, M. Barley, D. Winston, B. Rasmussen, F. Gauthier-Lafaye, P. Medvedev, N. Beukes, L.-L. Coetzee, E. N. Berdusco, R. Ruhanen, M. Köhler, M. Jirsa, M. J. Severson, J. Brouwer, R. Shapiro, G. L. LaBerge, B. Peucker-Ehrenbrink, S. Petsch, and H. Baioumy for advice and access to sample collections and L. Ball and J. Blusztajn for technical assistance. O.J.R. is grateful to M. Bickle and A. Galy from the University of Cambridge for the access to Belingwe Iron Formation samples and analytical support of the Nu Plasma. A.B.'s fieldwork in South Africa and Western Australia was supported by NASA and Petroleum Research Fund grants to H. D. Holland and by Australian Research Council and Minerals Energy Research Institute of Western Australia grants to M. Barley and B. Krapež. We thank J. M. Hayes, H. D. Holland, and two anonymous reviewers for constructive comments. The Fe isotope work was supported by NASA Astrobiology Institute Award NNA04CC04A From Early Biospheric Metabolisms to the Evolution of Complex Systems (K.J.E.). Support for O.J.R. was provided by a postdoctoral fellowship from the Deep Ocean Exploration Institute at Woods Hole Oceonagraphic Institue (WHOI). This is WHOI contribution number 11275.


* 이 정보는 Elsevier사의 SCOPUS DB에서 KISTI가 분석하여 추출한 것입니다.