Microbial production of isotopically light iron(II) in a modern chemically precipitated sediment and implications for isotopic variations in ancient rocks

Authors

G. E. Tangalos, University of Wisconsin - Madison
B. L. Beard, University of Wisconsin - Madison
C. M. Johnson, University of Wisconsin - Madison
Charles N. Alpers, U.S. Geological SurveyFollow
E. S. Shelobolina, University of Wisconsin - Madison
H. Xu, University of Wisconsin - Madison
H. Konishi, University of Wisconsin - Madison
E. E. Roden, University of Wisconsin - MadisonFollow

Document Type

Article

Date of this Version

2010

Comments

Published in Geobiology (2010), 8, 197–208; DOI:10.1111/j.1472-4669.2010.00237.x

Abstract

The inventories and Fe isotope composition of aqueous Fe(II) and solid-phase Fe compounds were quantified in neutral-pH, chemically precipitated sediments downstream of the Iron Mountain acid mine drainage site in northern California, USA. The sediments contain high concentrations of amorphous Fe(III) oxyhydroxides [Fe(III)_am] that allow dissimilatory iron reduction (DIR) to predominate over Fe–S interactions in Fe redox transformation, as indicated by the very low abundance of Cr(II)-extractable reduced inorganic sulfur compared with dilute HCl-extractable Fe. δ⁵⁶Fe values for bulk HCl- and HF-extractable Fe were ≈ 0. These near-zero bulk δ⁵⁶Fe values, together with the very low abundance of dissolved Fe in the overlying water column, suggest that the pyrite Fe source had near-zero δ⁵⁶Fe values, and that complete oxidation of Fe(II) took place prior to deposition of the Fe(III) oxide-rich sediment. Sediment core analyses and incubation experiments demonstrated the production of millimolar quantities of isotopically light (δ⁵⁶Fe ≈ -1.5 to -0.5⁰/₀₀) aqueous Fe(II) coupled to partial reduction of Fe(III)_am by DIR. Trends in the Fe isotope composition of solid-associated Fe(II) and residual Fe(III)_am are consistent with experiments with synthetic Fe(III) oxides, and collectively suggest an equilibrium Fe isotope fractionation between aqueous Fe(II) and Fe(III)_am of approximately) -2⁰/₀₀. These Fe(III) oxide-rich sediments provide a model for early diagenetic processes that are likely to have taken place in Archean and Paleoproterozoic marine sediments that served as precursors for banded iron formations. Our results suggest pathways whereby DIR could have led to the formation of large quantities of low-δ⁵⁶Fe minerals during BIF genesis.