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Generation of Banded Iron Formations by Internal Dynamics and Leaching of Oceanic Crust Yifeng Wang1*, Huifang Xu2, Enrique Merino3 and Hiromi Konishi2

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Generation of Banded Iron Formations by Internal Dynamics and Leaching of Oceanic Crust Yifeng Wang1*, Huifang Xu2, Enrique Merino3 and Hiromi Konishi2 LETTERS PUBLISHED ONLINE: 11 OCTOBER 2009 | DOI: 10.1038/NGEO652 Generation of banded iron formations by internal dynamics and leaching of oceanic crust Yifeng Wang1*, Huifang Xu2, Enrique Merino3 and Hiromi Konishi2 The chemical signatures and mineralogy of banded iron 1.7 Gyr ago and their occurrence in both shallow- and deep-water formations have the potential to provide information about the environments. Here we present a new model that successfully ocean environment on early Earth1–7. Their formation requires addresses all of these issues. iron- and silicon-rich fluids, but the mechanisms by which Our model assumes that a BIF forms by mixing of a discharged the alternating layers of Si- and Fe-rich rock formed remain submarine hydrothermal fluid (or plume) with its ambient sea 8–11 2,3 controversial . Here we use thermodynamic calculations water (Fig. 1). The fluid acquires dissolved SiO2 and Fe(ii) to show that Fe- and Si-rich fluids can be generated by through seawater circulation and leaching in the oceanic crust. hydrothermal leaching of low-Al oceanic crustal rocks such as Fe2C is predicted to form a strong complex with silicic acid, 2C − C 4:8 komatiites. We find that positive feedbacks occur among the Fe C H3SiO4 D FeH3SiO4 , with logK D 10 (Fig. 2). Thus, chemical reactions when hydrothermal fluids mix with ambient silica and Fe(ii) can be leached out simultaneously from the oceanic sea water. These feedbacks lead to alternating precipitation crust in high and comparable amounts. In contrast, owing to their of Fe and Si minerals, owing to the formation of complexes low stability constants with silicic acid (Fig. 2), Ca and Mg would between Fe(II) and silicic acid. We suggest that the small-scale be differentially left behind in the crust during leaching. This may (<1 cm) banding was produced by internal dynamics of the explain the rarity of Archaean dolomite-limestone deposition14 15 geochemical system, rather than any external forcing. As the despite high Archaean atmospheric CO2 concentrations . The Archaean eon progressed, the oceanic crust produced was rich mobilization of transition metals (such as Zn and Pb) and the in Al12. When Al-rich crust undergoes hydrothermal alteration, formation of ore deposits of these metals were still possible however Fe is locked in Al–Fe silicate minerals. This results in iron- during that time period6. depleted hydrothermal fluids, and thus prevents the deposition Now the question is: under what conditions can the circulating of Fe-rich minerals. We therefore conclude that the widespread fluid acquire roughly equal and high concentrations of dissolved cessation of banded iron formation deposition 1.7 billion years SiO2 and Fe(ii)? Our thermodynamic calculations show that such ago reflects the changing composition of the oceanic crust. a fluid can be generated only from low-Al oceanic rocks such as Banded iron formations (BIFs) are massive chemical deposits komatiites (Fig. 3a), but not from modern oceanic basalts (Fig. 3b), composed of alternating layers of chert and iron-rich minerals which have a high Al content. The concentration of dissolved Fe(ii) (such as haematite, magnetite and siderite), with three scales of in a fluid that has reacted with such basalts is orders of magnitude bandings—microbands (≤1 mm), mesobands (∼1 mm–10 cm) lower than that of dissolved SiO2 over the whole range of solid/water and macrobands (≥1 m; refs 1–3). BIFs have been extensively stud- ratios (Fig. 3b). This low concentration results from the fact that ied as an indicator for chemical and biological evolution of the early Fe(ii) is locked up by abundant Fe(ii)–Al chlorite formed during Earth4,5. Their abundance in the Archaean/early Proterozoic era and the hydrothermal alteration. In contrast, the alteration of komatiites their absence6 thereafter suggest that chemical conditions and iron results mainly in serpentinization; the scarcity of Al keeps chlorites transport pathways on the early Earth surface were different from from forming and thus leaves the Fe free to be leached out. 7 those after 1.7 billion years (Gyr) ago . BIF bandings have been at- Given the stoichiometry of chlorite T(Fe,Mg)5Al2Si3O10(OH)8U, a tributed to seasonal temperature variations8,9, microbially catalysed necessary condition for the generation of Fe–Si-rich hydrothermal Fe(iii) (hydr)oxide precipitation triggered by ocean temperature plumes is that the molar ratio of Al/(Fe C Mg) in oceanic rocks fluctuations10, episodic fluid mixing3 and deposition by density must be <2V5, a condition satisfied by komatiites or komatiitic currents11. However, surface temperature variations cannot be basalts. A similar argument applies to Mg/Si ratios. Too high responsible for the formation of BIFs in deep-water environments3, Mg contents in oceanic crust could lock up considerable silica and in any case, such seasonal surface temperature variations were as serpentine TMg3(Si2O5)(OH)4U. The predicted alkaline nature probably not significant in the warm Archaean atmosphere13. Low of ancient hydrothermal systems (Fig. 3a,b) is supported by the organic carbon contents in BIFs suggest that microbial activity recent discovery of the Lost City hydrothermal field developed in might not have a significant role in BIF precipitation2. ultramafic rocks, where the pH ranges from 9 to 11 (ref. 16). A reasonable BIF formation model must address three key issues. Systematic compositional analyses of komatiites and the related It must account for the generation of large volumes of water melting experiments reveal general trends of early oceanic crust containing roughly comparable, and high, contents of dissolved evolution: (1) Mg contents were high before 3.5 Gyr ago and then SiO2 and Fe(ii). It must also provide a credible mechanism for decreased with time; (2) Al, Ca and Na increased as Mg decreased; oscillatory precipitation of iron and silica minerals. Finally, it (3) Si and Fe remained roughly constant12. Our calculations thus must account for both the worldwide abundance of BIFs in suggest that the presence of low-Al ultramafic rocks (for example, the Archaean/early Proterozoic era and their disappearance after komatiitic rocks) in the early oceanic crust were probably the 1Sandia National Laboratories, PO Box 5800, Albuquerque, New Mexico 87185, USA, 2Department of Geology and Geophysics and NASA Astrobiology Institute, University of Wisconsin, Madison, Wisconsin 53706, USA, 3Department of Geological Sciences, Indiana University, Bloomington, Indiana 47405, USA. *e-mail: [email protected]. NATURE GEOSCIENCE j VOL 2 j NOVEMBER 2009 j www.nature.com/naturegeoscience 781 © 2009 Macmillan Publishers Limited. All rights reserved. LETTERS NATURE GEOSCIENCE DOI: 10.1038/NGEO652 Water surface O2 Ambient sea water S , D 1 1 Mixing zone S2, D2 Si¬Fe-rich + plume FeH3SiO4 Plateau or Fe2+ P ptn seamount BIF Hydrothermal system Mantle plume Figure 1 j Precipitation of BIFs from a hydrothermal system. The ambient sea water could be either oxic or anoxic (only oxic is shown here). Komatiitic rocks formed as a part of plateau or seamount above a deep mantle plume. Periodic precipitation of iron oxide and silica was induced through a self-organization mechanism. Pptn: mineral precipitation; S1, D1: the area of the upper surface of the mixing zone and the corresponding mass exchange coefficient for mixing respectively; S2, D2: the area of the lower surface of the mixing zone and the corresponding mass exchange coefficient for mixing, respectively. 12 Pu4+ accounts for only a very small fraction of iron precipitated during leaching. This result contradicts the existing hypothesis that rising 10 Th4+ Np4+ oceanic sulphur levels may have caused the disappearance of BIFs 3+ 19 Al Fe3+ after ∼1:7 Gyr ago . 8 Am3+ For BIF formation, our model requires that only some portion of Eu3+ the bulk oceanic crust was komatiitic. As ocean crust composed of 6 Ni2+ 17 log K Co2+ komatiites tended to form a part of oceanic plateaux/seamounts , Fe2+ Fe and Si leached from these rocks could be transported away and 4 deposited on the surrounding sea floor (Fig. 1). BIFs thus did not have to precipitate directly on their source rocks. 2 2+ A second condition for BIF formation is that the leaching should 2+ Mg Ca be carried out by moderately alkaline (pH D 7:2–9:0) fluids, as 0 024681012 very alkaline water would dissolve much more silica than Fe(ii), ¬0.0197Gs + 0.0244Gn + 0.896rZ ¬ 1.26Z and acid water would dissolve much more Fe(ii) than silica (Fig. 3c). This pH range is constrained by assuming that the leaching C Figure 2 j Prediction of stability constant of FeH3SiO4 using a linear fluid is equilibrated with Fe(OH)2(s) and SiO2(amorphous). The free-energy correlation. Fe2C is predicted to form a strong complex with formation of Fe-rich brucite-like mineral phases was observed for silicic acid. This complexation has an important role in controlling dissolved olivine serpentinization20. Together with Al enrichment, an increase SiO2 and Fe(II) in a geologic fluid leaching through an oceanic crust. Data in Na and Ca contents in the oceanic crust tends to push the for stability constants are taken from ref. 27. Gs and Gn are the solvation pH of hydrothermal fluids to the higher end, outside the optimal energy and the non-solvation energy of a cation respectively; r and Z are pH range, thus not favouring BIF formation (Fig. 3c). Similarly, the ionic radius and the charge of a cation, respectively28,29. if the leached rock initially contains sufficient Fe sulphides, as the modern oceanic crust does, the oxidation of these sulphides reason for both the formation of BIFs and their abundance in by the leaching sea water could push the pH of hydrothermal the Archaean/early Proterozoic era.
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