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48. Iron and Carbon Isotope Evidence for Microbial Iron Respiration

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Earth and Planetary Science Letters 303 (2011) 121–132 Contents lists available at ScienceDirect Earth and Planetary Science Letters journal homepage: www.elsevier.com/locate/epsl Iron and carbon isotope evidence for microbial iron respiration throughout the Archean Paul R. Craddock ⁎, Nicolas Dauphas Origins Laboratory, Department of the Geophysical Sciences and Enrico Fermi Institute, The University of Chicago, 5734 South Ellis Avenue, Chicago, IL 60637, United States article info abstract Article history: Banded Iron-Formations (BIFs) are voluminous chemical sediments that are rich in iron-oxide, carbonate and Received 17 August 2010 silica and whose occurrence is unique to the Precambrian. Their preservation in the geological record offers Received in revised form 20 December 2010 insights to the surface chemical and biological cycling of iron and carbon on early Earth. However, many details Accepted 22 December 2010 regarding the role of microbial activity in BIF deposition and diagenesis are unresolved. Laboratory studies have Available online 22 January 2011 + shown that reaction between carbon and iron through microbial iron respiration [2Fe2O3∙nH2O+CH2O+7H → 2+ − Editor: R.W. Carlson 4Fe +HCO3 +(2n+4)H2O+chemical energy] can impart fractionation to the isotopic compositions of these elements. Here, we report iron (δ56Fe, vs. IRMM-014) and carbon isotopic (δ13C, vs. V-PDB) compositions of Keywords: magnetite and of iron-rich and iron-poor carbonates in BIFs from the late Archean (~2.5 Ga) Hamersley Basin, iron-formation Australia and the early Archean (~3.8 Ga) Isua Supracrustal Belt (ISB), Greenland. The range of δ56Fe values Hamersley measured in the Hamersley Basin, including light values in magnetite and heavy values in iron-rich carbonates Isua (up to +1.2‰), are incompatible with their precipitation in equilibrium with seawater. Rather, the data together iron carbonates with previously reported light δ13C values in iron-rich carbonates record evidence for diagenetic reduction of iron respiration ferric oxide precursors to magnetite and carbonate through microbial iron respiration (i.e., dissimilatory iron reduction, DIR). Iron and carbon isotope data of iron-rich metacarbonates from the ISB are similar to those of late Archean BIFs. The isotopic signatures of these metacarbonates are supportive of an early diagenetic origin despite metasomatic overprint, and preserve evidence of microbial iron respiration within the oldest recognized sedimentary rocks on Earth. © 2010 Elsevier B.V. All rights reserved. 1. Introduction et al., 2000; Farquhar et al., 2000; Kasting, 1987; Ono et al., 2003; Pavlov and Kasting, 2002), is uncertain. Photochemical oxidation of Fe(II) Banded Iron-Formations (BIFs) are conspicuously laminated marine in surface ocean waters owing to interaction with incident UV radiation chemical sediments that are characterized by high concentrations of iron- has been proposed as an entirely abiological means of accounting for bearing minerals (20–40 wt.% bulk Fe) commonly interbedded with ferric iron in BIFs (Braterman et al., 1983; Cairns–Smith, 1978). Oxidation layers of silica, and whose occurrence is unique to the Precambrian of Fe(II) by O2 produced via photosynthesis has also been suggested (James, 1954, 1983). The mineralogy of the best-preserved BIFs consists of (Cloud, 1965, 1973), implying an indirect biological influence on BIF combinations of four dominant facies: oxide (magnetite, hematite), formation and hinting at the presence of free O2 oases in the Archean carbonate (siderite, ankerite, Fe–dolomite and, less commonly, calcite), surface ocean. Alternatively, direct biological activity has been implicated, chert and silicate (stilpnomelane, riebeckite, greenalite, minnesotaite), via anoxygenic photosynthesis that coupled oxidation of Fe(II) to and locally sulfide (pyrite) and phosphate (apatite). Most known BIFs reduction of inorganic carbon to yield organic compounds (Garrels have ages in the range ~3.8 to 1.8 Ga, but these formations also occur to a et al., 1973; Kappler et al., 2005; Konhauser et al., 2007; Widdel et al., lesser extent in the Neoproterozoic at ~700 Ma (Klein, 2005). The study of 1993). It is also uncertain the extent to which the mineral assemblages these formations preserved in the rock record offers critical insights to preserved in BIFs reflect either primary precipitates from seawater, surface geochemical cycles and chemical evolution of the ocean and possibly in near-chemical equilibrium with the ocean and atmosphere, or atmosphere in the Precambrian, and in particular the Archean (≥2.5 Ga). are authigenic minerals formed during early sedimentary diagenesis and Despite significant scientific interest and research, however, there is burial metamorphism. For example, the mineralogical, chemical (e.g., rare no consensus on the origin of BIFs. The primary mechanism for oxidation earth element) and isotopic (e.g., δ13C, δ18O) characteristics of iron-rich of Fe(II)aq in an Archean ocean that was purportedly anoxic (Canfield carbonates such as siderite [FeCO3]andankerite[Ca0.5(Fe,Mg)0.5CO3]in BIFs have been used to argue either for primary precipitation from an anoxic and stratified water column (Beukes et al., 1990; Kaufman et al., ⁎ Corresponding author. Tel.: +1 773 834 3997. 1990; Klein and Beukes, 1989) or for an authigenic origin (Becker and E-mail address: [email protected] (P.R. Craddock). Clayton, 1972; Heimann et al., 2010; Walker, 1984). 0012-821X/$ – see front matter © 2010 Elsevier B.V. All rights reserved. doi:10.1016/j.epsl.2010.12.045 122 P.R. Craddock, N. Dauphas / Earth and Planetary Science Letters 303 (2011) 121 Table 1 Iron and carbon isotopic compositions of oxides and carbonate from drill core samples of the Brockman Iron Formation, Hamersley Basin. Samplea Hole a Macroband Mesoband Type Depthb δ13C δ56Fe δ57Fe (m) (‰)c (‰) d (‰)d Ankerite Siderite Ankerite/Siderite Magnetite Hematite Ankerite/Siderite Magnetite Hematite Dales Gorge Member, Brockman Iron Formation Drill core from Wittenoom Gorge Area (118° 28′ E; 22° 25′ S) 13324 M1 27 BIF 12 Magnetite 85.2 0.424±0.031 0.630±0.043 13327 WC2 27 BIF 11 Chert 98.4 −11.41 −11.08 −0.289±0.031 0.205±0.031 −0.442±0.049 0.316±0.049 13327 WC1 27 BIF 11 Chert 98.4 −15.05 0.013±0.031 0.465±0.031 0.008±0.046 0.699±0.043 13321 HC 27 BIF 10 Chert+hematite 99.5 −6.98 −7.45 −0.705±0.031 0.908±0.038 −1.023±0.083 1.369±0.044 13318 M3 27 BIF 7 Magnetite 122.2 −9.24±0.03 0.006±0.036 0.005±0.057 13318 Pl 27 BIF 7 Chert 122.2 −9.83±0.04 −0.584±0.029 −0.865±0.051 13318 FM1 27 BIF 7 Chert 122.2 −9.72±0.06 0.118±0.031 −0.210±0.034 0.373 ±0.029 0.198±0.046 −0.298±0.054 0.561±0.051 13318 M1 27 BIF 7 Magnetite 122.3 0.159±0.029 0.230±0.051 13318 M2 27 BIF 7 Magnetite 122.3 0.112±0.031 0.179±0.046 13316 M1 27 BIF 6 Magnetite 128.1 0.650±0.038 0.949±0.058 13316 CA1 27 BIF 6 Fine−band combination 128.2 −9.31 0.641±0.031 0.636±0.033 0.933±0.083 0.914±0.060 13316 CB1 27 BIF 6 Coarse-band combination 128.2 −9.01 −9.41 0.178±0.033 0.196±0.031 0.283±0.060 0.244±0.049 13309 FM1 27 BIF 1 Chert 162.2 −9.87 0.057±0.031 0.588±0.031 0.070±0.046 0.852±0.043 13309 PC1 27 BIF 1 Chert 162.3 −10.06 −0.161±0.031 0.490±0.030 −0.236±0.043 0.710±0.046 13309 QIO1 27 BIF 1 Chert-matrix 162.4 0.675±0.031 0.790 ±0.034 0.990±0.046 1.144±0.054 13309 M2 27 BIF 1 Magnetite 162.4 0.488±0.030 0.694±0.044 13326 M1 28 BIF 12 Magnetite 110.9 0.418±0.031 0.610±0.046 – 13328 WC2 28 BIF 11 Chert 114.9 −11.07 −12.48 −0.555±0.031 −0.757±0.049 132 13328 WC1 28 BIF 11 Chert 115.0 −12.86 0.426±0.038 0.630±0.044 13322 WC1 28 BIF 10 Chert 125.2 −9.73 0.453±0.035 0.662±0.047 13322 WCIA 28 BIF 10 Chert 125.2 −9.61 0.294±0.027 0.419±0.040 13322 M1 28 BIF 10 Magnetite 125.2 0.730±0.033 1.107±0.060 13322 HC 28 BIF 10 Chert+hematite 125.2 −6.76 −8.26 −0.792±0.038 0.398±0.030 −1.142±0.044 0.584±0.057 13322 WHC 28 BIF 10 Chert+hematite 125.2 −6.50±0.03 −7.80 −1.081±0.033 −1.601±0.060 13322 FM1 28 BIF 10 Chert 125.3 −8.96 −9.79 0.787±0.033 1.194±0.033 1.158±0.044 1.778±0.044 13322 QIO1 28 BIF 10 Chert-matrix 125.3 0.566±0.038 0.998±0.038 0.847±0.058 1.477±0.058 13319 FM3 28 BIF 7 Chert 146.5 −9.74±0.03 −0.318±0.029 −0.287±0.030 −0.470±0.043 −0.422±0.044 13319 FM2 28 BIF 7 Chert 146.6 −10.18±0.01 0.086±0.030 0.064±0.030 0.156±0.044 0.077±0.044 13319 M1 28 BIF 7 Magnetite 146.6 −0.022±0.030 0.014±0.044 13319 FM1 28 BIF 7 Chert 146.6 −9.90 0.075±0.030 −0.149±0.029 0.093±0.044 −0.212±0.043 13313 M1 28 BIF 2 Magnetite 174.5 1.085±0.029 1.582±0.043 13310 PC1 28 BIF 1 Chert 186.7 −0.181±0.028 0.159±0.035 −0.303±0.047 0.241±0.047 M 2 40 BIF 2 Magnetite 196.8 0.551±0.035 0.810±0.047 P 2 40 BIF 2 Chert 196.8 −9.70±0.02 P 2A 40 BIF 2 Chert 196.8 −9.80±0.06 Table 1 (continued) Samplea Hole a Macroband Mesoband Type Depthb δ13C δ56Fe δ57Fe (m) (‰)c (‰) d (‰)d Ankerite Siderite Ankerite/Siderite Magnetite Hematite Ankerite/Siderite Magnetite Hematite Dales Gorge Member, Brockman Iron Formation Drill core from Wittenoom Gorge Area (118° 28′ E; 22° 25′ S) FM 2 40 BIF 2 Chert 196.8 −10.28±0.02 M 3 51 BIF 12 Magnetite 104.5 0.314±0.028 0.478±0.047 QIO 51 51 BIF 5 Chert-matrix 155.4 −0.189±0.028 −0.282±0.047 M 1 51 BIF 5 Magnetite 155.6 −0.092±0.035 −0.111±0.047 P l 51 BIF 5 Chert 155.6 −8.65 Drill core from Yampire Gorge Area (118° 37′ E; 22° 27′ S) 13325 WC2 Y3 BIF 12 Chert 66.2 −10.95±0.02 −0.305±0.041 0.202±0.029 −0.448±0.072 0.298±0.041 13325 M2 Y3 BIF 12 Magnetite 66.2 0.351±0.029 0.515±0.041 13325 M1 Y3 BIF 12 Magnetite 66.3 0.344±0.051 0.519±0.133 13325 FM1 Y3 BIF 12 Chert 66.3 −10.96 0.301±0.033 0.297±0.029 0.410±0.083 0.433±0.041 13325 WC1 Y3 BIF 12 Chert 66.4 −10.84±0.01 −0.404±0.029 0.194±0.029 −0.588±0.043 0.282±0.133 13329 M1 Y3 BIF 11 Magnetite 70.7 −12.59±0.50 −0.005±0.031 −0.017±0.083 13329 FM1 Y3 BIF 11 Chert 70.8 −11.11 0.244±0.033 0.408±0.033 0.674 ±0.051 0.395±0.083 0.632±0.083 1.057 ±0.133 P.R.
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    MANITOBA CANADA DEPARTMENT OF ENERGY AND MINES MANITOBA MINERAL RESOURCES DIVISION ECONOMIC GEOLOGY REPORT ER79-4 PORPHYRITIC INTRUSIONS AND RELATED MINERALIZATION IN THE FLIN FLON VOLCANIC BELT by D.A. BALDWIN 1980 Funding for this project was provided under the cost-shared Canada-Manitoba Non-renewable Resources Evaluation Program by the Canada Department of Energy, Mines and Resources and the Manitoba Department of Mines, Resources and Environmental Management. MANITOBA DEPARTMENT OF ENERGY AND MINES HON. DONALD W. CRAIK PAUL E. JARVIS Minister Deputy Minister MINERAL RESOURCES DIVISION IAN HAUGH Executive Director ECONOMIC GEOLOGY REPORT ER79-4 PORPHYRITIC INTRUSIONS AND RELATED MINERALIZATION IN THE FLIN FLON VOLCANIC BELT by D.A. BALDWIN 1980 LEGEND I Cliff Lake Stock 5 Elbow Lake Stock 2 Whitefish Lake Porphyry 6 Fourmile Island Intrusion 3 Alberts Lake Intrusion 7 Chisel Lake Intrusion 4 Nisto Lake Intrusion 8 Wekusko Lake Intrusion ,~ -./ - -, I \." ~herridon '" , ;. <,.... ,1 if 55°00' 55°00' c, t,:) ,J -3 , I"" . c;? '" 1[' . ::t} \'''If!? ~,/J~ /j' ., ~), F lin.~ i;\))F ' I,".!0l~' ,d ' ;)/", ' ~.;'. l ;' ~" ,r~n ;t j; (I:/,1 ,r Lake ' \\ ;\~ ' ~i'/ 'lUi':;- -'i' //{ ,'/ , ,\" ,,/,1,1 pI , .h .(,1;' '\:. (IiI' ' .. '~'4_hl i / 'Y{j,'{:" 5 2.5 a 10 15 KILOMETRES J!) "'.t3 f3,F-"\ ---- :i~ f)J~c~. V 99°30' ">/)AfhapaplJskoj¥ !ZJ Porphyritic Intrusive Rocks 54°30' ! ,1 Lake .; ... 100°30' D Felsic Volcanic Rocks FIGURE 1: Distribution of porphyritic intrusive and felsic volcanic rocks in the Flin Flon volcanic belt, TABLE OF
  • Chemical Oxides Analysis from Azara Baryte

    Chemical Oxides Analysis from Azara Baryte

    African Journal of Pure and Applied Chemistry Vol. 1 (2), pp. 015-017, November 2007 Available online at http://www.academicjournals.org/AJCAB ISSN 1996 - 0840 © 2007 Academic Journals Short Communication Chemical oxides analysis from Azara Baryte Hauwa Isa Department of Science Laboratory Technology School of Applied Sciences, Nuhu Bamalli Polytechnic, Zaria Nigeria. E- mail: [email protected] Accepted 26 September, 2007 Physical and chemical analysis of the two samples A and B of Azara baryte were conducted, such as moisture content, loss on ignition and elemental composition by the use of atomic absorption spectrophotometer(ASS) and flame photometer. The oxides values in 1.000 g sample of each element were obtained. Sample A (lower layer): moisture content = 0.020, loss on ignition = 0.060, Na2O = 0.250, K2O = 0.015, CaO = 0.014, MgO = 0.018, Fe2O3 = 0.029, SiO2 = 9.310, BaO = 89.630, Al2O3 = 6.200 Sample B (upper layer): moisture content = 0.030, loss on ignition = 0.040, Na2O = 0.030, K2O = 0.001, CaO = 0.006, MgO = 0.030, Fe2O3 = 0.028, SiO2 =18.12, BaO = 65.020, Al2O3 = 16.120. The result of the analysis revealed that the Azara baryte could use as source of inorganic chemical oxides and for the production of some laboratory chemicals such as barium sulphate and aluminum oxides Key words: Azara Baryte,Chemical oxides,analysis INTRODUCTION Baryte (BaSO4) – Barium sulphate is found naturally in mineral collector's market (RMRDC, 2005) Natural bary- the form of witherite (Othmer, 1964). It has various tes are chemically stable and highly temperature-resis- colours but mostly yellow, isomorphous orthorhombic tant.
  • Banded Iron Formations

    Banded Iron Formations

    Banded Iron Formations Cover Slide 1 What are Banded Iron Formations (BIFs)? • Large sedimentary structures Kalmina gorge banded iron (Gypsy Denise 2013, Creative Commons) BIFs were deposited in shallow marine troughs or basins. Deposits are tens of km long, several km wide and 150 – 600 m thick. Photo is of Kalmina gorge in the Pilbara (Karijini National Park, Hamersley Ranges) 2 What are Banded Iron Formations (BIFs)? • Large sedimentary structures • Bands of iron rich and iron poor rock Iron rich bands: hematite (Fe2O3), magnetite (Fe3O4), siderite (FeCO3) or pyrite (FeS2). Iron poor bands: chert (fine‐grained quartz) and low iron oxide levels Rock sample from a BIF (Woudloper 2009, Creative Commons 1.0) Iron rich bands are composed of hematitie (Fe2O3), magnetite (Fe3O4), siderite (FeCO3) or pyrite (FeS2). The iron poor bands contain chert (fine‐grained quartz) with lesser amounts of iron oxide. 3 What are Banded Iron Formations (BIFs)? • Large sedimentary structures • Bands of iron rich and iron poor rock • Archaean and Proterozoic in age BIF formation through time (KG Budge 2020, public domain) BIFs were deposited for 2 billion years during the Archaean and Proterozoic. There was another short time of deposition during a Snowball Earth event. 4 Why are BIFs important? • Iron ore exports are Australia’s top earner, worth $61 billion in 2017‐2018 • Iron ore comes from enriched BIF deposits Rio Tinto iron ore shiploader in the Pilbara (C Hargrave, CSIRO Science Image) Australia is consistently the leading iron ore exporter in the world. We have large deposits where the iron‐poor chert bands have been leached away, leaving 40%‐60% iron.
  • Ore Deposits

    Ore Deposits

    EARTH SCIENCES RESEARCH JOURNAL Earth Sci. Res. J. Vol. 20, No. 3 (September, 2016 ) : A1 - A10 ORE DEPOSITS Occurrence of Cr-bearing beryl in stream sediment from Eskişehir, NW Turkey Hülya Erkoyun and Selahattin Kadir * Eskişehir Osmangazi University, Deparment of Geological Engineering, TR−26480 Eskişehir, Turkey [email protected] [email protected] *corresponding author ABSTRACT Keywords: Beryl, Kaymaz, schist, SEM-EDX, IR. Beryl crystals are found within stream sediments transecting schists in the northeast of Eskişehir, western Anatolia. This paper studied the Eskişehir beryl crystals with optical microscopy, scanning electron microscopy (SEM-EDX), infrared spectroscopy (IR) and geochemical analyses. Beryl is accompanied by garnet, glaucophane, quartz, epidote, muscovite and chlorite in the stream sediments. The crystals are euhedral emerald (green gem beryl) and light bluish- green aquamarine, with ideal sharp IR bands. Wet chemical analysis of Eskişehir beryl yielded 61.28% SiO2, 15.13% Al2O3, 12.34% BeO, 0.18% Cr2O3, 1.49% MgO, 1.69% Na2O, 0.98% Fe2O3, and 0.008% V2O3, resulting in the formula (Al1.75Cr0.01Mg0.22Fe0.08)(Be2.90Si6.00)(Na0.32)O18. Large Ion Lithophile Elements (LILE) (barium, strontium), some transition metals (cobalt, except nickel) and High Field Strength Elements (HFSE) (niobium, zirconium, and yttrium) in stream sediments that are associated with beryl exhibited low content about metamorphic rocks. Beryl formation appears to be controlled by upthrust faults and fractures that juxtaposed them with Cr-bearing ophiolitic units and a regime of metasomatic reactions. Such beryl crystals have also been found in detrital sediments that are derived from the schists. Presencia de berilios relacionados con Cromo en corrientes sedimentarias de Eskisehir, noroeste de Turquía RESUMEN Cristales de berilio fueron encontrados en sedimentos de corrientes que atraviesan en esquistos en el noreste de Palabras clave: Berilio, Kaymaz, esquistos, Eskisehir, al oeste de Anatolia.