AustralieFrV1, PascalFrancis, Checkpoint, bibRecord, 002965

Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event

Identifieur interne : 002965 ( PascalFrancis/Checkpoint ); précédent : 002964; suivant : 002966

Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event

Auteurs : Kurt O. Konhauser [Canada] ; Ernesto Pecoits [Canada] ; Stefan V. Lalonde [Canada] ; Dominic Papineau [États-Unis] ; Euan G. Nisbet [Royaume-Uni] ; Mark E. Barley [Australie] ; Nicholas T. Arndt [France] ; Kevin Zahnle [États-Unis] ; Balz S. Kamber [Canada]

Source :

Nature : (London) [ 0028-0836 ] ; 2009.

RBID : Pascal:09-0225836

Descripteurs français

Pascal (Inist)
- Oxydation, Appauvrissement, Méthane, Paléoatmosphère, Concentration, Oxygène, Archéen, Altération météorique, Sulfure, Sulfate, Réduction chimique, Microorganisme, Formation ferrifère rubanée, Bactérie, Rapport chimique, Fer, Nickel, Refroidissement, Manteau sup, Roche ultramafique, Coefficient partage, Hydroxyde, Bactérie méthanogène, Océan, Production, Origine biogène, Enzyme, Condition oxydoréduction.
Wicri :
- topic : Oxygène, Fer, Nickel, Océan, Production, Enzyme.

English descriptors

KwdEn :
- Archean, BIF, bacteria, biogenic origin, chemical ratios, chemical reduction, concentration, cooling, depletion, enzymes, hydroxides, iron, methane, microorganisms, nickel, ocean, oxidation, oxidation-reduction conditions, oxygen, paleoatmosphere, partition coefficients, production, sulfates, sulfides, ultramafics, upper mantle, weathering.

Abstract

It has been suggested that a decrease in atmospheric methane levels triggered the progressive rise of atmospheric oxygen, the so-called Great Oxidation Event, about 2.4 Gyr ago¹. Oxidative weathering of terrestrial sulphides, increased oceanic sulphate, and the ecological success of sulphate-reducing microorganisms over methanogens has been proposed as a possible cause for the methane collapse¹, but this explanation is difficult to reconcile with the rock record^2,3. Banded iron formations preserve a history of Precambrian oceanic elemental abundance and can provide insights into our understanding of early microbial life and its influence on the evolution of the Earth system^4,5. Here we report a decline in the molar nickel to iron ratio recorded in banded iron formations about 2.7 Gyr ago, which we attribute to a reduced flux of nickel to the oceans, a consequence of cooling upper-mantle temperatures and decreased eruption of nickel-rich ultramafic rocks at the time. We measured nickel partition coefficients between simulated Precambrian sea water and diverse iron hydroxides, and subsequently determined that dissolved nickel concentrations may have reached ∼400nM throughout much of the Archaean eon, but dropped below ∼200 nM by 2.5 Gyr ago and to modern day values⁶ (∼9 nM) by ∼550 Myr ago. Nickel is a key metal cofactor in several enzymes of methanogens⁷ and we propose that its decline would have stifled their activity in the ancient oceans and disrupted the supply of biogenic methane. A decline in biogenic methane production therefore could have occurred before increasing environmental oxygenation and not necessarily be related to it. The enzymatic reliance of methanogens on a diminishing supply of volcanic nickel links mantle evolution to the redox state of the atmosphere.

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<profileDesc><textClass><keywords scheme="KwdEn" xml:lang="en"><term>Archean</term>
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<term>chemical ratios</term>
<term>chemical reduction</term>
<term>concentration</term>
<term>cooling</term>
<term>depletion</term>
<term>enzymes</term>
<term>hydroxides</term>
<term>iron</term>
<term>methane</term>
<term>microorganisms</term>
<term>nickel</term>
<term>ocean</term>
<term>oxidation</term>
<term>oxidation-reduction conditions</term>
<term>oxygen</term>
<term>paleoatmosphere</term>
<term>partition coefficients</term>
<term>production</term>
<term>sulfates</term>
<term>sulfides</term>
<term>ultramafics</term>
<term>upper mantle</term>
<term>weathering</term>
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<keywords scheme="Pascal" xml:lang="fr"><term>Oxydation</term>
<term>Appauvrissement</term>
<term>Méthane</term>
<term>Paléoatmosphère</term>
<term>Concentration</term>
<term>Oxygène</term>
<term>Archéen</term>
<term>Altération météorique</term>
<term>Sulfure</term>
<term>Sulfate</term>
<term>Réduction chimique</term>
<term>Microorganisme</term>
<term>Formation ferrifère rubanée</term>
<term>Bactérie</term>
<term>Rapport chimique</term>
<term>Fer</term>
<term>Nickel</term>
<term>Refroidissement</term>
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<term>Hydroxyde</term>
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<term>Océan</term>
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<front><div type="abstract" xml:lang="en">It has been suggested that a decrease in atmospheric methane levels triggered the progressive rise of atmospheric oxygen, the so-called Great Oxidation Event, about 2.4 Gyr ago<sup>1</sup>
. Oxidative weathering of terrestrial sulphides, increased oceanic sulphate, and the ecological success of sulphate-reducing microorganisms over methanogens has been proposed as a possible cause for the methane collapse<sup>1</sup>
, but this explanation is difficult to reconcile with the rock record<sup>2,3</sup>
. Banded iron formations preserve a history of Precambrian oceanic elemental abundance and can provide insights into our understanding of early microbial life and its influence on the evolution of the Earth system<sup>4,5</sup>
. Here we report a decline in the molar nickel to iron ratio recorded in banded iron formations about 2.7 Gyr ago, which we attribute to a reduced flux of nickel to the oceans, a consequence of cooling upper-mantle temperatures and decreased eruption of nickel-rich ultramafic rocks at the time. We measured nickel partition coefficients between simulated Precambrian sea water and diverse iron hydroxides, and subsequently determined that dissolved nickel concentrations may have reached ∼400nM throughout much of the Archaean eon, but dropped below ∼200 nM by 2.5 Gyr ago and to modern day values<sup>6</sup>
 (∼9 nM) by ∼550 Myr ago. Nickel is a key metal cofactor in several enzymes of methanogens<sup>7</sup>
 and we propose that its decline would have stifled their activity in the ancient oceans and disrupted the supply of biogenic methane. A decline in biogenic methane production therefore could have occurred before increasing environmental oxygenation and not necessarily be related to it. The enzymatic reliance of methanogens on a diminishing supply of volcanic nickel links mantle evolution to the redox state of the atmosphere.</div>
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<fA64 i1="01" i2="1"><s0>Nature : (London)</s0>
</fA64>
<fA66 i1="01"><s0>GBR</s0>
</fA66>
<fC01 i1="01" l="ENG"><s0>It has been suggested that a decrease in atmospheric methane levels triggered the progressive rise of atmospheric oxygen, the so-called Great Oxidation Event, about 2.4 Gyr ago<sup>1</sup>
. Oxidative weathering of terrestrial sulphides, increased oceanic sulphate, and the ecological success of sulphate-reducing microorganisms over methanogens has been proposed as a possible cause for the methane collapse<sup>1</sup>
, but this explanation is difficult to reconcile with the rock record<sup>2,3</sup>
. Banded iron formations preserve a history of Precambrian oceanic elemental abundance and can provide insights into our understanding of early microbial life and its influence on the evolution of the Earth system<sup>4,5</sup>
. Here we report a decline in the molar nickel to iron ratio recorded in banded iron formations about 2.7 Gyr ago, which we attribute to a reduced flux of nickel to the oceans, a consequence of cooling upper-mantle temperatures and decreased eruption of nickel-rich ultramafic rocks at the time. We measured nickel partition coefficients between simulated Precambrian sea water and diverse iron hydroxides, and subsequently determined that dissolved nickel concentrations may have reached ∼400nM throughout much of the Archaean eon, but dropped below ∼200 nM by 2.5 Gyr ago and to modern day values<sup>6</sup>
 (∼9 nM) by ∼550 Myr ago. Nickel is a key metal cofactor in several enzymes of methanogens<sup>7</sup>
 and we propose that its decline would have stifled their activity in the ancient oceans and disrupted the supply of biogenic methane. A decline in biogenic methane production therefore could have occurred before increasing environmental oxygenation and not necessarily be related to it. The enzymatic reliance of methanogens on a diminishing supply of volcanic nickel links mantle evolution to the redox state of the atmosphere.</s0>
</fC01>
<fC02 i1="01" i2="2"><s0>001E01I</s0>
</fC02>
<fC02 i1="02" i2="2"><s0>224A</s0>
</fC02>
<fC03 i1="01" i2="2" l="FRE"><s0>Oxydation</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="2" l="ENG"><s0>oxidation</s0>
<s5>01</s5>
</fC03>
<fC03 i1="01" i2="2" l="SPA"><s0>Oxidación</s0>
<s5>01</s5>
</fC03>
<fC03 i1="02" i2="2" l="FRE"><s0>Appauvrissement</s0>
<s5>02</s5>
</fC03>
<fC03 i1="02" i2="2" l="ENG"><s0>depletion</s0>
<s5>02</s5>
</fC03>
<fC03 i1="03" i2="2" l="FRE"><s0>Méthane</s0>
<s5>04</s5>
</fC03>
<fC03 i1="03" i2="2" l="ENG"><s0>methane</s0>
<s5>04</s5>
</fC03>
<fC03 i1="03" i2="2" l="SPA"><s0>Metano</s0>
<s5>04</s5>
</fC03>
<fC03 i1="04" i2="2" l="FRE"><s0>Paléoatmosphère</s0>
<s5>05</s5>
</fC03>
<fC03 i1="04" i2="2" l="ENG"><s0>paleoatmosphere</s0>
<s5>05</s5>
</fC03>
<fC03 i1="04" i2="2" l="SPA"><s0>Paleoatmósfera</s0>
<s5>05</s5>
</fC03>
<fC03 i1="05" i2="2" l="FRE"><s0>Concentration</s0>
<s5>06</s5>
</fC03>
<fC03 i1="05" i2="2" l="ENG"><s0>concentration</s0>
<s5>06</s5>
</fC03>
<fC03 i1="05" i2="2" l="SPA"><s0>Concentración</s0>
<s5>06</s5>
</fC03>
<fC03 i1="06" i2="2" l="FRE"><s0>Oxygène</s0>
<s5>07</s5>
</fC03>
<fC03 i1="06" i2="2" l="ENG"><s0>oxygen</s0>
<s5>07</s5>
</fC03>
<fC03 i1="06" i2="2" l="SPA"><s0>Oxígeno</s0>
<s5>07</s5>
</fC03>
<fC03 i1="07" i2="2" l="FRE"><s0>Archéen</s0>
<s2>NX</s2>
<s5>08</s5>
</fC03>
<fC03 i1="07" i2="2" l="ENG"><s0>Archean</s0>
<s2>NX</s2>
<s5>08</s5>
</fC03>
<fC03 i1="07" i2="2" l="SPA"><s0>Arqueano</s0>
<s2>NX</s2>
<s5>08</s5>
</fC03>
<fC03 i1="08" i2="2" l="FRE"><s0>Altération météorique</s0>
<s5>09</s5>
</fC03>
<fC03 i1="08" i2="2" l="ENG"><s0>weathering</s0>
<s5>09</s5>
</fC03>
<fC03 i1="08" i2="2" l="SPA"><s0>Alteración meteórica</s0>
<s5>09</s5>
</fC03>
<fC03 i1="09" i2="2" l="FRE"><s0>Sulfure</s0>
<s2>NZ</s2>
<s5>11</s5>
</fC03>
<fC03 i1="09" i2="2" l="ENG"><s0>sulfides</s0>
<s2>NZ</s2>
<s5>11</s5>
</fC03>
<fC03 i1="09" i2="2" l="SPA"><s0>Sulfuro</s0>
<s2>NZ</s2>
<s5>11</s5>
</fC03>
<fC03 i1="10" i2="2" l="FRE"><s0>Sulfate</s0>
<s2>NZ</s2>
<s5>12</s5>
</fC03>
<fC03 i1="10" i2="2" l="ENG"><s0>sulfates</s0>
<s2>NZ</s2>
<s5>12</s5>
</fC03>
<fC03 i1="10" i2="2" l="SPA"><s0>Sulfato</s0>
<s2>NZ</s2>
<s5>12</s5>
</fC03>
<fC03 i1="11" i2="2" l="FRE"><s0>Réduction chimique</s0>
<s5>13</s5>
</fC03>
<fC03 i1="11" i2="2" l="ENG"><s0>chemical reduction</s0>
<s5>13</s5>
</fC03>
<fC03 i1="11" i2="2" l="SPA"><s0>Reducción química</s0>
<s5>13</s5>
</fC03>
<fC03 i1="12" i2="2" l="FRE"><s0>Microorganisme</s0>
<s5>14</s5>
</fC03>
<fC03 i1="12" i2="2" l="ENG"><s0>microorganisms</s0>
<s5>14</s5>
</fC03>
<fC03 i1="12" i2="2" l="SPA"><s0>Microorganismo</s0>
<s5>14</s5>
</fC03>
<fC03 i1="13" i2="2" l="FRE"><s0>Formation ferrifère rubanée</s0>
<s2>NV</s2>
<s5>15</s5>
</fC03>
<fC03 i1="13" i2="2" l="ENG"><s0>BIF</s0>
<s2>NV</s2>
<s5>15</s5>
</fC03>
<fC03 i1="13" i2="2" l="SPA"><s0>Formación ferrífero en banda</s0>
<s2>NV</s2>
<s5>15</s5>
</fC03>
<fC03 i1="14" i2="2" l="FRE"><s0>Bactérie</s0>
<s2>NY</s2>
<s5>17</s5>
</fC03>
<fC03 i1="14" i2="2" l="ENG"><s0>bacteria</s0>
<s2>NY</s2>
<s5>17</s5>
</fC03>
<fC03 i1="15" i2="2" l="FRE"><s0>Rapport chimique</s0>
<s5>18</s5>
</fC03>
<fC03 i1="15" i2="2" l="ENG"><s0>chemical ratios</s0>
<s5>18</s5>
</fC03>
<fC03 i1="15" i2="2" l="SPA"><s0>Relación química</s0>
<s5>18</s5>
</fC03>
<fC03 i1="16" i2="2" l="FRE"><s0>Fer</s0>
<s5>19</s5>
</fC03>
<fC03 i1="16" i2="2" l="ENG"><s0>iron</s0>
<s5>19</s5>
</fC03>
<fC03 i1="16" i2="2" l="SPA"><s0>Hierro</s0>
<s5>19</s5>
</fC03>
<fC03 i1="17" i2="2" l="FRE"><s0>Nickel</s0>
<s5>20</s5>
</fC03>
<fC03 i1="17" i2="2" l="ENG"><s0>nickel</s0>
<s5>20</s5>
</fC03>
<fC03 i1="17" i2="2" l="SPA"><s0>Niquel</s0>
<s5>20</s5>
</fC03>
<fC03 i1="18" i2="2" l="FRE"><s0>Refroidissement</s0>
<s5>21</s5>
</fC03>
<fC03 i1="18" i2="2" l="ENG"><s0>cooling</s0>
<s5>21</s5>
</fC03>
<fC03 i1="18" i2="2" l="SPA"><s0>Enfriamiento</s0>
<s5>21</s5>
</fC03>
<fC03 i1="19" i2="2" l="FRE"><s0>Manteau sup</s0>
<s5>22</s5>
</fC03>
<fC03 i1="19" i2="2" l="ENG"><s0>upper mantle</s0>
<s5>22</s5>
</fC03>
<fC03 i1="19" i2="2" l="SPA"><s0>Manto globo sup</s0>
<s5>22</s5>
</fC03>
<fC03 i1="20" i2="2" l="FRE"><s0>Roche ultramafique</s0>
<s2>NV</s2>
<s5>23</s5>
</fC03>
<fC03 i1="20" i2="2" l="ENG"><s0>ultramafics</s0>
<s2>NV</s2>
<s5>23</s5>
</fC03>
<fC03 i1="21" i2="2" l="FRE"><s0>Coefficient partage</s0>
<s5>24</s5>
</fC03>
<fC03 i1="21" i2="2" l="ENG"><s0>partition coefficients</s0>
<s5>24</s5>
</fC03>
<fC03 i1="21" i2="2" l="SPA"><s0>Coeficiente repartición</s0>
<s5>24</s5>
</fC03>
<fC03 i1="22" i2="2" l="FRE"><s0>Hydroxyde</s0>
<s2>NZ</s2>
<s5>25</s5>
</fC03>
<fC03 i1="22" i2="2" l="ENG"><s0>hydroxides</s0>
<s2>NZ</s2>
<s5>25</s5>
</fC03>
<fC03 i1="22" i2="2" l="SPA"><s0>Hidróxido</s0>
<s2>NZ</s2>
<s5>25</s5>
</fC03>
<fC03 i1="23" i2="2" l="FRE"><s0>Bactérie méthanogène</s0>
<s4>INC</s4>
<s5>52</s5>
</fC03>
<fC03 i1="24" i2="2" l="FRE"><s0>Océan</s0>
<s5>61</s5>
</fC03>
<fC03 i1="24" i2="2" l="ENG"><s0>ocean</s0>
<s5>61</s5>
</fC03>
<fC03 i1="25" i2="2" l="FRE"><s0>Production</s0>
<s5>62</s5>
</fC03>
<fC03 i1="25" i2="2" l="ENG"><s0>production</s0>
<s5>62</s5>
</fC03>
<fC03 i1="25" i2="2" l="SPA"><s0>Producción</s0>
<s5>62</s5>
</fC03>
<fC03 i1="26" i2="2" l="FRE"><s0>Origine biogène</s0>
<s5>63</s5>
</fC03>
<fC03 i1="26" i2="2" l="ENG"><s0>biogenic origin</s0>
<s5>63</s5>
</fC03>
<fC03 i1="26" i2="2" l="SPA"><s0>Origen biogénico</s0>
<s5>63</s5>
</fC03>
<fC03 i1="27" i2="2" l="FRE"><s0>Enzyme</s0>
<s5>64</s5>
</fC03>
<fC03 i1="27" i2="2" l="ENG"><s0>enzymes</s0>
<s5>64</s5>
</fC03>
<fC03 i1="27" i2="2" l="SPA"><s0>Enzima</s0>
<s5>64</s5>
</fC03>
<fC03 i1="28" i2="2" l="FRE"><s0>Condition oxydoréduction</s0>
<s5>65</s5>
</fC03>
<fC03 i1="28" i2="2" l="ENG"><s0>oxidation-reduction conditions</s0>
<s5>65</s5>
</fC03>
<fC07 i1="01" i2="2" l="FRE"><s0>Précambrien</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="01" i2="2" l="ENG"><s0>Precambrian</s0>
<s2>NX</s2>
</fC07>
<fC07 i1="02" i2="2" l="FRE"><s0>Roche métamorphique</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="02" i2="2" l="ENG"><s0>metamorphic rocks</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="02" i2="2" l="SPA"><s0>Roca metamórfica</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="03" i2="2" l="FRE"><s0>Procaryote</s0>
<s2>NY</s2>
</fC07>
<fC07 i1="03" i2="2" l="ENG"><s0>prokaryotes</s0>
<s2>NY</s2>
</fC07>
<fC07 i1="04" i2="2" l="FRE"><s0>Roche plutonique</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="04" i2="2" l="ENG"><s0>plutonic rocks</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="04" i2="2" l="SPA"><s0>Roca granuda</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="05" i2="2" l="FRE"><s0>Roche ignée</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="05" i2="2" l="ENG"><s0>igneous rocks</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="05" i2="2" l="SPA"><s0>Roca ignea</s0>
<s2>NV</s2>
</fC07>
<fC07 i1="06" i2="2" l="FRE"><s0>Oxyde</s0>
<s2>NZ</s2>
</fC07>
<fC07 i1="06" i2="2" l="ENG"><s0>oxides</s0>
<s2>NZ</s2>
</fC07>
<fC07 i1="06" i2="2" l="SPA"><s0>Óxido</s0>
<s2>NZ</s2>
</fC07>
<fN21><s1>166</s1>
</fN21>
<fN44 i1="01"><s1>PSI</s1>
</fN44>
<fN82><s1>PSI</s1>
</fN82>
</pA>
</standard>
</inist>
<affiliations><list><country><li>Australie</li>
<li>Canada</li>
<li>France</li>
<li>Royaume-Uni</li>
<li>États-Unis</li>
</country>
<region><li>Angleterre</li>
<li>Auvergne-Rhône-Alpes</li>
<li>District de Columbia</li>
<li>Grand Londres</li>
<li>Rhône-Alpes</li>
</region>
<settlement><li>Grenoble</li>
<li>Londres</li>
<li>Washington (district de Columbia)</li>
</settlement>
<orgName><li>Université Joseph Fourier</li>
<li>Université de Londres</li>
</orgName>
</list>
<tree><country name="Canada"><noRegion><name sortKey="Konhauser, Kurt O" sort="Konhauser, Kurt O" uniqKey="Konhauser K" first="Kurt O." last="Konhauser">Kurt O. Konhauser</name>
</noRegion>
<name sortKey="Kamber, Balz S" sort="Kamber, Balz S" uniqKey="Kamber B" first="Balz S." last="Kamber">Balz S. Kamber</name>
<name sortKey="Lalonde, Stefan V" sort="Lalonde, Stefan V" uniqKey="Lalonde S" first="Stefan V." last="Lalonde">Stefan V. Lalonde</name>
<name sortKey="Pecoits, Ernesto" sort="Pecoits, Ernesto" uniqKey="Pecoits E" first="Ernesto" last="Pecoits">Ernesto Pecoits</name>
</country>
<country name="États-Unis"><region name="District de Columbia"><name sortKey="Papineau, Dominic" sort="Papineau, Dominic" uniqKey="Papineau D" first="Dominic" last="Papineau">Dominic Papineau</name>
</region>
<name sortKey="Zahnle, Kevin" sort="Zahnle, Kevin" uniqKey="Zahnle K" first="Kevin" last="Zahnle">Kevin Zahnle</name>
</country>
<country name="Royaume-Uni"><region name="Angleterre"><name sortKey="Nisbet, Euan G" sort="Nisbet, Euan G" uniqKey="Nisbet E" first="Euan G." last="Nisbet">Euan G. Nisbet</name>
</region>
</country>
<country name="Australie"><noRegion><name sortKey="Barley, Mark E" sort="Barley, Mark E" uniqKey="Barley M" first="Mark E." last="Barley">Mark E. Barley</name>
</noRegion>
</country>
<country name="France"><region name="Auvergne-Rhône-Alpes"><name sortKey="Arndt, Nicholas T" sort="Arndt, Nicholas T" uniqKey="Arndt N" first="Nicholas T." last="Arndt">Nicholas T. Arndt</name>
</region>
</country>
</tree>
</affiliations>
</record>

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	Serveur d'exploration sur les relations entre la France et l'Australie
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Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event

Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event

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