The buffering capacity of lithospheric mantle: implications for diamond formation
Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the...
Ausführliche Beschreibung
Autor*in: |
Luth, Robert W. [verfasserIn] Stachel, Thomas [verfasserIn] |
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E-Artikel |
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Sprache: |
Englisch |
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2014 |
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Übergeordnetes Werk: |
Enthalten in: Contributions to mineralogy and petrology - Berlin : Springer, 1947, 168(2014), 5 vom: 08. Nov. |
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Übergeordnetes Werk: |
volume:168 ; year:2014 ; number:5 ; day:08 ; month:11 |
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DOI / URN: |
10.1007/s00410-014-1083-6 |
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Katalog-ID: |
SPR005255260 |
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100 | 1 | |a Luth, Robert W. |e verfasserin |4 aut | |
245 | 1 | 4 | |a The buffering capacity of lithospheric mantle: implications for diamond formation |
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520 | |a Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. | ||
650 | 4 | |a Mantle petrology |7 (dpeaa)DE-He213 | |
650 | 4 | |a Diamonds |7 (dpeaa)DE-He213 | |
650 | 4 | |a Oxygen barometry |7 (dpeaa)DE-He213 | |
650 | 4 | |a Mantle oxidation state |7 (dpeaa)DE-He213 | |
650 | 4 | |a CHO fluid |7 (dpeaa)DE-He213 | |
700 | 1 | |a Stachel, Thomas |e verfasserin |4 aut | |
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10.1007/s00410-014-1083-6 doi (DE-627)SPR005255260 (SPR)s00410-014-1083-6-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Luth, Robert W. verfasserin aut The buffering capacity of lithospheric mantle: implications for diamond formation 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 Stachel, Thomas verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 168(2014), 5 vom: 08. Nov. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:168 year:2014 number:5 day:08 month:11 https://dx.doi.org/10.1007/s00410-014-1083-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_267 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 168 2014 5 08 11 |
spelling |
10.1007/s00410-014-1083-6 doi (DE-627)SPR005255260 (SPR)s00410-014-1083-6-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Luth, Robert W. verfasserin aut The buffering capacity of lithospheric mantle: implications for diamond formation 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 Stachel, Thomas verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 168(2014), 5 vom: 08. Nov. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:168 year:2014 number:5 day:08 month:11 https://dx.doi.org/10.1007/s00410-014-1083-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_267 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 168 2014 5 08 11 |
allfields_unstemmed |
10.1007/s00410-014-1083-6 doi (DE-627)SPR005255260 (SPR)s00410-014-1083-6-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Luth, Robert W. verfasserin aut The buffering capacity of lithospheric mantle: implications for diamond formation 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 Stachel, Thomas verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 168(2014), 5 vom: 08. Nov. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:168 year:2014 number:5 day:08 month:11 https://dx.doi.org/10.1007/s00410-014-1083-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_267 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 168 2014 5 08 11 |
allfieldsGer |
10.1007/s00410-014-1083-6 doi (DE-627)SPR005255260 (SPR)s00410-014-1083-6-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Luth, Robert W. verfasserin aut The buffering capacity of lithospheric mantle: implications for diamond formation 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 Stachel, Thomas verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 168(2014), 5 vom: 08. Nov. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:168 year:2014 number:5 day:08 month:11 https://dx.doi.org/10.1007/s00410-014-1083-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_267 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 168 2014 5 08 11 |
allfieldsSound |
10.1007/s00410-014-1083-6 doi (DE-627)SPR005255260 (SPR)s00410-014-1083-6-e DE-627 ger DE-627 rakwb eng 550 ASE 38.25 bkl 38.30 bkl Luth, Robert W. verfasserin aut The buffering capacity of lithospheric mantle: implications for diamond formation 2014 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 Stachel, Thomas verfasserin aut Enthalten in Contributions to mineralogy and petrology Berlin : Springer, 1947 168(2014), 5 vom: 08. Nov. (DE-627)25372208X (DE-600)1458979-5 1432-0967 nnns volume:168 year:2014 number:5 day:08 month:11 https://dx.doi.org/10.1007/s00410-014-1083-6 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER SSG-OPC-GGO SSG-OPC-ASE GBV_ILN_11 GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 GBV_ILN_39 GBV_ILN_40 GBV_ILN_60 GBV_ILN_62 GBV_ILN_63 GBV_ILN_65 GBV_ILN_69 GBV_ILN_70 GBV_ILN_73 GBV_ILN_74 GBV_ILN_90 GBV_ILN_95 GBV_ILN_100 GBV_ILN_105 GBV_ILN_110 GBV_ILN_120 GBV_ILN_138 GBV_ILN_150 GBV_ILN_151 GBV_ILN_152 GBV_ILN_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_206 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_267 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 GBV_ILN_381 GBV_ILN_602 GBV_ILN_636 GBV_ILN_702 GBV_ILN_2001 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2006 GBV_ILN_2007 GBV_ILN_2008 GBV_ILN_2009 GBV_ILN_2010 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2026 GBV_ILN_2027 GBV_ILN_2031 GBV_ILN_2034 GBV_ILN_2037 GBV_ILN_2038 GBV_ILN_2039 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2055 GBV_ILN_2056 GBV_ILN_2057 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2070 GBV_ILN_2086 GBV_ILN_2088 GBV_ILN_2093 GBV_ILN_2106 GBV_ILN_2107 GBV_ILN_2108 GBV_ILN_2110 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2116 GBV_ILN_2118 GBV_ILN_2119 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2144 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2188 GBV_ILN_2190 GBV_ILN_2232 GBV_ILN_2336 GBV_ILN_2446 GBV_ILN_2470 GBV_ILN_2472 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_2548 GBV_ILN_4012 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4246 GBV_ILN_4249 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4306 GBV_ILN_4307 GBV_ILN_4313 GBV_ILN_4322 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4325 GBV_ILN_4326 GBV_ILN_4328 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 38.25 ASE 38.30 ASE AR 168 2014 5 08 11 |
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Enthalten in Contributions to mineralogy and petrology 168(2014), 5 vom: 08. Nov. volume:168 year:2014 number:5 day:08 month:11 |
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Enthalten in Contributions to mineralogy and petrology 168(2014), 5 vom: 08. Nov. volume:168 year:2014 number:5 day:08 month:11 |
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Luth, Robert W. @@aut@@ Stachel, Thomas @@aut@@ |
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<?xml version="1.0" encoding="UTF-8"?><collection xmlns="http://www.loc.gov/MARC21/slim"><record><leader>01000caa a22002652 4500</leader><controlfield tag="001">SPR005255260</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20220110181558.0</controlfield><controlfield tag="007">cr uuu---uuuuu</controlfield><controlfield tag="008">201001s2014 xx |||||o 00| ||eng c</controlfield><datafield tag="024" ind1="7" ind2=" "><subfield code="a">10.1007/s00410-014-1083-6</subfield><subfield code="2">doi</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)SPR005255260</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(SPR)s00410-014-1083-6-e</subfield></datafield><datafield tag="040" ind1=" " ind2=" "><subfield code="a">DE-627</subfield><subfield code="b">ger</subfield><subfield code="c">DE-627</subfield><subfield code="e">rakwb</subfield></datafield><datafield tag="041" ind1=" " ind2=" "><subfield code="a">eng</subfield></datafield><datafield tag="082" ind1="0" ind2="4"><subfield code="a">550</subfield><subfield code="q">ASE</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">38.25</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">38.30</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="100" ind1="1" ind2=" "><subfield code="a">Luth, Robert W.</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="245" ind1="1" ind2="4"><subfield code="a">The buffering capacity of lithospheric mantle: implications for diamond formation</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">2014</subfield></datafield><datafield tag="336" ind1=" " ind2=" "><subfield code="a">Text</subfield><subfield code="b">txt</subfield><subfield code="2">rdacontent</subfield></datafield><datafield tag="337" ind1=" " ind2=" "><subfield code="a">Computermedien</subfield><subfield code="b">c</subfield><subfield code="2">rdamedia</subfield></datafield><datafield tag="338" ind1=" " ind2=" "><subfield code="a">Online-Ressource</subfield><subfield code="b">cr</subfield><subfield code="2">rdacarrier</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites.</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Mantle petrology</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Diamonds</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Oxygen barometry</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Mantle oxidation state</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">CHO fluid</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Stachel, Thomas</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="t">Contributions to mineralogy and petrology</subfield><subfield code="d">Berlin : Springer, 1947</subfield><subfield code="g">168(2014), 5 vom: 08. 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|
author |
Luth, Robert W. |
spellingShingle |
Luth, Robert W. ddc 550 bkl 38.25 bkl 38.30 misc Mantle petrology misc Diamonds misc Oxygen barometry misc Mantle oxidation state misc CHO fluid The buffering capacity of lithospheric mantle: implications for diamond formation |
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Luth, Robert W. |
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550 - Earth sciences |
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1432-0967 |
topic_title |
550 ASE 38.25 bkl 38.30 bkl The buffering capacity of lithospheric mantle: implications for diamond formation Mantle petrology (dpeaa)DE-He213 Diamonds (dpeaa)DE-He213 Oxygen barometry (dpeaa)DE-He213 Mantle oxidation state (dpeaa)DE-He213 CHO fluid (dpeaa)DE-He213 |
topic |
ddc 550 bkl 38.25 bkl 38.30 misc Mantle petrology misc Diamonds misc Oxygen barometry misc Mantle oxidation state misc CHO fluid |
topic_unstemmed |
ddc 550 bkl 38.25 bkl 38.30 misc Mantle petrology misc Diamonds misc Oxygen barometry misc Mantle oxidation state misc CHO fluid |
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ddc 550 bkl 38.25 bkl 38.30 misc Mantle petrology misc Diamonds misc Oxygen barometry misc Mantle oxidation state misc CHO fluid |
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Elektronische Aufsätze Aufsätze Elektronische Ressource |
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The buffering capacity of lithospheric mantle: implications for diamond formation |
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title_full |
The buffering capacity of lithospheric mantle: implications for diamond formation |
author_sort |
Luth, Robert W. |
journal |
Contributions to mineralogy and petrology |
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Contributions to mineralogy and petrology |
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eng |
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500 - Science |
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2014 |
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txt |
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Luth, Robert W. Stachel, Thomas |
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168 |
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550 ASE 38.25 bkl 38.30 bkl |
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Elektronische Aufsätze |
author-letter |
Luth, Robert W. |
doi_str_mv |
10.1007/s00410-014-1083-6 |
dewey-full |
550 |
author2-role |
verfasserin |
title_sort |
buffering capacity of lithospheric mantle: implications for diamond formation |
title_auth |
The buffering capacity of lithospheric mantle: implications for diamond formation |
abstract |
Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. |
abstractGer |
Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. |
abstract_unstemmed |
Abstract Current models for the formation of natural diamond involve either oxidation of a methane-bearing fluid by reaction with oxidized mantle, or reduction of a carbonate-bearing fluid (or melt) by reaction with reduced mantle. Implicit in both models is the ability of the mantle with which the fluid equilibrates to act as an oxidizing or reducing agent, or more simply, to act as a source or sink of $ O_{2} $. If only redox reactions involving iron are operating, the ability of mantle peridotite to fulfill this role in diamond formation may not be sufficient for either model to be viable. Using the recent experimental recalibration of olivine–orthopyroxene–garnet oxybarometers of Stagno et al. (2013), we re-evaluated the global database of ~200 garnet peridotite samples for which the requisite $ Fe^{3+} $/$ Fe^{2+} $ data for garnet exist. Relative to the previous calibration of Gudmundsson and Wood (1995), the new calibration yields somewhat more oxidized values of Δlog f$ O_{2} $ (FMQ), with the divergence increasing from <0.5 units of log f$ O_{2} $ at ~3 GPa to as much as 1.5 units at 5–6.5 GPa. Globally, there is a range of ~4 log units f$ O_{2} $ for samples from the diamond stability field at any given pressure. Most samples are sufficiently reduced such that diamond, rather than carbonate, would be stable, and CHO fluids at these conditions would be $ H_{2} $O-rich (>60 mol%), with $ CH_{4} $ being the next most abundant species. To ascertain the capacity for mantle peridotite to act as a source or sink of $ O_{2} $, we developed a new model to calculate the f$ O_{2} $ for a peridotite at a given P, T, and $ Fe^{3+} $/$ Fe^{2+} $. The results from this model predict 50 ppm or less $ O_{2} $ is required to shift a depleted mantle peridotite the observed four log units of f$ O_{2} $. Coupled with the observed distribution of samples at values of f$ O_{2} $ intermediate between the most reduced (metal-saturated) and most oxidized (carbonate-saturated) possible values for diamond stability, these results demonstrate that peridotites are very poor sinks or sources of $ O_{2} $ for possible redox reactions to form diamond. A corollary of the poor redox buffering capacity of cratonic peridotites is that they can be employed as faithful indicators of the redox state of the last metasomatic fluid that passed through them. We propose that diamond formation from CHO fluids is a predictable consequence either of isobaric cooling or of combined cooling and decompression of the fluid as it migrates upward in the lithosphere. This establishes a petrological basis for the observed close connection between subcalcic garnet and diamond: based on high solidus temperatures of harzburgite and dunite effectively precluding dilution of CHO fluids through incipient melts, such highly depleted cratonic peridotites are the preferred locus of diamond formation. Due to a rapid increase in solidus temperature with increasing $ CH_{4} $ content of the fluid, diamond formation related to reduced CHO fluids may also occur in some cratonic lherzolites. |
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container_issue |
5 |
title_short |
The buffering capacity of lithospheric mantle: implications for diamond formation |
url |
https://dx.doi.org/10.1007/s00410-014-1083-6 |
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score |
7.399288 |