Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton
Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall...
Ausführliche Beschreibung
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| Autor*in: |
Orsoev, D. A. [verfasserIn] |
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| Format: |
E-Artikel |
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| Sprache: |
Englisch |
| Erschienen: |
2010 |
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| Schlagwörter: |
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| Anmerkung: |
© Pleiades Publishing, Ltd. 2010 |
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| Übergeordnetes Werk: |
Enthalten in: Geology of ore deposits - Berlin : Springer Science + Business Media B.V., 2006, 52(2010), 7 vom: Dez., Seite 543-550 |
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| Übergeordnetes Werk: |
volume:52 ; year:2010 ; number:7 ; month:12 ; pages:543-550 |
| Links: |
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| DOI / URN: |
10.1134/S1075701510070032 |
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| Katalog-ID: |
SPR019983433 |
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| 520 | |a Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. | ||
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10.1134/S1075701510070032 doi (DE-627)SPR019983433 (SPR)S1075701510070032-e DE-627 ger DE-627 rakwb eng Orsoev, D. A. verfasserin aut Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton 2010 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2010 Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 Enthalten in Geology of ore deposits Berlin : Springer Science + Business Media B.V., 2006 52(2010), 7 vom: Dez., Seite 543-550 (DE-627)510462294 (DE-600)2230159-8 1555-6476 nnns volume:52 year:2010 number:7 month:12 pages:543-550 https://dx.doi.org/10.1134/S1075701510070032 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER 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_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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_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_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 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_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 52 2010 7 12 543-550 |
| spelling |
10.1134/S1075701510070032 doi (DE-627)SPR019983433 (SPR)S1075701510070032-e DE-627 ger DE-627 rakwb eng Orsoev, D. A. verfasserin aut Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton 2010 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2010 Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 Enthalten in Geology of ore deposits Berlin : Springer Science + Business Media B.V., 2006 52(2010), 7 vom: Dez., Seite 543-550 (DE-627)510462294 (DE-600)2230159-8 1555-6476 nnns volume:52 year:2010 number:7 month:12 pages:543-550 https://dx.doi.org/10.1134/S1075701510070032 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER 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_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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_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_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 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_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 52 2010 7 12 543-550 |
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10.1134/S1075701510070032 doi (DE-627)SPR019983433 (SPR)S1075701510070032-e DE-627 ger DE-627 rakwb eng Orsoev, D. A. verfasserin aut Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton 2010 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2010 Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 Enthalten in Geology of ore deposits Berlin : Springer Science + Business Media B.V., 2006 52(2010), 7 vom: Dez., Seite 543-550 (DE-627)510462294 (DE-600)2230159-8 1555-6476 nnns volume:52 year:2010 number:7 month:12 pages:543-550 https://dx.doi.org/10.1134/S1075701510070032 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER 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_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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_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_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 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_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 52 2010 7 12 543-550 |
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10.1134/S1075701510070032 doi (DE-627)SPR019983433 (SPR)S1075701510070032-e DE-627 ger DE-627 rakwb eng Orsoev, D. A. verfasserin aut Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton 2010 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2010 Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 Enthalten in Geology of ore deposits Berlin : Springer Science + Business Media B.V., 2006 52(2010), 7 vom: Dez., Seite 543-550 (DE-627)510462294 (DE-600)2230159-8 1555-6476 nnns volume:52 year:2010 number:7 month:12 pages:543-550 https://dx.doi.org/10.1134/S1075701510070032 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER 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_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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_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_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 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_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 52 2010 7 12 543-550 |
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10.1134/S1075701510070032 doi (DE-627)SPR019983433 (SPR)S1075701510070032-e DE-627 ger DE-627 rakwb eng Orsoev, D. A. verfasserin aut Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton 2010 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Pleiades Publishing, Ltd. 2010 Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 Enthalten in Geology of ore deposits Berlin : Springer Science + Business Media B.V., 2006 52(2010), 7 vom: Dez., Seite 543-550 (DE-627)510462294 (DE-600)2230159-8 1555-6476 nnns volume:52 year:2010 number:7 month:12 pages:543-550 https://dx.doi.org/10.1134/S1075701510070032 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_SPRINGER 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_161 GBV_ILN_170 GBV_ILN_171 GBV_ILN_187 GBV_ILN_213 GBV_ILN_224 GBV_ILN_230 GBV_ILN_250 GBV_ILN_281 GBV_ILN_285 GBV_ILN_293 GBV_ILN_370 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_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_4035 GBV_ILN_4037 GBV_ILN_4046 GBV_ILN_4112 GBV_ILN_4125 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_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4336 GBV_ILN_4338 GBV_ILN_4393 GBV_ILN_4700 AR 52 2010 7 12 543-550 |
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Enthalten in Geology of ore deposits 52(2010), 7 vom: Dez., Seite 543-550 volume:52 year:2010 number:7 month:12 pages:543-550 |
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Orsoev, D. A. |
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Orsoev, D. A. misc Olivine misc Oxygen Isotopic Composition misc Critical Zone misc Olivine Gabbro misc Olivine Gabbronorite Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton |
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Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton Olivine (dpeaa)DE-He213 Oxygen Isotopic Composition (dpeaa)DE-He213 Critical Zone (dpeaa)DE-He213 Olivine Gabbro (dpeaa)DE-He213 Olivine Gabbronorite (dpeaa)DE-He213 |
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Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton |
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Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton |
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distribution of oxygen isotopes in rocks and minerals from the critical zone of the ioko-dovyren pluton |
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Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton |
| abstract |
Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. © Pleiades Publishing, Ltd. 2010 |
| abstractGer |
Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. © Pleiades Publishing, Ltd. 2010 |
| abstract_unstemmed |
Abstract The oxygen isotopic composition was studied in minerals and rocks from the critical zone of the Ioko-Dovyren layered pluton. The $ δ^{18} $O values vary from +5.4 to +6.1‰ in rocks, from +4.8 to +5.8‰ in olivine, from +5.5 to 6.5‰ in pyroxene, and from +5.8 to +6.9‰ in plagioclase and fall into the interval of mantle values for continental mafic and ultramafic rocks. A decrease in $ δ^{18} $O could have been caused by penetration of meteoric water. Postmagmatic (retrograde) oxygen isotopic redistribution in the slowly cooling rocks is responsible for disturbance of oxygen isotope equilibria in the coexisting minerals, which were crystallized from the same magma at a high temperature. The nonequilibrium oxygen isotopic composition in the associated minerals and calculated temperature of the final isotopic equilibration do not contradict the model of “fluid” formation of low-sulfide PGE mineralization in the Ioko-Dovyren layered pluton. © Pleiades Publishing, Ltd. 2010 |
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Distribution of oxygen isotopes in rocks and minerals from the critical zone of the Ioko-Dovyren pluton |
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https://dx.doi.org/10.1134/S1075701510070032 |
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10.1134/S1075701510070032 |
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