Oxygen isotope fractionation in mantle minerals
Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{...
Ausführliche Beschreibung
Gespeichert in:
| Autor*in: |
Zheng, Yongfei [verfasserIn] |
|---|
| Format: |
Artikel |
|---|---|
| Sprache: |
Englisch |
| Erschienen: |
1998 |
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| Schlagwörter: |
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| Anmerkung: |
© Science in China Press 1998 |
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| Übergeordnetes Werk: |
Enthalten in: Science in China / D - Science in China Press, 1996, 41(1998), 1 vom: Apr., Seite 95-103 |
|---|---|
| Übergeordnetes Werk: |
volume:41 ; year:1998 ; number:1 ; month:04 ; pages:95-103 |
| Links: |
|---|
| DOI / URN: |
10.1007/BF02932427 |
|---|
| Katalog-ID: |
OLC2063770433 |
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| 520 | |a Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. | ||
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10.1007/BF02932427 doi (DE-627)OLC2063770433 (DE-He213)BF02932427-p DE-627 ger DE-627 rakwb eng 550 VZ 550 VZ 13 ssgn Zheng, Yongfei verfasserin aut Oxygen isotope fractionation in mantle minerals 1998 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Science in China Press 1998 Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. oxygen isotope fractionation geochemical layering Earth’s interior mantle minerals MgSiO Mg SiO Wei, Chunsheng aut Zhou, Gentao aut Xu, Baolong aut Enthalten in Science in China / D Science in China Press, 1996 41(1998), 1 vom: Apr., Seite 95-103 (DE-627)193118238 (DE-600)1307899-9 (DE-576)062316923 1006-9313 nnns volume:41 year:1998 number:1 month:04 pages:95-103 https://doi.org/10.1007/BF02932427 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-OAS SSG-OLC-MFO SSG-OPC-GGO GBV_ILN_22 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_4082 AR 41 1998 1 04 95-103 |
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10.1007/BF02932427 doi (DE-627)OLC2063770433 (DE-He213)BF02932427-p DE-627 ger DE-627 rakwb eng 550 VZ 550 VZ 13 ssgn Zheng, Yongfei verfasserin aut Oxygen isotope fractionation in mantle minerals 1998 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Science in China Press 1998 Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. oxygen isotope fractionation geochemical layering Earth’s interior mantle minerals MgSiO Mg SiO Wei, Chunsheng aut Zhou, Gentao aut Xu, Baolong aut Enthalten in Science in China / D Science in China Press, 1996 41(1998), 1 vom: Apr., Seite 95-103 (DE-627)193118238 (DE-600)1307899-9 (DE-576)062316923 1006-9313 nnns volume:41 year:1998 number:1 month:04 pages:95-103 https://doi.org/10.1007/BF02932427 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-OAS SSG-OLC-MFO SSG-OPC-GGO GBV_ILN_22 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_4082 AR 41 1998 1 04 95-103 |
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10.1007/BF02932427 doi (DE-627)OLC2063770433 (DE-He213)BF02932427-p DE-627 ger DE-627 rakwb eng 550 VZ 550 VZ 13 ssgn Zheng, Yongfei verfasserin aut Oxygen isotope fractionation in mantle minerals 1998 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Science in China Press 1998 Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. oxygen isotope fractionation geochemical layering Earth’s interior mantle minerals MgSiO Mg SiO Wei, Chunsheng aut Zhou, Gentao aut Xu, Baolong aut Enthalten in Science in China / D Science in China Press, 1996 41(1998), 1 vom: Apr., Seite 95-103 (DE-627)193118238 (DE-600)1307899-9 (DE-576)062316923 1006-9313 nnns volume:41 year:1998 number:1 month:04 pages:95-103 https://doi.org/10.1007/BF02932427 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-OAS SSG-OLC-MFO SSG-OPC-GGO GBV_ILN_22 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_4082 AR 41 1998 1 04 95-103 |
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10.1007/BF02932427 doi (DE-627)OLC2063770433 (DE-He213)BF02932427-p DE-627 ger DE-627 rakwb eng 550 VZ 550 VZ 13 ssgn Zheng, Yongfei verfasserin aut Oxygen isotope fractionation in mantle minerals 1998 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Science in China Press 1998 Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. oxygen isotope fractionation geochemical layering Earth’s interior mantle minerals MgSiO Mg SiO Wei, Chunsheng aut Zhou, Gentao aut Xu, Baolong aut Enthalten in Science in China / D Science in China Press, 1996 41(1998), 1 vom: Apr., Seite 95-103 (DE-627)193118238 (DE-600)1307899-9 (DE-576)062316923 1006-9313 nnns volume:41 year:1998 number:1 month:04 pages:95-103 https://doi.org/10.1007/BF02932427 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-OAS SSG-OLC-MFO SSG-OPC-GGO GBV_ILN_22 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_4082 AR 41 1998 1 04 95-103 |
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10.1007/BF02932427 doi (DE-627)OLC2063770433 (DE-He213)BF02932427-p DE-627 ger DE-627 rakwb eng 550 VZ 550 VZ 13 ssgn Zheng, Yongfei verfasserin aut Oxygen isotope fractionation in mantle minerals 1998 Text txt rdacontent ohne Hilfsmittel zu benutzen n rdamedia Band nc rdacarrier © Science in China Press 1998 Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. oxygen isotope fractionation geochemical layering Earth’s interior mantle minerals MgSiO Mg SiO Wei, Chunsheng aut Zhou, Gentao aut Xu, Baolong aut Enthalten in Science in China / D Science in China Press, 1996 41(1998), 1 vom: Apr., Seite 95-103 (DE-627)193118238 (DE-600)1307899-9 (DE-576)062316923 1006-9313 nnns volume:41 year:1998 number:1 month:04 pages:95-103 https://doi.org/10.1007/BF02932427 lizenzpflichtig Volltext GBV_USEFLAG_A SYSFLAG_A GBV_OLC SSG-OLC-OAS SSG-OLC-MFO SSG-OPC-GGO GBV_ILN_22 GBV_ILN_40 GBV_ILN_65 GBV_ILN_70 GBV_ILN_4082 AR 41 1998 1 04 95-103 |
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Oxygen isotope fractionation in mantle minerals |
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Oxygen isotope fractionation in mantle minerals |
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Zheng, Yongfei |
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Science in China / D |
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1998 |
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Zheng, Yongfei Wei, Chunsheng Zhou, Gentao Xu, Baolong |
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oxygen isotope fractionation in mantle minerals |
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Oxygen isotope fractionation in mantle minerals |
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Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. © Science in China Press 1998 |
| abstractGer |
Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. © Science in China Press 1998 |
| abstract_unstemmed |
Abstract The increment method is adopted to calculate oxygen isotope fractionation factors for mantle minerals, particularly for the polymorphic phases of $ MgSiO_{3} $ and $ Mg_{2} $$ SiO_{4} $. The results predict the following sequence $ of^{18} $O-enrichment:pyroxene (Mg, Fe, Ca)2$ Si_{2} $$ O_{6} $>olivine (Mg, Fe)2$ SiO_{4} $ > spinel (Mg, Fe)2$ SiO_{4} $> ilmenite (Mg, Fe, Ca) $ SiO_{3} $>perovskite (Mg, Fe, Ca) $ SiO_{3} $. The calculated fractionations for the calcite-perovskite ($ CaTiO_{3} $) System are in excellent agreement with the experimental calibrations. If there would be complete isotopic equilibration in the mantle, the spinel-structured silicates in the transition zone are predicted to be enriched $ in^{18} $O relative to the perovskite-structured silicates in the lower mantle but depleted $ in^{18} $O relative to olivines and pyroxenes in the upper mantle. The oxygen isotope layering of the mantle might result from differences in the chemical composition and crystal structure of mineral phases at different mantle depths. Assuming isotopic equilibrium on a whole earth scale, the chemical structure of the Earth’s interior can be described by the following sequence $ of^{18} $O-enrichment:upper crust>lower crust>upper mantle>transition zone>lower mantle>core. © Science in China Press 1998 |
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