Iodine abundances in oceanic basalts: implications for Earth dynamics
Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of o...
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E-Artikel |
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Englisch |
| Erschienen: |
1992 |
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Elsevier Journal Backfiles on ScienceDirect 1907 - 2002 |
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| Übergeordnetes Werk: |
in: Earth and Planetary Science Letters - Amsterdam : Elsevier, 108(1992), 4, Seite 217-227 |
| Übergeordnetes Werk: |
volume:108 ; year:1992 ; number:4 ; pages:217-227 |
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| 520 | |a Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. | ||
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(DE-627)NLEJ180726749 (DE-599)GBVNLZ180726749 DE-627 ger DE-627 rakwb eng Iodine abundances in oceanic basalts: implications for Earth dynamics 1992 nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. Elsevier Journal Backfiles on ScienceDirect 1907 - 2002 Deruelle, B. oth Dreibus, G. oth Jambon, A. oth in Earth and Planetary Science Letters Amsterdam : Elsevier 108(1992), 4, Seite 217-227 (DE-627)NLEJ177233850 (DE-600)1466659-5 0012-821X nnns volume:108 year:1992 number:4 pages:217-227 http://linkinghub.elsevier.com/retrieve/pii/0012-821X(92)90024-P GBV_USEFLAG_H ZDB-1-SDJ GBV_NL_ARTICLE AR 108 1992 4 217-227 |
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(DE-627)NLEJ180726749 (DE-599)GBVNLZ180726749 DE-627 ger DE-627 rakwb eng Iodine abundances in oceanic basalts: implications for Earth dynamics 1992 nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. Elsevier Journal Backfiles on ScienceDirect 1907 - 2002 Deruelle, B. oth Dreibus, G. oth Jambon, A. oth in Earth and Planetary Science Letters Amsterdam : Elsevier 108(1992), 4, Seite 217-227 (DE-627)NLEJ177233850 (DE-600)1466659-5 0012-821X nnns volume:108 year:1992 number:4 pages:217-227 http://linkinghub.elsevier.com/retrieve/pii/0012-821X(92)90024-P GBV_USEFLAG_H ZDB-1-SDJ GBV_NL_ARTICLE AR 108 1992 4 217-227 |
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(DE-627)NLEJ180726749 (DE-599)GBVNLZ180726749 DE-627 ger DE-627 rakwb eng Iodine abundances in oceanic basalts: implications for Earth dynamics 1992 nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. Elsevier Journal Backfiles on ScienceDirect 1907 - 2002 Deruelle, B. oth Dreibus, G. oth Jambon, A. oth in Earth and Planetary Science Letters Amsterdam : Elsevier 108(1992), 4, Seite 217-227 (DE-627)NLEJ177233850 (DE-600)1466659-5 0012-821X nnns volume:108 year:1992 number:4 pages:217-227 http://linkinghub.elsevier.com/retrieve/pii/0012-821X(92)90024-P GBV_USEFLAG_H ZDB-1-SDJ GBV_NL_ARTICLE AR 108 1992 4 217-227 |
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(DE-627)NLEJ180726749 (DE-599)GBVNLZ180726749 DE-627 ger DE-627 rakwb eng Iodine abundances in oceanic basalts: implications for Earth dynamics 1992 nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. Elsevier Journal Backfiles on ScienceDirect 1907 - 2002 Deruelle, B. oth Dreibus, G. oth Jambon, A. oth in Earth and Planetary Science Letters Amsterdam : Elsevier 108(1992), 4, Seite 217-227 (DE-627)NLEJ177233850 (DE-600)1466659-5 0012-821X nnns volume:108 year:1992 number:4 pages:217-227 http://linkinghub.elsevier.com/retrieve/pii/0012-821X(92)90024-P GBV_USEFLAG_H ZDB-1-SDJ GBV_NL_ARTICLE AR 108 1992 4 217-227 |
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Iodine abundances in oceanic basalts: implications for Earth dynamics |
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Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. |
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Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. |
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Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer. |
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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">NLEJ180726749</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20210706133911.0</controlfield><controlfield tag="007">cr uuu---uuuuu</controlfield><controlfield tag="008">070505s1992 xx |||||o 00| ||eng c</controlfield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)NLEJ180726749</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-599)GBVNLZ180726749</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="245" ind1="1" ind2="0"><subfield code="a">Iodine abundances in oceanic basalts: implications for Earth dynamics</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">1992</subfield></datafield><datafield tag="336" ind1=" " ind2=" "><subfield code="a">nicht spezifiziert</subfield><subfield code="b">zzz</subfield><subfield code="2">rdacontent</subfield></datafield><datafield tag="337" ind1=" " ind2=" "><subfield code="a">nicht spezifiziert</subfield><subfield code="b">z</subfield><subfield code="2">rdamedia</subfield></datafield><datafield tag="338" ind1=" " ind2=" "><subfield code="a">nicht spezifiziert</subfield><subfield code="b">zu</subfield><subfield code="2">rdacarrier</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Iodine analyses by neutron activation have been performed on 32 oceanic basalts glasses, 1 phonolite and 3 subaerial arc basalts. The world-wide sample set encompasses all typical geodynamic settings [ridges (MORB), oceanic islands (OIB), arcs (IAB) and back-arc basins (BABB)] and the diversity of oceanic basalt types [depleted (N), intermediate (T) and enriched (P)]. Most basalts, including all N-types, all but one T-type, and some P-types, exhibit low iodine concentrations (2.5-13 ppb). Very high I concentrations (up to 363 ppb) in a small number of samples (all P-types) are interpreted to be the result of a recycled component which includes organic matter of sedimentary origin (sediment organic matter accounts for about 80% of total terrestrial iodine). Iodine appears to be the most incompatible element after the noble gases. Mass balance considerations permit the mantle iodine concentration and hence the bulk silicate abundance of the Earth to be constrained to 9-24 ppb, with a preferred value of 10 ppb. The low terrestrial iodine abundance, coupled with a chondrite-like chlorine/iodine ratio, strongly favours the late veneer model of Earth accretion. The scenario proposed to explain the terrestrial iodine distribution includes heterogeneous accretion, iodine extraction from the mantle simultaneous with (or even before) continent formation, and depleted mantle homogenization. As iodine is not recycled into the mantle by oceanic crust, heterogeneities in the mantle should result from organic sediment (C) recycling, of which iodine may be a good tracer.</subfield></datafield><datafield tag="533" ind1=" " ind2=" "><subfield code="f">Elsevier Journal Backfiles on ScienceDirect 1907 - 2002</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Deruelle, B.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Dreibus, G.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Jambon, A.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">in</subfield><subfield code="t">Earth and Planetary Science Letters</subfield><subfield code="d">Amsterdam : Elsevier</subfield><subfield code="g">108(1992), 4, Seite 217-227</subfield><subfield code="w">(DE-627)NLEJ177233850</subfield><subfield code="w">(DE-600)1466659-5</subfield><subfield code="x">0012-821X</subfield><subfield code="7">nnns</subfield></datafield><datafield tag="773" ind1="1" ind2="8"><subfield code="g">volume:108</subfield><subfield code="g">year:1992</subfield><subfield code="g">number:4</subfield><subfield code="g">pages:217-227</subfield></datafield><datafield tag="856" ind1="4" ind2="0"><subfield code="u">http://linkinghub.elsevier.com/retrieve/pii/0012-821X(92)90024-P</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_USEFLAG_H</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">ZDB-1-SDJ</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_NL_ARTICLE</subfield></datafield><datafield tag="951" ind1=" " ind2=" "><subfield code="a">AR</subfield></datafield><datafield tag="952" ind1=" " ind2=" "><subfield code="d">108</subfield><subfield code="j">1992</subfield><subfield code="e">4</subfield><subfield code="h">217-227</subfield></datafield></record></collection>
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