Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data
Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data...
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| Autor*in: |
Chenyi, Marie-Louise Vohnyui [verfasserIn] |
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| Format: |
E-Artikel |
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| Sprache: |
Englisch |
| Erschienen: |
2024 |
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© Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. |
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Enthalten in: Arabian journal of geosciences - Springer International Publishing, 2008, 17(2024), 3 vom: 28. Feb. |
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volume:17 ; year:2024 ; number:3 ; day:28 ; month:02 |
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| DOI / URN: |
10.1007/s12517-024-11906-7 |
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| Katalog-ID: |
SPR054952352 |
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| 245 | 1 | 0 | |a Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data |
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| 520 | |a Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. | ||
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| 650 | 4 | |a Mantle xenoliths |7 (dpeaa)DE-He213 | |
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| 650 | 4 | |a Moho depth |7 (dpeaa)DE-He213 | |
| 650 | 4 | |a Lithospheric mantle upwelling |7 (dpeaa)DE-He213 | |
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| 700 | 1 | |a Bardintzeff, Jacques-Marie |4 aut | |
| 700 | 1 | |a Njueya, Adoua Kopa |4 aut | |
| 700 | 1 | |a Nkouathio, David Guimolaire |4 aut | |
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10.1007/s12517-024-11906-7 doi (DE-627)SPR054952352 (SPR)s12517-024-11906-7-e DE-627 ger DE-627 rakwb eng 550 VZ Chenyi, Marie-Louise Vohnyui verfasserin aut Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data 2024 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 Wotchoko, Pierre aut Bardintzeff, Jacques-Marie aut Njueya, Adoua Kopa aut Nkouathio, David Guimolaire aut Enthalten in Arabian journal of geosciences Springer International Publishing, 2008 17(2024), 3 vom: 28. Feb. (DE-627)572421877 (DE-600)2438771-X 1866-7538 nnns volume:17 year:2024 number:3 day:28 month:02 https://dx.doi.org/10.1007/s12517-024-11906-7 lizenzpflichtig Volltext SYSFLAG_0 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_152 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_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_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_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_2118 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_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 AR 17 2024 3 28 02 |
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10.1007/s12517-024-11906-7 doi (DE-627)SPR054952352 (SPR)s12517-024-11906-7-e DE-627 ger DE-627 rakwb eng 550 VZ Chenyi, Marie-Louise Vohnyui verfasserin aut Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data 2024 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 Wotchoko, Pierre aut Bardintzeff, Jacques-Marie aut Njueya, Adoua Kopa aut Nkouathio, David Guimolaire aut Enthalten in Arabian journal of geosciences Springer International Publishing, 2008 17(2024), 3 vom: 28. Feb. (DE-627)572421877 (DE-600)2438771-X 1866-7538 nnns volume:17 year:2024 number:3 day:28 month:02 https://dx.doi.org/10.1007/s12517-024-11906-7 lizenzpflichtig Volltext SYSFLAG_0 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_152 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_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_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_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_2118 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_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 AR 17 2024 3 28 02 |
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10.1007/s12517-024-11906-7 doi (DE-627)SPR054952352 (SPR)s12517-024-11906-7-e DE-627 ger DE-627 rakwb eng 550 VZ Chenyi, Marie-Louise Vohnyui verfasserin aut Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data 2024 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 Wotchoko, Pierre aut Bardintzeff, Jacques-Marie aut Njueya, Adoua Kopa aut Nkouathio, David Guimolaire aut Enthalten in Arabian journal of geosciences Springer International Publishing, 2008 17(2024), 3 vom: 28. Feb. (DE-627)572421877 (DE-600)2438771-X 1866-7538 nnns volume:17 year:2024 number:3 day:28 month:02 https://dx.doi.org/10.1007/s12517-024-11906-7 lizenzpflichtig Volltext SYSFLAG_0 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_152 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_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_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_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_2118 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_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 AR 17 2024 3 28 02 |
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10.1007/s12517-024-11906-7 doi (DE-627)SPR054952352 (SPR)s12517-024-11906-7-e DE-627 ger DE-627 rakwb eng 550 VZ Chenyi, Marie-Louise Vohnyui verfasserin aut Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data 2024 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 Wotchoko, Pierre aut Bardintzeff, Jacques-Marie aut Njueya, Adoua Kopa aut Nkouathio, David Guimolaire aut Enthalten in Arabian journal of geosciences Springer International Publishing, 2008 17(2024), 3 vom: 28. Feb. (DE-627)572421877 (DE-600)2438771-X 1866-7538 nnns volume:17 year:2024 number:3 day:28 month:02 https://dx.doi.org/10.1007/s12517-024-11906-7 lizenzpflichtig Volltext SYSFLAG_0 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_152 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_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_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_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_2118 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_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 AR 17 2024 3 28 02 |
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10.1007/s12517-024-11906-7 doi (DE-627)SPR054952352 (SPR)s12517-024-11906-7-e DE-627 ger DE-627 rakwb eng 550 VZ Chenyi, Marie-Louise Vohnyui verfasserin aut Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data 2024 Text txt rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 Wotchoko, Pierre aut Bardintzeff, Jacques-Marie aut Njueya, Adoua Kopa aut Nkouathio, David Guimolaire aut Enthalten in Arabian journal of geosciences Springer International Publishing, 2008 17(2024), 3 vom: 28. Feb. (DE-627)572421877 (DE-600)2438771-X 1866-7538 nnns volume:17 year:2024 number:3 day:28 month:02 https://dx.doi.org/10.1007/s12517-024-11906-7 lizenzpflichtig Volltext SYSFLAG_0 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_152 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_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_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_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_2118 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_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 AR 17 2024 3 28 02 |
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Enthalten in Arabian journal of geosciences 17(2024), 3 vom: 28. Feb. volume:17 year:2024 number:3 day:28 month:02 |
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Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law.</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL.</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Oku Volcanic Complex</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Mantle xenoliths</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Teleseismic receiver function</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Moho depth</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="650" ind1=" " ind2="4"><subfield code="a">Lithospheric mantle upwelling</subfield><subfield code="7">(dpeaa)DE-He213</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Wotchoko, Pierre</subfield><subfield code="4">aut</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Bardintzeff, Jacques-Marie</subfield><subfield code="4">aut</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Njueya, Adoua Kopa</subfield><subfield code="4">aut</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Nkouathio, David Guimolaire</subfield><subfield code="4">aut</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="t">Arabian journal of geosciences</subfield><subfield code="d">Springer International Publishing, 2008</subfield><subfield code="g">17(2024), 3 vom: 28. 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Chenyi, Marie-Louise Vohnyui |
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Chenyi, Marie-Louise Vohnyui ddc 550 misc Oku Volcanic Complex misc Mantle xenoliths misc Teleseismic receiver function misc Moho depth misc Lithospheric mantle upwelling Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data |
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550 VZ Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data Oku Volcanic Complex (dpeaa)DE-He213 Mantle xenoliths (dpeaa)DE-He213 Teleseismic receiver function (dpeaa)DE-He213 Moho depth (dpeaa)DE-He213 Lithospheric mantle upwelling (dpeaa)DE-He213 |
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Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data |
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Chenyi, Marie-Louise Vohnyui Wotchoko, Pierre Bardintzeff, Jacques-Marie Njueya, Adoua Kopa Nkouathio, David Guimolaire |
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depth of the lithospheric mantle discontinuities beneath the northwest flank of oku volcanic complex, cameroon volcanic line: constraints from mantle xenolith and teleseismic data |
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Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data |
| abstract |
Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. |
| abstractGer |
Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. |
| abstract_unstemmed |
Abstract In Northwestern Cameroon, the northwest flank of Oku Volcanic Complex forms part of the continental sector of the Cameroon Volcanic Line (CVL). Detailed study of petrology and mineral chemistry of nine mantle xenoliths from the NW flank of Oku Volcanic Complex with derived teleseismic data have been conducted to determine the nature and depth of the lithospheric mantle beneath the flank and CVL as a whole. Petrographically, mantle xenoliths are olivine websterite and plagioclase-spinel lherzolite consisting of a five-phase mineral assemblage (olivine, orthopyroxene, clinopyroxene, spinel and plagioclase) with varied textural changes (protogranular, porphyroclastic and porphyroblastic) characterizing the equilibrium conditions of the upper mantle. Mineralogically, magnesian olivine (forsterite and chrysolite), clinopyroxene (diopside), and orthopyroxene (clinoenstatite) with plagioclases (labradorite with rare bytownite) dominate. We propose hereditary representations to explain the occurrence of plagioclase in the mantle peridotites. (1) Subsolidus transformation of spinel to plagioclase, (2) crystallisation of melt pockets from partial melting of the upper mantle and (3) accumulations from melts that impregnated the lithospheric mantle. Velocity and synthetic models obtained from the inversion of the receiver functions indicate that the Moho depth or crustal discontinuity is 33.2 km for CM20 and 40.8 km for CM23 with a mean thickness of 37 km. The lithospheric mantle thickness is 28.1 km and 20.5 km for CM20 and CM23 respectively with a mean thickness of 24.3 km. The low velocity zone is located at intervals of 61.3 to 113 km, exhibiting a thickness of 51.7 km and 42.5 km for CM20 and CM23 respectively, resulting in a mean thickness of 47.05 km. The discontinuities are located at 37 km for the Mohorovicic discontinuity and between 61.3 km and 61.5 km for the Lithospheric-Asthenospheric Boundary. The occurrence of plagioclase in the mantle peridotite, coupled with results from the receiver function techniques, provides evidence of mantle upwelling beneath this region, particularly within the continental sector of the CVL. © Saudi Society for Geosciences and Springer Nature Switzerland AG 2024. Springer Nature or its licensor (e.g. a society or other partner) holds exclusive rights to this article under a publishing agreement with the author(s) or other rightsholder(s); author self-archiving of the accepted manuscript version of this article is solely governed by the terms of such publishing agreement and applicable law. |
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Depth of the lithospheric mantle discontinuities beneath the northwest flank of Oku Volcanic Complex, Cameroon Volcanic Line: constraints from mantle xenolith and teleseismic data |
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Wotchoko, Pierre Bardintzeff, Jacques-Marie Njueya, Adoua Kopa Nkouathio, David Guimolaire |
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| score |
7.4000654 |