The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal
Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e.,...
Ausführliche Beschreibung
Gespeichert in:
| Autor*in: |
Yanchilina, A.G. [verfasserIn] |
|---|
| Format: |
E-Artikel |
|---|---|
| Sprache: |
Englisch |
| Erschienen: |
2021transfer abstract |
|---|
| Übergeordnetes Werk: |
Enthalten in: An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan - Miyata, Hugo Hissashi ELSEVIER, 2022, (including Isotope geoscience) : official journal of the European Association for Geochemistry, New York, NY [u.a.] |
|---|---|
| Übergeordnetes Werk: |
volume:570 ; year:2021 ; day:5 ; month:06 ; pages:0 |
| Links: |
|---|
| DOI / URN: |
10.1016/j.chemgeo.2021.120175 |
|---|
| Katalog-ID: |
ELV053658892 |
|---|
| LEADER | 01000caa a22002652 4500 | ||
|---|---|---|---|
| 001 | ELV053658892 | ||
| 003 | DE-627 | ||
| 005 | 20230626035151.0 | ||
| 007 | cr uuu---uuuuu | ||
| 008 | 210910s2021 xx |||||o 00| ||eng c | ||
| 024 | 7 | |a 10.1016/j.chemgeo.2021.120175 |2 doi | |
| 028 | 5 | 2 | |a /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica |
| 035 | |a (DE-627)ELV053658892 | ||
| 035 | |a (ELSEVIER)S0009-2541(21)00119-4 | ||
| 040 | |a DE-627 |b ger |c DE-627 |e rakwb | ||
| 041 | |a eng | ||
| 082 | 0 | 4 | |a 004 |q VZ |
| 084 | |a 85.35 |2 bkl | ||
| 084 | |a 54.80 |2 bkl | ||
| 100 | 1 | |a Yanchilina, A.G. |e verfasserin |4 aut | |
| 245 | 1 | 4 | |a The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| 264 | 1 | |c 2021transfer abstract | |
| 336 | |a nicht spezifiziert |b zzz |2 rdacontent | ||
| 337 | |a nicht spezifiziert |b z |2 rdamedia | ||
| 338 | |a nicht spezifiziert |b zu |2 rdacarrier | ||
| 520 | |a Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. | ||
| 520 | |a Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. | ||
| 700 | 1 | |a Yam, R. |4 oth | |
| 700 | 1 | |a Shemesh, A. |4 oth | |
| 773 | 0 | 8 | |i Enthalten in |n Elsevier |a Miyata, Hugo Hissashi ELSEVIER |t An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |d 2022 |d (including Isotope geoscience) : official journal of the European Association for Geochemistry |g New York, NY [u.a.] |w (DE-627)ELV008354693 |
| 773 | 1 | 8 | |g volume:570 |g year:2021 |g day:5 |g month:06 |g pages:0 |
| 856 | 4 | 0 | |u https://doi.org/10.1016/j.chemgeo.2021.120175 |3 Volltext |
| 912 | |a GBV_USEFLAG_U | ||
| 912 | |a GBV_ELV | ||
| 912 | |a SYSFLAG_U | ||
| 936 | b | k | |a 85.35 |j Fertigung |q VZ |
| 936 | b | k | |a 54.80 |j Angewandte Informatik |q VZ |
| 951 | |a AR | ||
| 952 | |d 570 |j 2021 |b 5 |c 0605 |h 0 | ||
| author_variant |
a y ay |
|---|---|
| matchkey_str |
yanchilinaagyamrshemesha:2021----:hefcosdmnltooynxgnstpcmoiinnpaernfra |
| hierarchy_sort_str |
2021transfer abstract |
| bklnumber |
85.35 54.80 |
| publishDate |
2021 |
| allfields |
10.1016/j.chemgeo.2021.120175 doi /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica (DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 DE-627 ger DE-627 rakwb eng 004 VZ 85.35 bkl 54.80 bkl Yanchilina, A.G. verfasserin aut The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal 2021transfer abstract nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Yam, R. oth Shemesh, A. oth Enthalten in Elsevier Miyata, Hugo Hissashi ELSEVIER An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan 2022 (including Isotope geoscience) : official journal of the European Association for Geochemistry New York, NY [u.a.] (DE-627)ELV008354693 volume:570 year:2021 day:5 month:06 pages:0 https://doi.org/10.1016/j.chemgeo.2021.120175 Volltext GBV_USEFLAG_U GBV_ELV SYSFLAG_U 85.35 Fertigung VZ 54.80 Angewandte Informatik VZ AR 570 2021 5 0605 0 |
| spelling |
10.1016/j.chemgeo.2021.120175 doi /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica (DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 DE-627 ger DE-627 rakwb eng 004 VZ 85.35 bkl 54.80 bkl Yanchilina, A.G. verfasserin aut The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal 2021transfer abstract nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Yam, R. oth Shemesh, A. oth Enthalten in Elsevier Miyata, Hugo Hissashi ELSEVIER An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan 2022 (including Isotope geoscience) : official journal of the European Association for Geochemistry New York, NY [u.a.] (DE-627)ELV008354693 volume:570 year:2021 day:5 month:06 pages:0 https://doi.org/10.1016/j.chemgeo.2021.120175 Volltext GBV_USEFLAG_U GBV_ELV SYSFLAG_U 85.35 Fertigung VZ 54.80 Angewandte Informatik VZ AR 570 2021 5 0605 0 |
| allfields_unstemmed |
10.1016/j.chemgeo.2021.120175 doi /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica (DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 DE-627 ger DE-627 rakwb eng 004 VZ 85.35 bkl 54.80 bkl Yanchilina, A.G. verfasserin aut The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal 2021transfer abstract nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Yam, R. oth Shemesh, A. oth Enthalten in Elsevier Miyata, Hugo Hissashi ELSEVIER An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan 2022 (including Isotope geoscience) : official journal of the European Association for Geochemistry New York, NY [u.a.] (DE-627)ELV008354693 volume:570 year:2021 day:5 month:06 pages:0 https://doi.org/10.1016/j.chemgeo.2021.120175 Volltext GBV_USEFLAG_U GBV_ELV SYSFLAG_U 85.35 Fertigung VZ 54.80 Angewandte Informatik VZ AR 570 2021 5 0605 0 |
| allfieldsGer |
10.1016/j.chemgeo.2021.120175 doi /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica (DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 DE-627 ger DE-627 rakwb eng 004 VZ 85.35 bkl 54.80 bkl Yanchilina, A.G. verfasserin aut The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal 2021transfer abstract nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Yam, R. oth Shemesh, A. oth Enthalten in Elsevier Miyata, Hugo Hissashi ELSEVIER An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan 2022 (including Isotope geoscience) : official journal of the European Association for Geochemistry New York, NY [u.a.] (DE-627)ELV008354693 volume:570 year:2021 day:5 month:06 pages:0 https://doi.org/10.1016/j.chemgeo.2021.120175 Volltext GBV_USEFLAG_U GBV_ELV SYSFLAG_U 85.35 Fertigung VZ 54.80 Angewandte Informatik VZ AR 570 2021 5 0605 0 |
| allfieldsSound |
10.1016/j.chemgeo.2021.120175 doi /cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica (DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 DE-627 ger DE-627 rakwb eng 004 VZ 85.35 bkl 54.80 bkl Yanchilina, A.G. verfasserin aut The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal 2021transfer abstract nicht spezifiziert zzz rdacontent nicht spezifiziert z rdamedia nicht spezifiziert zu rdacarrier Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. Yam, R. oth Shemesh, A. oth Enthalten in Elsevier Miyata, Hugo Hissashi ELSEVIER An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan 2022 (including Isotope geoscience) : official journal of the European Association for Geochemistry New York, NY [u.a.] (DE-627)ELV008354693 volume:570 year:2021 day:5 month:06 pages:0 https://doi.org/10.1016/j.chemgeo.2021.120175 Volltext GBV_USEFLAG_U GBV_ELV SYSFLAG_U 85.35 Fertigung VZ 54.80 Angewandte Informatik VZ AR 570 2021 5 0605 0 |
| language |
English |
| source |
Enthalten in An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan New York, NY [u.a.] volume:570 year:2021 day:5 month:06 pages:0 |
| sourceStr |
Enthalten in An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan New York, NY [u.a.] volume:570 year:2021 day:5 month:06 pages:0 |
| format_phy_str_mv |
Article |
| bklname |
Fertigung Angewandte Informatik |
| institution |
findex.gbv.de |
| dewey-raw |
004 |
| isfreeaccess_bool |
false |
| container_title |
An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |
| authorswithroles_txt_mv |
Yanchilina, A.G. @@aut@@ Yam, R. @@oth@@ Shemesh, A. @@oth@@ |
| publishDateDaySort_date |
2021-01-05T00:00:00Z |
| hierarchy_top_id |
ELV008354693 |
| dewey-sort |
14 |
| id |
ELV053658892 |
| language_de |
englisch |
| fullrecord |
<?xml version="1.0" encoding="UTF-8"?><collection xmlns="http://www.loc.gov/MARC21/slim"><record><leader>01000caa a22002652 4500</leader><controlfield tag="001">ELV053658892</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20230626035151.0</controlfield><controlfield tag="007">cr uuu---uuuuu</controlfield><controlfield tag="008">210910s2021 xx |||||o 00| ||eng c</controlfield><datafield tag="024" ind1="7" ind2=" "><subfield code="a">10.1016/j.chemgeo.2021.120175</subfield><subfield code="2">doi</subfield></datafield><datafield tag="028" ind1="5" ind2="2"><subfield code="a">/cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)ELV053658892</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(ELSEVIER)S0009-2541(21)00119-4</subfield></datafield><datafield tag="040" ind1=" " ind2=" "><subfield code="a">DE-627</subfield><subfield code="b">ger</subfield><subfield code="c">DE-627</subfield><subfield code="e">rakwb</subfield></datafield><datafield tag="041" ind1=" " ind2=" "><subfield code="a">eng</subfield></datafield><datafield tag="082" ind1="0" ind2="4"><subfield code="a">004</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">85.35</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">54.80</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="100" ind1="1" ind2=" "><subfield code="a">Yanchilina, A.G.</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="245" ind1="1" ind2="4"><subfield code="a">The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">2021transfer abstract</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">Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates.</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates.</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Yam, R.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Shemesh, A.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="n">Elsevier</subfield><subfield code="a">Miyata, Hugo Hissashi ELSEVIER</subfield><subfield code="t">An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan</subfield><subfield code="d">2022</subfield><subfield code="d">(including Isotope geoscience) : official journal of the European Association for Geochemistry</subfield><subfield code="g">New York, NY [u.a.]</subfield><subfield code="w">(DE-627)ELV008354693</subfield></datafield><datafield tag="773" ind1="1" ind2="8"><subfield code="g">volume:570</subfield><subfield code="g">year:2021</subfield><subfield code="g">day:5</subfield><subfield code="g">month:06</subfield><subfield code="g">pages:0</subfield></datafield><datafield tag="856" ind1="4" ind2="0"><subfield code="u">https://doi.org/10.1016/j.chemgeo.2021.120175</subfield><subfield code="3">Volltext</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_USEFLAG_U</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ELV</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SYSFLAG_U</subfield></datafield><datafield tag="936" ind1="b" ind2="k"><subfield code="a">85.35</subfield><subfield code="j">Fertigung</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="936" ind1="b" ind2="k"><subfield code="a">54.80</subfield><subfield code="j">Angewandte Informatik</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="951" ind1=" " ind2=" "><subfield code="a">AR</subfield></datafield><datafield tag="952" ind1=" " ind2=" "><subfield code="d">570</subfield><subfield code="j">2021</subfield><subfield code="b">5</subfield><subfield code="c">0605</subfield><subfield code="h">0</subfield></datafield></record></collection>
|
| author |
Yanchilina, A.G. |
| spellingShingle |
Yanchilina, A.G. ddc 004 bkl 85.35 bkl 54.80 The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| authorStr |
Yanchilina, A.G. |
| ppnlink_with_tag_str_mv |
@@773@@(DE-627)ELV008354693 |
| format |
electronic Article |
| dewey-ones |
004 - Data processing & computer science |
| delete_txt_mv |
keep |
| author_role |
aut |
| collection |
elsevier |
| remote_str |
true |
| illustrated |
Not Illustrated |
| topic_title |
004 VZ 85.35 bkl 54.80 bkl The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| topic |
ddc 004 bkl 85.35 bkl 54.80 |
| topic_unstemmed |
ddc 004 bkl 85.35 bkl 54.80 |
| topic_browse |
ddc 004 bkl 85.35 bkl 54.80 |
| format_facet |
Elektronische Aufsätze Aufsätze Elektronische Ressource |
| format_main_str_mv |
Text Zeitschrift/Artikel |
| carriertype_str_mv |
zu |
| author2_variant |
r y ry a s as |
| hierarchy_parent_title |
An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |
| hierarchy_parent_id |
ELV008354693 |
| dewey-tens |
000 - Computer science, knowledge & systems |
| hierarchy_top_title |
An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |
| isfreeaccess_txt |
false |
| familylinks_str_mv |
(DE-627)ELV008354693 |
| title |
The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| ctrlnum |
(DE-627)ELV053658892 (ELSEVIER)S0009-2541(21)00119-4 |
| title_full |
The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| author_sort |
Yanchilina, A.G. |
| journal |
An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |
| journalStr |
An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan |
| lang_code |
eng |
| isOA_bool |
false |
| dewey-hundreds |
000 - Computer science, information & general works |
| recordtype |
marc |
| publishDateSort |
2021 |
| contenttype_str_mv |
zzz |
| container_start_page |
0 |
| author_browse |
Yanchilina, A.G. |
| container_volume |
570 |
| class |
004 VZ 85.35 bkl 54.80 bkl |
| format_se |
Elektronische Aufsätze |
| author-letter |
Yanchilina, A.G. |
| doi_str_mv |
10.1016/j.chemgeo.2021.120175 |
| dewey-full |
004 |
| title_sort |
effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| title_auth |
The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| abstract |
Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. |
| abstractGer |
Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. |
| abstract_unstemmed |
Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates. |
| collection_details |
GBV_USEFLAG_U GBV_ELV SYSFLAG_U |
| title_short |
The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal |
| url |
https://doi.org/10.1016/j.chemgeo.2021.120175 |
| remote_bool |
true |
| author2 |
Yam, R. Shemesh, A. |
| author2Str |
Yam, R. Shemesh, A. |
| ppnlink |
ELV008354693 |
| mediatype_str_mv |
z |
| isOA_txt |
false |
| hochschulschrift_bool |
false |
| author2_role |
oth oth |
| doi_str |
10.1016/j.chemgeo.2021.120175 |
| up_date |
2024-07-06T19:33:32.125Z |
| _version_ |
1803859433490481152 |
| fullrecord_marcxml |
<?xml version="1.0" encoding="UTF-8"?><collection xmlns="http://www.loc.gov/MARC21/slim"><record><leader>01000caa a22002652 4500</leader><controlfield tag="001">ELV053658892</controlfield><controlfield tag="003">DE-627</controlfield><controlfield tag="005">20230626035151.0</controlfield><controlfield tag="007">cr uuu---uuuuu</controlfield><controlfield tag="008">210910s2021 xx |||||o 00| ||eng c</controlfield><datafield tag="024" ind1="7" ind2=" "><subfield code="a">10.1016/j.chemgeo.2021.120175</subfield><subfield code="2">doi</subfield></datafield><datafield tag="028" ind1="5" ind2="2"><subfield code="a">/cbs_pica/cbs_olc/import_discovery/elsevier/einzuspielen/GBV00000000001359.pica</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(DE-627)ELV053658892</subfield></datafield><datafield tag="035" ind1=" " ind2=" "><subfield code="a">(ELSEVIER)S0009-2541(21)00119-4</subfield></datafield><datafield tag="040" ind1=" " ind2=" "><subfield code="a">DE-627</subfield><subfield code="b">ger</subfield><subfield code="c">DE-627</subfield><subfield code="e">rakwb</subfield></datafield><datafield tag="041" ind1=" " ind2=" "><subfield code="a">eng</subfield></datafield><datafield tag="082" ind1="0" ind2="4"><subfield code="a">004</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">85.35</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="084" ind1=" " ind2=" "><subfield code="a">54.80</subfield><subfield code="2">bkl</subfield></datafield><datafield tag="100" ind1="1" ind2=" "><subfield code="a">Yanchilina, A.G.</subfield><subfield code="e">verfasserin</subfield><subfield code="4">aut</subfield></datafield><datafield tag="245" ind1="1" ind2="4"><subfield code="a">The effect of sediment lithology on oxygen isotope composition and phase transformation of marine biogenic opal</subfield></datafield><datafield tag="264" ind1=" " ind2="1"><subfield code="c">2021transfer abstract</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">Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates.</subfield></datafield><datafield tag="520" ind1=" " ind2=" "><subfield code="a">Biogenic amorphous opal (biogenic opal-A; SiO2·nH2O) in the form of diatoms, radiolaria, and sponge spicules, matures to more stable thermodynamic silica phases of opal-CT and microquartz chert upon accumulation and burial in deep sea sediments. Both temperature and lithology of the sediments (i.e., amounts of clay relative to calcium carbonate) influence the time and depth of maturation. Given that δ18O of silica reflects the δ18O of the water and temperature in which silica forms, it is possible to trace pathways of maturation by measuring δ18O of the different silica phases. We measured δ18O of biogenic opal-A, opal-CT, and microquartz chert from carbonate rich sediments to characterize the effects of lithology on the silica maturation. We have identified a set of cores with calcium carbonate rich and clay poor lithologies from ODP sites 1049–1053 in which these phases and phase transformations occur. The mineralogical phases are characterized by X-ray diffraction (XRD) and the purity of the samples with Scanning Electron Microscope/Energy Dispersive X-ray spectroscopy (SEM/EDS). The δ18O of biogenic opal-A is ~41 to 45‰, the δ18O of opal-A' (a transition silica phase from opal-A to opal-CT) is ~38 to 43‰, the δ18O of opal-CT is ~37 to 45‰, and δ18O of two microquartz cherts is ~38‰. δ18O of opal-A' and opal-CT indicate maturation at low temperature and with shallow depths in the sediments out of silica equilibrium with local porewater δ18O and temperature. In contrast, δ18O of two microquartz cherts reflect formation in isotope equilibrium with local porewater δ18O and temperature. Such scenarios of silica phase transformations appear to be unique to geographical locations with a low geothermal gradient and where sediments are composed of high calcium carbonate to clay ratio, either leading to a shallow and young maturation of biogenic opal-A or a delay by as much as several hundreds of meters and tens of millions of years. Heavy δ18O of porcellanites (siliceous sedimentary rocks with opal-CT mineralogy) and potentially also cherts through geologic time must reflect formation at shallow depths within the sediments, a maturation scenario influenced by simultaneous depositions of marine calcium carbonates.</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Yam, R.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="700" ind1="1" ind2=" "><subfield code="a">Shemesh, A.</subfield><subfield code="4">oth</subfield></datafield><datafield tag="773" ind1="0" ind2="8"><subfield code="i">Enthalten in</subfield><subfield code="n">Elsevier</subfield><subfield code="a">Miyata, Hugo Hissashi ELSEVIER</subfield><subfield code="t">An iterated greedy algorithm for distributed blocking flow shop with setup times and maintenance operations to minimize makespan</subfield><subfield code="d">2022</subfield><subfield code="d">(including Isotope geoscience) : official journal of the European Association for Geochemistry</subfield><subfield code="g">New York, NY [u.a.]</subfield><subfield code="w">(DE-627)ELV008354693</subfield></datafield><datafield tag="773" ind1="1" ind2="8"><subfield code="g">volume:570</subfield><subfield code="g">year:2021</subfield><subfield code="g">day:5</subfield><subfield code="g">month:06</subfield><subfield code="g">pages:0</subfield></datafield><datafield tag="856" ind1="4" ind2="0"><subfield code="u">https://doi.org/10.1016/j.chemgeo.2021.120175</subfield><subfield code="3">Volltext</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_USEFLAG_U</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">GBV_ELV</subfield></datafield><datafield tag="912" ind1=" " ind2=" "><subfield code="a">SYSFLAG_U</subfield></datafield><datafield tag="936" ind1="b" ind2="k"><subfield code="a">85.35</subfield><subfield code="j">Fertigung</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="936" ind1="b" ind2="k"><subfield code="a">54.80</subfield><subfield code="j">Angewandte Informatik</subfield><subfield code="q">VZ</subfield></datafield><datafield tag="951" ind1=" " ind2=" "><subfield code="a">AR</subfield></datafield><datafield tag="952" ind1=" " ind2=" "><subfield code="d">570</subfield><subfield code="j">2021</subfield><subfield code="b">5</subfield><subfield code="c">0605</subfield><subfield code="h">0</subfield></datafield></record></collection>
|
| score |
7.400522 |