Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics
The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ...
Ausführliche Beschreibung
Gespeichert in:
| Autor*in: |
Sun, Y.D. [verfasserIn] Orchard, M.J. [verfasserIn] Kocsis, Á.T. [verfasserIn] Joachimski, M.M. [verfasserIn] |
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| Format: |
E-Artikel |
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| Sprache: |
Englisch |
| Erschienen: |
2020 |
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| Schlagwörter: |
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| Übergeordnetes Werk: |
Enthalten in: Earth and planetary science letters - Amsterdam [u.a.] : Elsevier, 1966, 534 |
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| Übergeordnetes Werk: |
volume:534 |
| DOI / URN: |
10.1016/j.epsl.2020.116082 |
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ELV003589196 |
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| 520 | |a The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. | ||
| 650 | 4 | |a Late Triassic | |
| 650 | 4 | |a palaeothemometry | |
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| 650 | 4 | |a faunal turnovers | |
| 650 | 4 | |a Wrangellia Terrane | |
| 700 | 1 | |a Orchard, M.J. |e verfasserin |4 aut | |
| 700 | 1 | |a Kocsis, Á.T. |e verfasserin |4 aut | |
| 700 | 1 | |a Joachimski, M.M. |e verfasserin |0 (orcid)0000-0001-6088-3261 |4 aut | |
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10.1016/j.epsl.2020.116082 doi (DE-627)ELV003589196 (ELSEVIER)S0012-821X(20)30025-X DE-627 ger DE-627 rda eng 550 DE-600 38.35 bkl 39.29 bkl Sun, Y.D. verfasserin (orcid)0000-0003-4032-2082 aut Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics 2020 nicht spezifiziert zzz rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane Orchard, M.J. verfasserin aut Kocsis, Á.T. verfasserin aut Joachimski, M.M. verfasserin (orcid)0000-0001-6088-3261 aut Enthalten in Earth and planetary science letters Amsterdam [u.a.] : Elsevier, 1966 534 Online-Ressource (DE-627)266015778 (DE-600)1466659-5 (DE-576)074959980 1385-013X nnns volume:534 GBV_USEFLAG_U SYSFLAG_U GBV_ELV SSG-OPC-GGO SSG-OPC-GEO SSG-OPC-AST GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 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_150 GBV_ILN_151 GBV_ILN_224 GBV_ILN_370 GBV_ILN_602 GBV_ILN_702 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2027 GBV_ILN_2034 GBV_ILN_2038 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2056 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2118 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2190 GBV_ILN_2336 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4313 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4393 38.35 Endogene Geologie: Allgemeines 39.29 Theoretische Astronomie: Sonstiges AR 534 |
| spelling |
10.1016/j.epsl.2020.116082 doi (DE-627)ELV003589196 (ELSEVIER)S0012-821X(20)30025-X DE-627 ger DE-627 rda eng 550 DE-600 38.35 bkl 39.29 bkl Sun, Y.D. verfasserin (orcid)0000-0003-4032-2082 aut Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics 2020 nicht spezifiziert zzz rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane Orchard, M.J. verfasserin aut Kocsis, Á.T. verfasserin aut Joachimski, M.M. verfasserin (orcid)0000-0001-6088-3261 aut Enthalten in Earth and planetary science letters Amsterdam [u.a.] : Elsevier, 1966 534 Online-Ressource (DE-627)266015778 (DE-600)1466659-5 (DE-576)074959980 1385-013X nnns volume:534 GBV_USEFLAG_U SYSFLAG_U GBV_ELV SSG-OPC-GGO SSG-OPC-GEO SSG-OPC-AST GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 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_150 GBV_ILN_151 GBV_ILN_224 GBV_ILN_370 GBV_ILN_602 GBV_ILN_702 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2027 GBV_ILN_2034 GBV_ILN_2038 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2056 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2118 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2190 GBV_ILN_2336 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4313 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4393 38.35 Endogene Geologie: Allgemeines 39.29 Theoretische Astronomie: Sonstiges AR 534 |
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10.1016/j.epsl.2020.116082 doi (DE-627)ELV003589196 (ELSEVIER)S0012-821X(20)30025-X DE-627 ger DE-627 rda eng 550 DE-600 38.35 bkl 39.29 bkl Sun, Y.D. verfasserin (orcid)0000-0003-4032-2082 aut Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics 2020 nicht spezifiziert zzz rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane Orchard, M.J. verfasserin aut Kocsis, Á.T. verfasserin aut Joachimski, M.M. verfasserin (orcid)0000-0001-6088-3261 aut Enthalten in Earth and planetary science letters Amsterdam [u.a.] : Elsevier, 1966 534 Online-Ressource (DE-627)266015778 (DE-600)1466659-5 (DE-576)074959980 1385-013X nnns volume:534 GBV_USEFLAG_U SYSFLAG_U GBV_ELV SSG-OPC-GGO SSG-OPC-GEO SSG-OPC-AST GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 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_150 GBV_ILN_151 GBV_ILN_224 GBV_ILN_370 GBV_ILN_602 GBV_ILN_702 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2027 GBV_ILN_2034 GBV_ILN_2038 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2056 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2118 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2190 GBV_ILN_2336 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4313 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4393 38.35 Endogene Geologie: Allgemeines 39.29 Theoretische Astronomie: Sonstiges AR 534 |
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10.1016/j.epsl.2020.116082 doi (DE-627)ELV003589196 (ELSEVIER)S0012-821X(20)30025-X DE-627 ger DE-627 rda eng 550 DE-600 38.35 bkl 39.29 bkl Sun, Y.D. verfasserin (orcid)0000-0003-4032-2082 aut Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics 2020 nicht spezifiziert zzz rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane Orchard, M.J. verfasserin aut Kocsis, Á.T. verfasserin aut Joachimski, M.M. verfasserin (orcid)0000-0001-6088-3261 aut Enthalten in Earth and planetary science letters Amsterdam [u.a.] : Elsevier, 1966 534 Online-Ressource (DE-627)266015778 (DE-600)1466659-5 (DE-576)074959980 1385-013X nnns volume:534 GBV_USEFLAG_U SYSFLAG_U GBV_ELV SSG-OPC-GGO SSG-OPC-GEO SSG-OPC-AST GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 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_150 GBV_ILN_151 GBV_ILN_224 GBV_ILN_370 GBV_ILN_602 GBV_ILN_702 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2027 GBV_ILN_2034 GBV_ILN_2038 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2056 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2118 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2190 GBV_ILN_2336 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4313 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4393 38.35 Endogene Geologie: Allgemeines 39.29 Theoretische Astronomie: Sonstiges AR 534 |
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10.1016/j.epsl.2020.116082 doi (DE-627)ELV003589196 (ELSEVIER)S0012-821X(20)30025-X DE-627 ger DE-627 rda eng 550 DE-600 38.35 bkl 39.29 bkl Sun, Y.D. verfasserin (orcid)0000-0003-4032-2082 aut Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics 2020 nicht spezifiziert zzz rdacontent Computermedien c rdamedia Online-Ressource cr rdacarrier The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane Orchard, M.J. verfasserin aut Kocsis, Á.T. verfasserin aut Joachimski, M.M. verfasserin (orcid)0000-0001-6088-3261 aut Enthalten in Earth and planetary science letters Amsterdam [u.a.] : Elsevier, 1966 534 Online-Ressource (DE-627)266015778 (DE-600)1466659-5 (DE-576)074959980 1385-013X nnns volume:534 GBV_USEFLAG_U SYSFLAG_U GBV_ELV SSG-OPC-GGO SSG-OPC-GEO SSG-OPC-AST GBV_ILN_20 GBV_ILN_22 GBV_ILN_23 GBV_ILN_24 GBV_ILN_31 GBV_ILN_32 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_150 GBV_ILN_151 GBV_ILN_224 GBV_ILN_370 GBV_ILN_602 GBV_ILN_702 GBV_ILN_2003 GBV_ILN_2004 GBV_ILN_2005 GBV_ILN_2011 GBV_ILN_2014 GBV_ILN_2015 GBV_ILN_2020 GBV_ILN_2021 GBV_ILN_2025 GBV_ILN_2027 GBV_ILN_2034 GBV_ILN_2038 GBV_ILN_2044 GBV_ILN_2048 GBV_ILN_2049 GBV_ILN_2050 GBV_ILN_2056 GBV_ILN_2059 GBV_ILN_2061 GBV_ILN_2064 GBV_ILN_2065 GBV_ILN_2068 GBV_ILN_2111 GBV_ILN_2112 GBV_ILN_2113 GBV_ILN_2118 GBV_ILN_2122 GBV_ILN_2129 GBV_ILN_2143 GBV_ILN_2147 GBV_ILN_2148 GBV_ILN_2152 GBV_ILN_2153 GBV_ILN_2190 GBV_ILN_2336 GBV_ILN_2507 GBV_ILN_2522 GBV_ILN_4035 GBV_ILN_4037 GBV_ILN_4112 GBV_ILN_4125 GBV_ILN_4126 GBV_ILN_4242 GBV_ILN_4251 GBV_ILN_4305 GBV_ILN_4313 GBV_ILN_4323 GBV_ILN_4324 GBV_ILN_4326 GBV_ILN_4333 GBV_ILN_4334 GBV_ILN_4335 GBV_ILN_4338 GBV_ILN_4393 38.35 Endogene Geologie: Allgemeines 39.29 Theoretische Astronomie: Sonstiges AR 534 |
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Sun, Y.D. |
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Sun, Y.D. ddc 550 bkl 38.35 bkl 39.29 misc Late Triassic misc palaeothemometry misc palaeoceanography misc reef development misc faunal turnovers misc Wrangellia Terrane Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics |
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550 DE-600 38.35 bkl 39.29 bkl Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics Late Triassic palaeothemometry palaeoceanography reef development faunal turnovers Wrangellia Terrane |
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Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics |
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carnian–norian (late triassic) climate change: evidence from conodont oxygen isotope thermometry with implications for reef development and wrangellian tectonics |
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Carnian–Norian (Late Triassic) climate change: Evidence from conodont oxygen isotope thermometry with implications for reef development and Wrangellian tectonics |
| abstract |
The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. |
| abstractGer |
The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. |
| abstract_unstemmed |
The Carnian–Norian (C–N) transition (Late Triassic) has long been postulated as an interval of major climatic changes, though the nature of such changes and their ecological impact remains largely unexplored. We use oxygen isotopes measured on monogeneric conodont assemblages ( δ 18 OPO4) from the Canadian Cordillera to trace seawater temperature evolution at the western margin of Pangea and in the allochthonous Wrangellia Terrane. Different conodont taxa show conspicuous offsets in δ 18 OPO4, suggesting that they had preferential habitat depths and genus-specific temperature corrections must be applied. Thus, δ 18 OPO4 from the Williston Lake sections indicates low mid-latitude sea surface temperatures (SSTs) ranging from ∼28 to 35°C, favouring a generally warm Late Triassic climate scenario. The parvus Subzone of C–N transition, which marks the peak faunal turnover, records major climatic perturbations: SSTs peaking at ∼34°C then decreasing to ∼29°C. This is followed by a quick temperature rebound and a second pulse of cooling from 33 to 27°C in the asymmetrica-Norigondolella Subzone, marking the coldest temperatures in the ∼20 Myr study interval. A secular warming trend towards the late Norian reinstated after the transient cooling in the earliest Norian, coinciding with reef expansions in the Late Triassic. The middle–late Norian (Alaunian 3–Sevatian 1) represents a hothouse climate comparable to the Paleocene–Eocene Thermal Maximum and its warmth supressed both diversity and origination rates of reef-building biota. Early Norian δ 18 OPO4 data from Frederick Island, Haida Gwaii (part of the Wrangellia Terrane) are more depleted in 18O compared to coeval samples from the Black Bear Ridge, indicating ∼3–5°C warmer temperatures than the Laurentian epicontinental sea. The temperature difference supports a more southern, probably sub-equatorial position for at least part of the Wrangellia Terrane during the earliest Norian. |
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|
| score |
7.39999 |