Permo-Triassic boundary superanoxia and stratified superocean: Records from lost deep sea

Science

Volumn 276, Issue 5310, 1997, Pages 235-238

  Isozaki, Yukio ^a  

^a TOKYO INSTITUTE OF TECHNOLOGY   (Japan)

Author keywords

[No Author keywords available]

Indexed keywords

ARTICLE; GEOGRAPHY; NONHUMAN; OXIDATION REDUCTION STATE; PRIORITY JOURNAL; SEA;

ANOXIA; MASS EXTINCTION; PANTHALASSA; PERMIAN/TRIASSIC BOUNDARY; STRATIFICATION;

CANADA, BRITISH COLUMBIA; JAPAN;

EID: 0030620777     PISSN: 00368075     EISSN: None     Source Type: Journal    
DOI: 10.1126/science.276.5310.235     Document Type: Article

References (45)

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8. Absence of carbonate and coarse-grained terrigenous grains indicates that the primary depositional site was deeper than the carbonate compensation depth (CCD) of ∼4000 m and was remote from land areas. [T. Matsuda and Y. Isozaki, Tectonics 10, 475 (1991); Y. Isozaki, Island Arc 5, 289 (1996); ibid. 6, 28 (1997)].
9. Absence of carbonate and coarse-grained terrigenous grains indicates that the primary depositional site was deeper than the carbonate compensation depth (CCD) of ∼4000 m and was remote from land areas. [T. Matsuda and Y. Isozaki, Tectonics 10, 475 (1991); Y. Isozaki, Island Arc 5, 289 (1996); ibid. 6, 28 (1997)].
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11. C. Scotese and R. P. Langford, in Paleogeography, Paleoclimates, Stratigraphy, vol. 1 of The Permian of Northern Pangea, P. A. Scholle, T. M. Peryt, D. S. Ulmer-Scholle, Eds. (Springer-Verlag, Berlin, 1995), pp. 3-19.
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17. Age assignment of the PTBU is based on conodont biostratigraphy. The youngest Permian conodonts occur from the lower siliceous claystone. They are poorly preserved but morphologically resemble Gondolella changxingensis (Wang), an index species for the Changxingian stage, latest Permian. The oldest Triassic conodonts are from the upper siliceous claystone and include Neospathodus dieneri (Sweet), N. waageni (Sweet), and N. conservativus (Müller) that indicate the Dienerian to Spathian, Early Triassic. Although no index fossil indicating the Changxingian or Griesbachian stage has been obtained, the boundary is assigned in the carbonaceous claystone. Late Permian and Early Triassic radiolarian faunas from adjacent cherts are consistent with this age assignment. See S. Yamakita, 1993 Annual Meeting of the Geological Society of Japan, Abstracts with Program, p. 65; K. Sugiyama, Trans. Proc. Paleont. Soc. Jpn. 167, 1180 (1992); K. Kuwahara, S. Nakae, A. Yao, J. Geol. Soc. Jpn. 97, 1005 (1993); (3, 4). The time-scale used here is after C. Ross, A. Baud, and M. Menning [Can. Soc. Petrol. Geol. Mem. 17, 81 (1994)]. Concerning the relevant Permo-Triassic interval, chronology of stage boundaries is not well constrained except for two tie-points, that is, 251 million years ago at the P-T boundary and 234 million years ago at the Anisian-Ladinian boundary.
18. Age assignment of the PTBU is based on conodont biostratigraphy. The youngest Permian conodonts occur from the lower siliceous claystone. They are poorly preserved but morphologically resemble Gondolella changxingensis (Wang), an index species for the Changxingian stage, latest Permian. The oldest Triassic conodonts are from the upper siliceous claystone and include Neospathodus dieneri (Sweet), N. waageni (Sweet), and N. conservativus (Müller) that indicate the Dienerian to Spathian, Early Triassic. Although no index fossil indicating the Changxingian or Griesbachian stage has been obtained, the boundary is assigned in the carbonaceous claystone. Late Permian and Early Triassic radiolarian faunas from adjacent cherts are consistent with this age assignment. See S. Yamakita, 1993 Annual Meeting of the Geological Society of Japan, Abstracts with Program, p. 65; K. Sugiyama, Trans. Proc. Paleont. Soc. Jpn. 167, 1180 (1992); K. Kuwahara, S. Nakae, A. Yao, J. Geol. Soc. Jpn. 97, 1005 (1993); (3, 4). The time-scale used here is after C. Ross, A. Baud, and M. Menning [Can. Soc. Petrol. Geol. Mem. 17, 81 (1994)]. Concerning the relevant Permo-Triassic interval, chronology of stage boundaries is not well constrained except for two tie-points, that is, 251 million years ago at the P-T boundary and 234 million years ago at the Anisian-Ladinian boundary.
19. Age assignment of the PTBU is based on conodont biostratigraphy. The youngest Permian conodonts occur from the lower siliceous claystone. They are poorly preserved but morphologically resemble Gondolella changxingensis (Wang), an index species for the Changxingian stage, latest Permian. The oldest Triassic conodonts are from the upper siliceous claystone and include Neospathodus dieneri (Sweet), N. waageni (Sweet), and N. conservativus (Müller) that indicate the Dienerian to Spathian, Early Triassic. Although no index fossil indicating the Changxingian or Griesbachian stage has been obtained, the boundary is assigned in the carbonaceous claystone. Late Permian and Early Triassic radiolarian faunas from adjacent cherts are consistent with this age assignment. See S. Yamakita, 1993 Annual Meeting of the Geological Society of Japan, Abstracts with Program, p. 65; K. Sugiyama, Trans. Proc. Paleont. Soc. Jpn. 167, 1180 (1992); K. Kuwahara, S. Nakae, A. Yao, J. Geol. Soc. Jpn. 97, 1005 (1993); (3, 4). The time-scale used here is after C. Ross, A. Baud, and M. Menning [Can. Soc. Petrol. Geol. Mem. 17, 81 (1994)]. Concerning the relevant Permo-Triassic interval, chronology of stage boundaries is not well constrained except for two tie-points, that is, 251 million years ago at the P-T boundary and 234 million years ago at the Anisian-Ladinian boundary.
20. Age assignment of the PTBU is based on conodont biostratigraphy. The youngest Permian conodonts occur from the lower siliceous claystone. They are poorly preserved but morphologically resemble Gondolella changxingensis (Wang), an index species for the Changxingian stage, latest Permian. The oldest Triassic conodonts are from the upper siliceous claystone and include Neospathodus dieneri (Sweet), N. waageni (Sweet), and N. conservativus (Müller) that indicate the Dienerian to Spathian, Early Triassic. Although no index fossil indicating the Changxingian or Griesbachian stage has been obtained, the boundary is assigned in the carbonaceous claystone. Late Permian and Early Triassic radiolarian faunas from adjacent cherts are consistent with this age assignment. See S. Yamakita, 1993 Annual Meeting of the Geological Society of Japan, Abstracts with Program, p. 65; K. Sugiyama, Trans. Proc. Paleont. Soc. Jpn. 167, 1180 (1992); K. Kuwahara, S. Nakae, A. Yao, J. Geol. Soc. Jpn. 97, 1005 (1993); (3, 4). The time-scale used here is after C. Ross, A. Baud, and M. Menning [Can. Soc. Petrol. Geol. Mem. 17, 81 (1994)]. Concerning the relevant Permo-Triassic interval, chronology of stage boundaries is not well constrained except for two tie-points, that is, 251 million years ago at the P-T boundary and 234 million years ago at the Anisian-Ladinian boundary.
21. Y. Isozaki et al., in Geology and Paleontology of Japan and East Asia, H. Noda and K. Sashida, Eds. (Gakujutu Tosho, Tokyo, 1996), pp. 245-251. For the Permian and Middle to Late Triassic cherts, see F. Cordey [Curr. Res. Geol. Surv. Can. 86-1A, 595 (1986)] and M. Orchard [ibid., 84-1B, 197 (1984)].
22. Y. Isozaki et al., in Geology and Paleontology of Japan and East Asia, H. Noda and K. Sashida, Eds. (Gakujutu Tosho, Tokyo, 1996), pp. 245-251. For the Permian and Middle to Late Triassic cherts, see F. Cordey [Curr. Res. Geol. Surv. Can. 86-1A, 595 (1986)] and M. Orchard [ibid., 84-1B, 197 (1984)].
23. Y. Isozaki et al., in Geology and Paleontology of Japan and East Asia, H. Noda and K. Sashida, Eds. (Gakujutu Tosho, Tokyo, 1996), pp. 245-251. For the Permian and Middle to Late Triassic cherts, see F. Cordey [Curr. Res. Geol. Surv. Can. 86-1A, 595 (1986)] and M. Orchard [ibid., 84-1B, 197 (1984)].
24. The Permo-Triassic chert sections with the PTBU occur in the Jurassic accretionary complex for nearly 1000 km along the Japanese islands from north of Tokyo to Kyushu island (3), which suggests that its primary distribution was more extensive.
25. The deep-sea anoxia started in the Follicucullus scholasticus (radiolarian) zone that indicates the latest Guadalupian to earliest Wuchapingian, and it ended in the Eptingium manfredi-group (radiolarian) zone of the mid-Anisian. According to the timescale (9), this interval is estimated to be nearly 20 My.
26. The well-known Cenomanian-Turonian (Cretaceous) anoxia is no longer than 1 to 2 My and others are much shorter [H. C. Jenkyns, J. Geol. Soc. London 137, 171 (1980); Am. J. Sci. 288, 101 (1988); W. W. Hay, Geol. Soc. Am. Bull. 100, 1934 (1988)].
27. The well-known Cenomanian-Turonian (Cretaceous) anoxia is no longer than 1 to 2 My and others are much shorter [H. C. Jenkyns, J. Geol. Soc. London 137, 171 (1980); Am. J. Sci. 288, 101 (1988); W. W. Hay, Geol. Soc. Am. Bull. 100, 1934 (1988)].
28. The well-known Cenomanian-Turonian (Cretaceous) anoxia is no longer than 1 to 2 My and others are much shorter [H. C. Jenkyns, J. Geol. Soc. London 137, 171 (1980); Am. J. Sci. 288, 101 (1988); W. W. Hay, Geol. Soc. Am. Bull. 100, 1934 (1988)].
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45. P. F. Hoffman and J. M. Edmond critically reviewed an early version of the manuscript. W. R. Danner, F. Cordey, M. Orchard, T. Koike, and H. Sano provided valuable information of the Cache Creek cherts. Supported by the Ministry of Culture and Education of Japan (Intensified Study Area Program number 259, 1995 through 1997).