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The recommended Cambrian–Ordovician global Boundary stratotype of the Xiaoyangqiao section (Dayangcha, Jilin Province), China

Published online by Cambridge University Press:  01 May 2009

Chen Jun-Yuan ,
Qian Yi-Yuan ,
Zhang Jun-Ming ,
Lin Yao-Kun ,
Yin Lei-Ming ,
Wang Zhi-Hao ,
Wang Zong-Zhe ,
Yang Jie-Dong  and
Wang Ying-Xi
Chen Jun-Yuan
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Qian Yi-Yuan
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Zhang Jun-Ming
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Lin Yao-Kun
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Yin Lei-Ming
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Wang Zhi-Hao
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Wang Zong-Zhe
Affiliation:
Nanjing Institute of Geology and Palaeontology, Academia Sinica, Nanjing, People's Republic of China.
Yang Jie-Dong
Affiliation:
University of Nanjing, Nanjing, People's Republic of China.
Wang Ying-Xi
Affiliation:
University of Nanjing, Nanjing, People's Republic of China.
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Abstract

This paper provides a brief outline of the current, detailed inter-disciplinary work on the Xiaoyangquiao section, trying to expose all the aspects for reference tied to the Global Single Stratigraphic Point (GSSP) Concept for defining the Cambrian–Ordovician Boundary. The 45 m critical interval of this section outcrops very well along the steep bank of a stream and is free from folding, faulting, intrusions, and has not been affected by weathering. Colour alternation of conodonts and acritarchs, and crystallinity indices of illite all indicate a maximum thermal grade of 100 °C. The lithofacies, being of great lateral persistence for a hundred kilometres, consists mainly of a rhythmical sequence of lime mudstone and shales deposited in a moderately deep outer shelf environment of quiet water, well below the normal storm wave base. Chemical investigation of the rocks demonstrates strong positive correlation between A12O3 content and those of K2O, MgO, Fe2O3, TiO2, Be, Cr, Co, Ni, Zn and Ba, indicating these components are tied to the clay fractions. A stable depositional environment is demonstrated by the uniform chemistries through the boundary interval. Close to the boundary itself P2O5 contents are low, indicating continuous sedimentation at fairly substantial rates.

The major biological events, the biostratigraphic framework, and the stratigraphic range of conodont, graptolite, trilobite, and acritarch taxa are illustrated briefly with diagrams. Following the majority views of the Calgary Plenary Session, the boundary level is to be chosen at a point marked by the First Appearance Datum (FAD) of the selected conodont taxon or taxa in the vicinity of the level close to, but below, the first influx of nematophorous graptolites. The following four points marked by the incoming of conodont taxon or taxa are recommended for consideration of the ‘Golden Spike'‘: (1) FAD of Cordylodus intermedius at 5.28 m below the first influx of nematophorous graptolites; (2) FAD of Hirsutodontus simpler–Cordylodus drucei–Albiconus postcostatus at 5.23 m; (3) FAD of Semiacontiodus lavadamensis–Utahconus utahensis–Monocostodus sevierensis at 3.85 m; (4) FAD of Cordylodus lindstromi at 2.23 m. For the following reasons the FAD of H. simplex–C. drucei–A. postcostatus is favoured: (1) the taxa are all distinct and widely dispersed; (2) intensive evolutionary change took place in conodonts, graptolites, trilobites and acritarchs prior to or after this point; all the fossil groups occur together, providing correlation with many regions throughout the world; (3) the point is in a position between the previously widely accepted boundary levels based on graptolites and trilobites; (4) the proposed point lies within a thin, laterally persistent, rhythmical sequence. The FAD of Cordylodus lindstromi is also a favourable point, sharing many advantages mentioned above. But this point is less satisfactory in being defined by the FAD of a single taxon C. lindstromi which also has an extremely small population size.

An isochron age of 500.7 ± 7.4 Ma is determined from clay fractions of mudstones 8.5 m below the proposed point by means of the Rubidium–Strontium method.

The ɛND signature determined from conodonts, trilobites hyolithids and acrotretid brachiopods has a mean value of −6.7, comparable with that of the coeval oceanic water mass occupying southeastern North America and Europe, and indicating that northeastern China bordered the same ocean. The mean Tdm model age determined was 1.26 Ga at the time of sedimentation, compatible with the mean Tdm model age of approximately 1.1 Ga for the Pacific Ocean today. The relatively low value of the Tdm model age indicates a substantial input from young orogenic volcanic island arcs and terranes.

Type
Articles
Information
Geological Magazine , Volume 125 , Issue 4 , July 1988 , pp. 415 - 444
Copyright
Copyright © Cambridge University Press 1988

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References

Aigner, T. 1979 Schill–tempestite im oberen Muschelkak (Trias, SW-Deutschland). Neues Jahrbuch für Geologie and Paläontologie, Abh. 157, 326–43.Google Scholar
Aigner, T. & Futterer, E. 1978. Kolk-Topfe und -Rinnen (pot and gutter casts) im Muschelkalk-Anzeiger für Wattenmeer. Neues Jahrbuch für Geologie und Paläontologie, Abh. 156, 285–304.Google Scholar
Allegre, C. J. & Dominique, R. 1984. The growth of the continent through geological time studied by Nd isotopic analysis of shale. Earth and Planetary Science Letters 67, 19–34.CrossRefGoogle Scholar
Berg, R. T. & Ross, R. J. Jr 1959. Trilobite from the Peerless and Manitou Formation, Colorado. Journal of Paleontology 33, 106–119.Google Scholar
Bulman, O. M. B. 1954. The graptolite fauna of the Dictyonema Shales of the Oslo region. Norsk Geologisk Tidsskrift 33, 1–40, pls. 1–8.Google Scholar
Burley, S. D. 1984. Patterns of diagenesis in the Sherwood sandstone group (Triassic), United Kigdom. Clay Minerals 19, 403–40.Google Scholar
Chen, Juan-Yuan, Erdtmann, B.-D., Gong, We-Li, Li, Hui-Ming, Lin, Yao-Kun, Qian, Yi-Yuan, Tao, Xian-Chong, Wang, Ying-Xi, Wang, Zong-Zhe, Yang, Jie-Dong, Yin, Lei-Ming & Zhang, Jun-Ming. 1986. Aspects of Cambrian–Ordovician Boundary in Dayangcha, China. Beijing: pp. 1–410, pls. 1–98. China Prospect Publishing House.Google Scholar
Chen, Jun-Yuan, Erdtmann, B.-D., Lin, Yao-Kun, Qian, Yi-Yuan, Wang, Zhi-Hao, Yin, Lei-Ming & Zhang, Jun-Ming. 1985. Study on Cambrian–Ordovician Boundary strata and its biota in Dayangcha, Hunjiang, Jilin, China; Beijing: pp. 1–138, pls. 1–39. China Prospect Publishing House.Google Scholar
Chen, Jun-Yuan, Teichert, C., Zhou, Zhi-yi, Lin, Yao-kun, Wang, Zhi-hao & Xu, Jun-tao. 1983. Faunal sequence across the Cambrian–Ordovician boundary in northern China and its international correlation. Geologica et Palaeontologica 17, 1–15.Google Scholar
Chen, Jun-yuan, Yang, Jie-dong, Wang, Ying-xi & Wang, Zong-zhe (in prep.). A clue to lost ocean: Nd isotopic composition and Sm/Nd rations of biogenic apatites.Google Scholar
Clauer, N. 1981. Rb–Sr and K–Ar dating of Precambrian clay and glauconites. Precambrian Research 15, 331–52.CrossRefGoogle Scholar
Clauer, N. & Millot, G. 1978. Genese des mineraux argileux et geochimie isotopique du strontium; ‘Livre Jubilaire Jacques Flandrin’. Documents Laboratoire de Geologie, Faculte des Sciences de Lyon N.S. 4, 129–42.Google Scholar
Correia, M. 1977. Diagenesis of sporopollenin and other comparable organic substances: application of hydrocarbon research. In Sporopollenin (eds Brooks, J. et al. ), pp. 569–620. London: Academic Press.Google Scholar
Cowie, J. W., Ziegler, W., Boucot, A. J., Bassett, M. G. & Remane, J. 1986. Guidelines and statutes of the International Commission on Stratigraphy (ICS). Courier Forschungsingsinstitut Senckenberg 83, 1–14.Google Scholar
Dean, W. T. & Martin, F. 1982. The sequence of trilobite faunas and acritarch microfloras at the Cambrian–Ordovician Boundary, Wilcox Press, Alberta, Canada. In The Cambrian–Ordovician Boundary: sections, fossil distributions, and correlations (ed. Bassett, M. G. Dean, W. T.), pp. 131–40. National Museum of Wales, Geological Series No. 3, Cardiff.Google Scholar
De Segonzac, Dunoyer G. 1970. The transformation of clay minerals during diagenesis and low-grade meta-morphism; a review. Sedimentology 15, 281–346.CrossRefGoogle Scholar
Epstein, A. G., Epstein, J. B. & Harris, L. D. 1977. Conodont color alteration – an index to organic meta-morphism; U.S. Geological Survey Professional Paper 995, 1–27.Google Scholar
Erdtmann, B.-D. 1982. A reorganization and proposed phylogenetic classification of planktic Tremadoc (Early Ordovician) dendroid graptolites. Norsk Geologisk Tidsskrift 61, 121–44.Google Scholar
Huang, He-ling, Qin, Xiang-jun, Yang, Wei & Liu, Ning. 1984. Magnetic Polarity Stratigraphy of the Cambrian and Ordovician in Western Zhejiang and Eastern Hebei, China. In Stratigraphy and Palaeontology of Systemic Boundaries in China, Cambrian–Ordovician Boundaries (1), pp. 331–38. Hefei: Anhui Science and Technology Publishing House.Google Scholar
Jin, Yu-qin & Wang, Xiao-feng. 1977. Discovery of the graptolite fauna of Baishuqi Formation, Early Ordovician, and multiramuous graptolite fauna from central Hunan. Proceedings of Stratigraphy and Palaeontology 3, 74–107 [in Chinese.]Google Scholar
Keto, L. S. & Jacobsen, S. B. 1987. Nd and Sr isotopic variations of Lower Paleozoic oceans. Earth and Planetary Science Letters 84, 27–41.Google Scholar
Kubler, B. 1968. Evaluation quantitative du métamorphisme par la cristallinite de l'illite – Etat des progrés réalisés ces dernieres années. Bulletin du Centre de Recherches de PAU–S.N.P.A. 2, 385–97.Google Scholar
Kuo, Hung-chun, Duan, Ji-ye & An, Su-lan. 1982. Cambrian–Ordovician boundary in the North China platform with description of trilobites. Paper for the Fourth International Symposium on the Ordovician System; Department of Geology, Changchun College of Geology, pp. 1–3.Google Scholar
Lindström, M. & Chen, Jun-yuan, 1987. Chemical sedimentology of the Cambrian–Ordovician Boundary Section at Dayangcha, NE China. Geologiska Föreningesis i Stockholm Förhandlingar 109, 4.Google Scholar
Martin, F. & Yin, Lei-ming (in prep.). Selected Early Ordovician acritarchs from Southern Jilin Province. Northeastern China.Google Scholar
Miller, J. F. 1980. Taxonomic revisions of some Upper Cambrian–Lower Ordovician conodonts with comments on their evolution. University of Kansas, Palaeontology Contribution 99, 1–39, pls. 1–2.Google Scholar
Miller, J. F. 1984. Cambrian and Earliest Ordovician conodont evolution, biofacies, and provincialism. Geological Society of America, Special Paper 196, 43–68.Google Scholar
En-zhi, Mu & Yao-kun., Lin 1984. The Xinchangian graptolites from western Zhejiang. In Stratigraphy and Palaeontology of Systemic Boundaries in China, Cambrian–Ordovician Boundary (1), pp. 165–82, Hefei: Anhui Science and Technology Publishing House.Google Scholar
En-zhi, Mu, Da-quan, Yang Yu-nan, Ni Ji-jin, Li, Xu, Chen Yao-kun, Lin Jian-hua, Yu Shi-ding, Jiao, Yi-Ting, Fang&Mei-Yu, Ge 1983. Graptolites. In Palaeontological Atlas of East China (1), volume of Early Paleozoic, pp. 353–496. Nanjing Institute of Geology and Mineral Resources (ed.), Beijing: Geological Publishing House.Google Scholar
Müller, K. J. 1959. Kambriske Conodonten. Zeitschrift der Deutschen geologischen Gesellschaft 111, 434–85, pls. 11–15.CrossRefGoogle Scholar
Odin, G. S. & Letolle, R. 1980. Glauconitization and phosphatization environment: a tentative comparison. Society of Economic Paleontologists and Mineralogists, Special Publication 29, 227–37.Google Scholar
Odin, G. S. & Matter, A. 1981. De glauconiarum origine. Sedimentology 28, 611–41.Google Scholar
Shan-chi., Peng 1984. Cambrian–Ordovician boundary in the Cili-Taoyuan border area, northwestern Hunan with descriptions of relative trilobites. In Stratigraphy and Palaeontology of Systemic Boundaries in China, Cambrian–Ordovician Boundary (1), pp. 286–405, 17 pls. Hefei: Anhui Science and Technology Publishing House.Google Scholar
Powell, T. G., Foscolos, A. E., Gunther, P. R. & Snowdon, L. R. 1978. Diagenesis of organic matter and fine clay minerals: a comparative study. Geochemica et Cosmochemica Acta 42, 1181–97.Google Scholar
Sengupta, S. 1975. Experimental alterations of the spores of Lycopodium clavatum as related to diagenesis. Review of Palaeobotany and Palynology 19, 173–92.CrossRefGoogle Scholar
Shaw, H. F. & Wassenburg, G. J. 1985. Sm/Nd in marine Carbonates and phosphates: implications for Nd isotopes in seawater and crustal ages. Geochimica et Cosmochimia Acta 49, 503–18.Google Scholar
Shergold, J. H. 1975. Late Cambrian and Early Ordovician trilobites from the Burke River Structural Belt, western Queensland, Australia. Bureau of Mineral Resources Australia, Geology and Geophysics, Bulletin 153, 1–252, 58 pls.Google Scholar
Shergold, J. H. 1980. Late Cambrian trilobites from the Chatsworth Limestone; Western Queensland. Bureau of Mineral Resources Australia, Geology and Geophysics, Bulletin 186, 1–108, 35 pls.Google Scholar
Sudo, T., Shimoda, S., Yotsumoto, H. & Aita, S. 1981. Electron Micrographs of Clay Minerals. Developments in Sedimentology, vol. 31, pp. 1–203, Kodansha. Elsevier.Google Scholar
Veizer, J. & Compston, W. 1974. Sr87/Sr86 composition of seawater during the Phanerozoic. Geochemica et Cosmochemica Acta 38, 1461–84.CrossRefGoogle Scholar
Weaver, C. E. 1960. Possible uses of clay minerals in search for oil. Bulletin of the American Association of Petroleum Geologists 44, 9, 1505–18.Google Scholar
Whitaker, J. H. Mc. 1973. Gutter casts, a new name for scour-and-fill structures: with examples from the Llandoverian of Ringerike and Malmoya, southern Norway. Norsk Geologisk Tidsskrift 53, 403–17.Google Scholar
Wright, J., Miller, J. F. & Holser, W. T. 1986. Conodont chemostratigraphy across the Cambrian–Ordovician boundary; western Utah and southeast China; In, Conodonts: Investigative Techniques and Applications (ed. Austin, R. L.), pp. 256–83. Chichester: Ellis Horwood.Google Scholar
Wright, J., Schrader, H. & Holser, W. T. 1987. Paleoredox variations in ancient oceans recorded by rare earth elements in fossil apatite. Geochimica et Cosmochimica Acta 51, pp. 631–44.CrossRefGoogle Scholar
Wright, J., Seymour, R. S. & Shaw, H. F. 1984. REE and Nd isotopes in conodont apatite: variations with geological age and depositional environment; In Conodont Biofacies and Provincialism (ed. Clark, D. L.), Geological Society of America, Special Paper 196, pp. 325–40.Google Scholar
Zhi-yi, Zhou & Jin-lin., Zhang 1978. Cambrian–Ordovician boundary of the Tangshan area with descriptions of the related trilobite fauna. Acta Palaeontologica Sinica 17, 1, 1–23, 4 pls. [In Chinese with English summary.]Google Scholar
Zhi-ye, Zhou & Jin-lin., Zhang 1984. Uppermost Cambrian and Lowest Ordovician trilobites of North and Northeast China; In Stratigraphy and Palaeontology of Systemic Boundaries in China, Cambrian–Ordovician Boundary (2), pp. 63–163, 29 pls. Hefei: Anhui Science and Technology Publishing House.Google Scholar