Mao et al.—New early Permian crinoid fauna 92(6):1066–1080


Table 1. Most significant previous localities, ages, and formations of Permian crinoid publications. Author(s)


Locality


Wanner, 1916; Wanner, 1924; Wanner, 1937; Webster, 2012a; Webster and Donovan, 2012


Yakovlev, 1926; Yakovlev, 1927; Yakovlev, 1930; Yakovlev and Ivanov, 1956


Moore and Plummer, 1940 Pabian and Strimple, 1974


Lane and Webster, 1966; Webster and Lane, 1967; Webster and Lane, 2007


Willink, 1978; Willink, 1979a; Willink, 1979b; Willink, 1980; Webster and Jell, 1999b


Webster and Jell, 1992; Webster, 1987 Webster, 1990; Teichert and Webster, 1993


Sieverts-Doreck, 1942


Webster and Sevastopulo, 2007; Webster et al., 2009b


Webster and Jell, 1993 Webster et al., 2009a Webster, 2012b


Branisa, 1965; Burke and Pabian, 1978; Strimple and Moore, 1971


Tien, 1926


Chen and Yao, 1993; Webster et al., 2009c Gorzelak et al., 2013


Valette, 1934; Lane, 1979


Gregorio, 1930; Ramovš and Sieverts-Doreck, 1968; Strimple and Sevastopulo, 1982


Waagen, 1887


Donovan et al., 1986 Reich, 2007


Basleo, Timor Ural Mountains, Russia


Texas, United States Nebraska, United States Nevada, United States


Eastern Australia


Western Australia Western Australia


Tasmania, Australia Northeastern Oman


Southern Thailand British Columbia


Bolivia Artinskian Artinskian


Wolfcampian Wolfcampian


Middle Wolfcampian Artinskian–Roadian


1067


Geologic age


Formation


Either the Maubisse Formation or Atahoc and Cribas Formation


Div’ya Formation


Cibolo Limestone Foraker Formation


Bird Spring Formation


Wandrawandian Siltstone; Catherine Sandstone; Berry Formation; Condamine Beds


Late Sakmarian–early Artinskian Callytharra Formation Artinskian–Tatarian


Sakmarian–Artinskian Sakmarian


Artinskian? Sakmarian?


North-central Crete, Greece Asselian–Artinskian? Sakmarian–Artinskian


Northern China


Southwestern China Spitsbergen Tunisia Sicily


Salt Range, Pakistan Northeast England


Pennsylvanian?


Sakmarian–Artinskian Late Artinskian–Roadian Wordian/Guadalupian Wordian


Wordian Guadlupian–Lopingian Eastern Thuringia, Germany Wuchiapingian


of the Cambrian; in the north of the line, the sedimentary gap lies at the top of the Ordovician. No Upper Ordovician, Silurian, Devonian, or Mississippian deposits occur. Unconformably overlying the Cambrian or Ordovician limestones is the Pennsyl- vanian Benchi Formation, which is dominated by terrestrial deposits (e.g., Hou et al., 1987; Lü and Chen, 2014). The Benchi Formation is composed dominantly of siltstone and contains abundant vascular plant fossils and bauxite. It is biostrati- graphically dated by the conodont Idiognathodus delicates–I. podolskensis Assemblage Zone as the middle to upper Moscov- ian, Pennsylvanian. Strata above the Pennsylvanian Benchi For- mation are the Permian Taiyuan, Shanxi, Shihezi, and Shiqianfeng formations in ascending order (Hou et al., 1987; Wu et al., 1987). The base of the Taiyuan Formation is currently defined by the first occurrence of the limestones sharply differing from the Benchi Formation below. The Taiyuan Formation is composed of tens to hundreds of meters of strata and is characterized by limestones interbedded with siltstones and mudstones with rare coal beds indicating alternating of marine and terrestrial facies (Bureau of Geology and Mineral Resources of Henan Province, 1990).


Darlington Limestone Al Jil Formation; Saiwan Formation


Phuket Group and Rat Buri Limestone Mount Mark Formation The point of rocks Copacabana Group


Taiyuan Series


Dingjiazhai Formation Kapp Starostin Formation Djebel Tebaga Sosio Formation


Wargal Formation Ford Formation


Werra-Karbonat Formation


Conodont dating suggests that it is earliest Permian, Asselian, in age (Wang et al., 1987; Lang andWang, 2007). Anyang is located in the central part of the North China


Block. Coal, iron, limestone, and bauxite of Pennsylvanian and Permian age are important economic resources of this region. Upper Paleozoic outcrops along the Tianxi section are dis- continuous. The lower part of the Taiyuan Formation is covered by roads and houses and partly measured as 15m in thickness (Fig. 2). Brown siltstones yielding fossils of vascular plants, especially ferns, and insect fossils are indicators of a nonmarine environment. The marine fossil-bearing unit consists of thin- bedded calcareous siltstones and thick-bedded bioclastic lime- stones and is the Dajian Member, middle part of the Taiyuan Formation. Above the Dajian Member are sandstones of the Mojie Member (Wang et al., 1987). Thus, the Dajian Member biologically and lithologically indicates a dramatic transgres- sional interval yielding a shallow marine fauna. Well-preserved crinoid fossils are concentrated within the


calcareous siltstones in an interval approximately 1.5m thick. Co-occurring macrofossils are the trilobite Ditomopyge sp.;


Wandagee Formation; Cundlego Formation; Quinnanie Shale:Billidee Formation


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