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Journal of Paleontology 91(6):1199–1219
Pangea (e.g., Texas), where evaporites or terrestrial deposits occur (Jin et al., 1994; Mei and Henderson, 2001). The lowstand resulted in nearly half of the area of South China being covered by the Lungtan Formation, which represents transitional facies between terrestrial and marine (Fig. 1.2). An obvious sequence boundary, indicated by the Wangpo Shale, is present in the basal part of the Wuchiaping Formation. Only a few structural troughs (e.g., Qin-Fang region) have continuous marine deposition across the Guadalupian-Lopingian boundary (GLB) interval. According to conodont data, the uppermost Guadalupian conodont zone is Jinogondolella postserrata in some regions (e.g., Shangsi; Fig. 1.2), which implies that the end-Guadalupian regression might begin in the upper part of the J. postserrata Zone in South China. The lowest Lopingian conodont zone is Clarkina dukouensis in most regions (Fig. 1.2), which suggests that the beginning of the early Lopingian transgression occurs in the lower part of the C. dukouensis Zone in South China. Thus, one or more conodont zones of Jinogondolella altudaensis, J. shannoni, J. prexuanhanensis, J. xuanhanensis, J. granti, Clarkina postbitteri hongshuiensis,or C. postbitteri postbitteri,is not recognized around the GLB interval in most regions of South China (Fig. 1.2), and the obvious boundary between the Guadalupian and Lopingian is the same as the distinct transition from Jinogondolella to Clarkina,which may also indicate the time framework of the pre-Lopingian extinction interval (Shen and Shi, 2009). The C. postbitteri postbitteri Zone is missing in almost all regions of South China. However, Clarkina juvenile specimens also have an obvious cusp and more discrete denticles, which are similar to C. postbitteri postbitteri and are easily misidentified as C. postbitteri postbitteri.
Materials and methods
All conodont materials illustrated in this paper are from the Penglaitan, Dukou, and Nanjiang sections (Fig. 1.1). The Penglaitan Section is the GSSP for the base of theWuchiapingian Stage and is located 20 kmeast of Laibin, Guangxi Province. The Wuchiapingian Stage in this section consists of the uppermost Maokou Formation and theHeshan Formation (Shen et al., 2007). The Dukou and Nanjiang sections are located in northeastern Sichuan, and are found in Xuanhan and Nanjiang counties, respectively. The Wuchiapingian Stage of both sections consists of the Wuchiaping Formation only. The Penglaitan and Dukou sections were continuously sampled from the top of the Maokou Formation to the top of theHeshan/Wuchiaping Formation. Some SEM illustrated specimens were re-examined from samples previously collected byMei in Mei et al. (1994a, b, 1998a). P1 elements are only used to differentiate Clarkina species
in this paper, and we herein attempt to illustrate a series of growth stages for each species as completely as possible to show most characteristics of a species and their intraspecific variation. A few elements of the C. orientalis apparatus are also illustrated.
Repository and institutional abbreviation.—The new conodont material is stored in the Nanjing Institute of Geology and Palaeontology (NIGP), Chinese Academy of Sciences.
Systematic paleontology
Class Conodonta Eichenberg, 1930 Order Ozarkodinida Dzik, 1976
Family Gondolellidae Lindstroem, 1970 Genus Jinogondolella Mei and Wardlaw, 1994
Type species.—Gondolella nankingensis Ching (Jin), 1960 from the Kufeng Formation, Jiangsu Province, China.
Jinogondolella granti (Mei and Wardlaw in Mei et al., 1994b) Figure 3.1–3.18
1994b Mesogondolella granti Mei and Wardlaw in Mei et al., p. 229, pl. 1, figs. 8–12.
1998a Jinogondolella granti; Mei et al., p. 62, pl. 3, figs. 1–4, 10–14, pl. 7, figs. 8, 9, 12, 15–24.
2000 Mesogondolella altudaensis; Wang, pl. 4, figs. 2–10. 2000 Mesogondolella granti; Wang, pl. 5, figs. 1–7, 12, pl. 7, figs. 8–12.
2000 Mesogondolella prexuanhanensis;Wang, pl. 5, figs. 8, 9, pl. 7, figs. 2–5.
2000 Mesogondolella shannoni; Wang, pl. 5, figs.10, 11, 13–18.
2000 Mesogondolella laibinensis Wang, pl. 6, figs. 5–12. 2002
2006a Jinogondolella granti; Jin et al., figs. 7.11, 7.12.
Jinogondolella granti; Henderson et al., p. 731, pl. 1, figs. 12–16.
?2008 Jinogondolella granti; Zhang et al., p. 438, pl. 1, fig. 28.
?2008 Clarkina postbitteri hongshuiensis; Zhang et al., pl. 1, figs. 19–21, 23, pl. 2, fig. 1.
Holotype.—NIGP123478, from the Maokou Formation, Guangxi Province, China (Mei et al., 1994b, pl. 1, figs. 8, 9).
Original diagnosis.—A species of Mesogondolella (=Jinogondolella in this paper) characterized by a P1 element that has a bluntly rounded posterior, slender platform with nearly parallel sides in its posterior part where the platform narrows gradually to the anterior end, high and large terminal cusp, and nearly entirely fused carina in its middle part. The fused carina is nearly flat, with both posterior and anterior ends arching downward when viewed in lateral profile (Mei et al., 1994b, p. 229).
Emended diagnosis.—Aspecies of Jinogondolella characterized by a P1 element with a slender, symmetrical, arched and long platform whose lateral margins are nearly parallel in the middle portion in most individuals, and then narrowing gradually in the
Figure 3. (1–18) Jinogondolella granti (Mei and Wardlaw in Mei et al., 1994b): (1, 2) Holotype, NIGP123478, from sample LPD-117 at Penglaitan Section in Mei et al. (1994b); (3–18) from sample PLT 5b at Penglaitan Section, registration nos. NIGP166056-166063. (19–34) Clarkina postbitteri hongshuiensis Henderson, Mei, and Wardlaw, 2002: (19, 20) Holotype, NIGP134579, (21–34) Paratypes, NIGP134575–134578, 134580–134584, all from sample Bed 6i at Penglaitan Section in Henderson et al. (2002).
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