Trilobites of the Pseudokoldinioidia Fauna (Uppermost Cambrian) From the Taebaek Group, Taebaeksan Basin, Korea
By Lee, Seung-Bae Choi, Duck K
ABSTRACT- The Pseudokoldinioidia Fauna is a newly documented uppermost Cambrian trilobite assemblage from the Dongjeom Formation of the Taebaek Group, Taebaeksan Basin, Korea. It is characterized by low species diversity comprising six trilobite taxa: Micragnostus chiushuensis, Koldinioidia typicalis, leiostegiid genus and species indeterminate, Pseudokoldinioidia perpetis, Onychopyge borealis, and pilekiid genus and species indeterminate. Of these, special attention has been paid to Pseudokoldinioidia perpetis, which was originally assigned to Missisquoia, an index fossil for the uppermost Cambrian in Laurentia. Pseudokoldinioidia is restricted to eastern Asia, whereas Missisquoia is confined to Laurentia. The appearance of the Pseudokoldinioidia Fauna is interpreted as contemporaneous with the base of the ‘Missisquoia’ perpetis Zone of North China, which in turn is correlated with the base of the Missisquoia typicalis Subzone of Laurentia. The associated Koldinioidia and Onychopyge make it possible to compare the Pseudokoldinioidia Fauna of Korea and North China with the latest Cambrian trilobite assemblages of South China, Australia, South America, and Mexico, and also suggests an interesting biogeographic connection among these areas in the latest Cambrian.
TRILOBITES ARE among the most abundant fossil groups in Korea. They occur in the lower Paleozoic Joseon Supergroup of the Taebaeksan Basin, located in the central-eastern part of the Korean Peninsula (Fig. 1). The Joseon Supergroup ranges in age from late Early Cambrian to Middle Ordovician and is divided into five groups, based on different lithologic successions in different regions: i.e., the Taebaek, Yeongwol, Yongtan, Pyeongchang, and Mungyeong Groups (Choi, 1998; Fig. 1.2). The stratigraphy of the Taebaek and Yeongwol Groups is well established thanks to relatively abundant occurrence of trilobites, whereas the other three groups are poorly fossiliferous and hence their internal stratigraphy is less completely resolved. The Taebaek Group is exposed in the eastern half of the Taebaeksan Basin and includes, in ascending order, the Jangsan/Myeonsan, Myobong, Daegi, Sesong, Hwajeol, Dongjeom, Dumugol, Makgol, Jigunsan, and Duwibong Formations (Kobayashi, 1966; Choi and Chough, 2005). The Cambrian-Ordovician boundary has been traditionally placed at the boundary between the Hwajeol and Dongjeom Formations (Kobayashi, 1966).
Choi et al. (2004a) presented a detailed account of the lithostratigraphy of the Taebaek Group in the southeastern corner of the Taebaeksan Basin, in which three trilobite assemblages from the lower part of the Dongjeom Formation were briefly mentioned. They were designated the Mictosaukia, Missisquoia-Onychopyge, and kainellid-dominated faunas. Of particular interest is the occurrence of Missisquoia Shaw, 1951, inasmuch as the genus Missisquoia was for some time employed as an index fossil for recognizing the base of the Ordovician in North America (Winston and Nicholls, 1967; Stitt, 1971, 1977; Loch et al., 1993; Ross et al., 1997). However, the recently ratified global standard stratotype section and point (GSSP) for the Cambrian-Ordovician boundary was set at a slightly younger level at the lowest occurrence of the conodont Iapetognathus fluctivagus Nicoll et al., 1999 (Cooper et al., 2001), thereby placing the Missisquoia Zone in the uppermost Cambrian (Miller et al., 2003). Recent reevaluation of the Missisquoia-Onychopyge fauna reveals that the specimens referred to Missisquoia are morphologically distinct from the Laurentian Missisquoia, and they are reassigned herein to another missisquoiid genus, Pseudokoldinioidia Endo, 1944, which is known from Liaoning, North China. Accordingly, the Missisquoia-Onychopyge fauna is herein renamed as the Pseudokoldinioidia Fauna. Despite the generic reassignment, the appearance of the Pseudokoldinioidia Fauna appears correlative with the base of the ‘Missisquoia’ perpetis Zone of North China and the Missisquoia typicalis Subzone of the Missisquoia Zone in Laurentia. The objectives of this paper are to describe the trilobites of the Pseudokoldinioidia Fauna from the Dongjeom Formation of Korea and to discuss their stratigraphic and paleogeographic implications.
GEOLOGY AND STRATIGRAPHY
The Taebaeksan Basin occupies the central-eastern part of the Korean Peninsula (Fig. 1.1) and comprises mainly the Cambrian- Ordovician Joseon Supergroup and the Carboniferous-Permian Pyeongan Supergroup. The Joseon Supergroup rests unconformably on Precambrian granitic gneiss and metasedimentary rocks and is in turn overlain unconformably by post-Ordovician sedimentary rocks. The lower Paleozoic sedimentary rocks are shallow marine in origin and consist of limestone, sandstone, and shale. In the early Paleozoic, the Taebaeksan Basin was a shallow-marine, mixed siliciclastic- carbonate system with progressively greater depth to the west (Chough et al., 2000). This siliciclastic-carbonate system persisted throughout the Cambrian, but a high rate of carbonate accumulation in the Yeongwol area during latest Cambrian time resulted in development of a widespread carbonate platform across the Taebaeksan Basin in the Early Ordovician. Sedimentological features reveal that the carbonate platform in the Ordovician was characterized by low relief with shoals, lagoons, and tidal flats (Choi et al., 2001). Marine sedimentation ceased over the whole Taebaeksan Basin in the Late Ordovician, and most of the basin remained emergent through the mid-Paleozoic until a marine transgression in the Late Carboniferous.
The Joseon Supergroup is divided into the Taebaek, Yeongwol, Yongtan, Pyeongchang, and Mungyeong Groups (Choi, 1998). The Taebaek Group was deposited in the eastern half of the Taebaeksan Basin (Fig. 1.2) and comprises, in ascending order, the Jangsan/Myeonsan, Myobong, Daegi, Sesong, Hwajeol, Dongjeom, Dumugol, Makgol, Jigunsan, and Duwibong Formations (Kobayashi, 1966; Choi et al., 2004a). The Dongjeom Formation, from which the present material was recovered, consists largely of light- to dark-gray sandstone with scattered shale and limestone layers. In the southeastern part of the Taebaeksan Basin, the Dongjeom Formation is divided into three informal members (Fig. 2). The lower member is dominated by thickly- laminated fine-grained sandstone intercalated with thinly-laminated or normally graded fine-grained sandstone layers. The middle member is composed largely of coarse-grained massive or cross-stratified sandstone. The upper member is characterized by fine- to medium- grained sandstone intermingled with mud layers and massive sandstone with intercalation of thin carbonate facies.
FIGURE 1-Index maps. 1, Tectonic map of the Korean peninsula and surrounding area showing the location of the Taebaeksan Basin. Q-D = QinlingDabie Belt, S = Sulu Belt, N = Nangnim Massif, P = Pyeongnam Basin, I = Imjingang Belt, G = Gyeonggi Massif, O = Okcheon Belt, T = Taebaeksan Basin, Y = Yeongnam Massif; 2, Simplified geologic map showing the distribution of the lower Paleozoic Joseon Supergroup in the Taebaeksan Basin. The fossil locality of the Pseudokoldinioidia Fanua is indicated by a solid arrow near the eastern edge of the map. Modified from Choi et al. (2001).
FIGURE 2-Stratigraphic columns of the Dongjeom Formation showing lithology, sampling units, and trilobite faunas. Solid bars with unit number in the right column indicate the intervals from which trilobite specimens are collected.
The Dongjeom Formation historically had yielded very few fossils. The Pseudokainella Zone was the only biozone established on a single specimen of Pseudokainella iwayai Kobayashi, 1953 in the lower part of the formation. This occurrence was a basis for placing the Cambrian-Ordovician boundary within the Taebaek Group at the base of the Dongjeom Formation (Kobayashi, 1966). Recent detailed paleontological investigations on the Taebaek Group have refined the biostratigraphy across the Cambrian-Ordovician boundary interval (Choi et al., 2003, 2004a). These studies recognized three trilobite assemblages across the boundary between the Hwajeol and Dongjeom Formations: in ascending order, Mictosaukia, Missisquoia- Onychopyge, and kainellid-dominated faunas (Choi et al., 2004a). The latter two faunas are renamed herein as the Pseudokoldinioidia and Richardsonella faunas, respectively (Fig. 2), to accommodate recent taxonomic revisions. Although these trilobite faunas have yet to be studied in detail, they generally indicate a close affinity with Upper Cambrian faunas elsewhere. The Mictosaukia Fauna has many taxa in common with the Mictosaukia-Fatocephalus fauna of North China (Zhou and Zhang, 1985; Duan et al., 1986; Chen et al., 1988), South China (Peng, 1984), and Assemblage 1 of the Pacoota Sandstone, Australia (Shergold, 1991). The Pseudokoldinioidia Fauna is equivalent in part with the Missisquoia Zone of North China (Zhou and Zhang, 1985; Duan et al., 1986) and North America (Stitt, 1977; Ross et al., 1997). The Richardsonella Fauna is most likely contemporaneous with the Richardsonella-Platypeltoides Zone (uppermost Cambrian) of North China (Chen et al., 1988).
FOSSIL LOCALITY AND MATERIAL
All of the trilobites considered in this study were collected from the lowermost part of the Dongjeom Formation, exposed along a mountain trail in the southeastern corner of the Taebaeksan Basin (Fig. 1.2). The mountain trail, called the Seokgaejae section, exposes a nearly complete succession (ca. 1,100 m thick) of the Taebaek Group (Choi et al., 2004a). The Hwajeol and Dongjeom Formations are well exposed and yield relatively well-preserved invertebrate fossils, including trilobites, brachiopods, and echinoderms (Lee et al., 2005). The Hwajeol Formation (ca. 50 m thick) is composed largely of alternating limestone and shale, while the Dongjeom Formation (ca. 90 m thick) consists predominantly of sandstone (Fig. 2). Trilobites are relatively abundant in the transitional interval (ca. 20 m thick) across the boundary between the Hwajeol and Dongjeom Formations, which occupies the middle portion of the Seokgaejae section with geographic coordinates of 129[degrees]08’39”E and 37[degrees]04’19”N. The transitional interval shows gradual change from carbonate-dominated facies to siliciclastic-dominated facies. This interval was divided into 57 units for lithologic description and fossil collection. The units are variable in thickness, ranging from a few cm thick to ca. 50 cm thick, and are designated from bottom to top as SCO1, SCO2, SCO3, . . . . The SCO denotes the Cambrian-Ordovician boundary interval at the Seokgaejae section. Trilobites were collected from 20 units, while other units are unfossiliferous or contain brachiopods or echinoderm debris only. The Pseudokoldinioidia Fauna was recovered from two units, SCO29 and SCO30, which together span ca. 50 cm (Fig. 2) of thinly-laminated calcareous fine-grained sandstone. More than 130 trilobite specimens have been recovered as silicified sclerites from severely weathered rock samples. The collection includes cranidia, pygidia, librigenae, hypostomes, and thoracic segments. These trilobites are associated with isolated plates of rhombiferans, orthid brachiopods, and sponge spicules.
GEOLOGIC AGE AND CORRELATION
The Pseudokoldinioidia Fauna is characterized by relatively low species diversity. It includes one agnostoid and five polymerid trilobites: i.e., Micragnostus chiushuensis Kobayashi, 1931 (26.4%), Koldinioidia typicalis Kobayashi, 1931 (8.3%), leiostegiid gen. and sp. indet. (16.7%), Pseudokoldinioidia perpetis (Zhou and Zhang, 1985) (25.0%), Onychopyge borealis Zhou and Zhang, 1978 (22.2%), and pilekiid gen. and sp. indet. (1.4%).
Micragnostus chiushuensis is a long-ranging species in Upper Cambrian to Tremadocian strata. It was known largely from China, but also had been reported from Iran (Peng et al., 1999), North America (Dean, 1989; Westrop, 1995), and Argentina (Tortello et al., 1999; Tortello and Rao, 2000). The genus Koldinioidia Kobayashi, 1931 is widely distributed, having been reported from the Upper Cambrian to Tremadocian of Korea (Sohn and Choi, 2002), North China (Zhou and Zhang, 1985; Duan et al., 1986; Qian, 1986; Zhang and Jell, 1987; Zhu and Wittke, 1989), South China (Lu and Lin, 1984; Lu and Zhou, 1990; Peng, 1992), Australia (Shergold, 1975,1991), Iran (Peng et al., 1999), Kazakhstan (Ergaliev, 1983), Mexico (Robison and Pantoja- Alor, 1968), and Bolivia (Privyl and Vanek, 1980). Koldinioidia typicalis, however, is more restricted within the uppermost Cambrian (MictosaukiaFatocephalus to Richardsonella-Platypeltoides Zones) of North China (Zhou and Zhang, 1985; Duan et al., 1986; Zhu and Wittke, 1989), with a putative occurrence from slightly older strata (Archaeuloma taoyuanensis-Leiagnostus cf. bexelli to Mictosaukia striata-Fatocephalus Assemblage Zones) in South China (Peng, 1984).
Onychopyge Harrington, 1938 was originally erected from the Tremadocian of Argentina (Harrington and Leanza, 1957) and subsequently was documented from the uppermost Cambrian of Australia (Shergold, 1975) and North China (Zhou and Zhang, 1978; Lu et al., 1984; Qian, 1986), and the Tremadocian of Mexico (Robison and Pantoja-Alor, 1968), Bolivia (Suarez-Soruco, 1975; Privyl and Vanek, 1980), South China (Peng, 1984, 1990), and Tasmania (Jell, 1985). However, the new GSSP for the Cambrian-Ordovician boundary (Cooper et al., 2001) redefines some previous Tremadocian occurrences for Onychopyge as uppermost Cambrian in age. One example is the occurrence of O. riojana Harrington, 1938 from the lower part of the Parabolina frequens argentina Zone of Argentina (Tortello and Esteban, 1999). In any event, Onychopyge has a relatively long stratigraphie range from Upper Cambrian to lower Tremadocian. The oldest species, O. primitiva Lu et al., 1984 from Nei Mongol of North China, was reported from the Sinoeremoceras Assemblage (upper Fengshanian) of North China. Younger species include O. tricuspis Lu et al., 1984 and O. peculiaris Lu et al., 1984 from Nei Mongol, O. borealis from the ‘ Missisquoia’ perpetis to RichardsonellaTroedssonia Zones of North China (Zhou and Zhang, 1985; Qian, 1986; Duan et al., 1986), and O. assula Shergold, 1975 from the Cordylodus proavus Zone of Australia. The early Tremadocian representatives are O. austrina Peng, 1984 from the Hysterolenus- Onychopyge Zone of South China (Peng, 1990), O. parkerae Jell, 1985 from Tasmania, O. sp. from New Zealand (Wright et al., 1994), several species of Onychopyge from Argentina (Harrington, 1938; Harrington and Leanza, 1957), O. branisi SuarezSoruco, 1975 and O. tarijensis Privyl and Vanek, 1980 from Bolivia, and O. sculptura Robison and Pantoja-Alor, 1968 from Mexico. The stratigraphic and geographic occurrences of Onychopyge suggest that the genus may have originated from Nei Mongol of North China in Late Cambrian times, subsequently migrated into other regions of Gondwana, and eventually became extinct during the Tremadocian.
Pseudokoldinioidia is a missisquoiid genus endemic to China and Korea. The oldest species are P. granulosa Endo, 1944, P. taiziheensis Duan et al., 1986, and P. hemicycla Duan et al., 2005, all from the Ptychaspis-Tsinania Zone (early Fengshanian) of Liaoning, North China. Uppermost Cambrian species includes P. perpetis and P. funingensis Duan et al., 2005 from the Mictosaukia- Fatocephalus and ‘Missisquoia’ perpetis Zones of North China and P. expansa Lu and Zhou, 1990 from the Mictosaukia guizhouensis Zone of Guizhou Province, South China. Pseudokoldinioidia perpetis has been most frequently reported from the Sino-Korean Block, including Nei Mongol, Shanxi, Hebei, Shandong, Liaoning, and Jilin Provinces of China and Korea. The sole Ordovician occurrence of the genus is P. encrinuroides Lu and Zhou, 1990 from the lower Tremadocian of Guizhou Province, South China.
In summary, closely comparable faunas to the Pseudokoldinioidia Fauna are widespread in North China (Zhou and Zhang, 1985; Duan et al., 1986; Qian, 1986). The co-occurrence of Pseudokoldinioidia perpetis and Onychopyge borealis from the ‘Misisquoia’ perpetis Assemblage Zone (Zhou and Zhang, 1985; Qian, 1986; Chen et al, 1988) and the lower part of the Richardsonella-Troedssonia Zone (equivalent to the ”Missisquoia’ perpetis Assemblage Zone) of North China (Duan et al., 1986) clearly indicate that the Pseudokoldinioidia Fauna of Korea is contemporaneous at least in part with those units in North China (Fig. 3).
It is not easy to correlate the Pseudokoldinioidia Fauna with those outside of the Sino-Korean Block, as its constituent species have rarely been found in other parts of the world. The occurrences of Koldinioidia, Pseudokoldinioidia, and Onychopyge in South China allow only imprecise correlation with the Pseudokoldinioidia Fauna (Fig. 3). Peng (1984) recovered Koldinioidia cf. typicalis from the Archaeuloma taoyuanensis-Leiagnostus cf. bexelli to Mictosaukia striata-Fatocephalus Assemblage Zones and Onychopyge austrina from the Hysterolenus-Onychopyge Assemblage Zone of Hunan Province. Therefore the Pseudokoldinioidia Fauna can be correlated with part of the interval between the Archaeuloma taoyuanensis-Leiagnostus cf. bexelli and Hysterolenus-Onychopyge Assemblage Zones of South China (Fig. 3). Lu and Zhou (1990) recorded Pseudokoldinioidia expansa and P. encrinuroides from the Mictosaukia guizhouensis and overlying Troedssonia wimani-Pseudokoldinioidia expansa Assemblage Zones of Guizhou Province, both of which are assigned to the uppermost Cambrian to lower Tremadocian.
FIGURE 3-Stratigraphic correlation of the Pseudokoldinioidia Fauna of Korea with coeval zones of other parts of the world. Modified from Shergold (1988), Geyer and Shergold (2000), Choi et al. (2003), and Miller et al. (2003).
Trilobite-based correlation with Australia is also difficult, even though Koldinioidia and Onychopyge have been documented there. Koldinioidia cf. cylindrica (Shergold, 1972) and K. payntonensis Shergold, 1975 from the Iverian and Payntonian Stages seem to represent early forms of the genus, while Onychopyge assula was recovered from the uppermost Cambrian Cordylodus proavus Zone (Datsonian) of Queensland (Shergold, 1975) and is therefore closer in age to the Pseudokoldinioidia Fauna. Onychopyge parkerae from Tasmania is associated with a fauna of Tremadocian affinity (Jell, 1985). Elsewhere, both Koldinioidia and Onychopyge occur in the strata across the Cambrian-Ordovician boundary interval in Mexico (Robison and Pantoja-Alor, 1968) and South America (Harrington and Leanza, 1957; Privyl and Vanek, 1980). These co-occurrences of Koldinioidia and Onychopyge suggest that the Sino-Korean Block had a biogeographic link with South America and Mexico in the early Paleozoic, even though they were located far away from each other.
In the past, ‘Missisquoia’ in North China (Zhou and Zhang, 1985; Qian, 1986; Chen et al., 1988) was considered to be a good biostratigraphic marker for correlation with Laurentia: i.e., the ‘Missisquoia’ perpetis Zone was correlated with the Missisquoia typicalis Subzone of Laurentia (Shergold, 1988; Chen et al., 1988). However, ‘Missisquoia’ in North China is morphologically distinct from the Laurentian Missisquoia (see below) and therefore its biostratigraphic significance should be reassessed. Fortunately, detailed information on the trilobite and conodont assemblages across the Cambrian-Ordovician boundary intervals is available both in North China (Zhou and Zhang, 1985; Duan et al., 1986; Qian, 1986; Chen et al., 1988) and Laurentia (Ross et al., 1997; Miller et al., 2003). Chen et al. (1988) equated the ‘Missisquoia’ perpetis Zone of North China with the middle part of the Cordylodus proavus Zone, based on the occurrence of Fryxellodontus inornatus Miller, 1969. Similarly the bases of the Missisquoia typicalis Subzone of the Missisquoia Zone and the Fryxellodontus inornatus conodont Subzone of the Cordylodus proavus Zone correspond precisely in Laurentia (Ross et al., 1997; Miller et al., 2003). Therefore, the revised taxonomy of the missisquoiids in eastern Asia does not alter the previous biostratigraphic framework. In short, the base of the ‘Missisquoia’ perpetis Zone of North China, equivalent to the lowest occurrence of the Pseudokoldinioidia Fauna of Korea, is still confidently correlated with the base of the Missisquoia typicalis Subzone of Laurentia (Fig. 3). SYSTEMATIC PALEONTOLOGY
The morphological terms generally follow Whittington and Kelly (1997), but the term ‘glabella’, as used here, excludes the occipital ring. Descriptive terms for glabellar furrows and facial sutures are adopted from Henningsmoen (1957). All of the specimens described in this paper are reposited in the paleontological collections of Seoul National University, Korea, under the registered SNUP numbers.
Order AGNOSTIDA Salter, 1864
Suborder AGNOSTINA Salter, 1864
Family AGNOSTIDAE M’Coy, 1849
Subfamily AGNOSTINAE M’Coy, 1849
Genus MICRAGNOSTUS Howell, 1935
Type species.-Agnostus calvus Lake, 1906 from the Tremadocian of Wales (by original designation).
Discussion.-Since Fortey (1980) proposed that Micragnostus can be distinguished from Geragnostus Howell, 1935 by its transverse and straight F3 and posteriorly located glabellar node, a number of Upper Cambrian and Lower Ordovician agnostids were transferred to Micragnostus (Ludvigsen et al., 1989; Sun, 1989; Nielsen, 1997). Nonetheless, the generic concept of Micragnostus does not appear to be resolved in relation to closely comparable genera such as Homagnostus Howell, 1935, Oncagnostus Whitehouse, 1936, Trilobagnostus Harrington, 1938, and Innitagnostus Opik, 1967 (Shergold and Sdzuy, 1984; Ludvigsen et al., 1989; Sun, 1989; Shergold et al., 1990; Pratt, 1992; Nielsen, 1997; Peng et al., 1999; Choi et al., 2004b). Among others, Micragnostus may be distinguishable from Homagnostus by the absence of median preglabellar furrow and comparatively shorter pygidial axis (Robison and Pantoja-Alor, 1968; Fortey, 1980).
FIGURE 4-Micragnostus chiushuensis (Kobayashi, 1931) from the Pseudokoldinioidia Fauna, Dongjeom Formation, Seokgaejae section, Taebaeksan Basin, Korea. 1, SNUP3026, incomplete small cephalon, x 12; 2, SNUP3009, ventral surface of incomplete cephalon, x 11; 3, SNUP3027, incomplete cephalon showing backwardly bent transglabellar furrow and faint F2, x 9; 4, SNUP3028, incomplete large cephalon showing faint F2 and vestige of median preglabellar furrow, x 7; 5, SNUP3029, ventral surface of nearly complete pygidium with narrow axis and broad border and doublure, x 14; 6, SNUP3030, ventral surface of incomplete pygidium, x 14; 7, SNUP3031, ventral surface of partly broken pygidium with relatively wide axis and long spine, x 9; 8, SNUP3032, large pygidium with narrow axis, x 9.
MICRAGNOSTUS CHIUSHUENSIS (Kobayashi, 1931)
Agnostus chiushuensis KOBAYASHI, 1931, p. 173, pl. 22, figs. 1- 5; ENDO in ENDO AND RESSER, 1937, p. 315, pl. 70, fig. 2; pl. 73, figs. 7-9.
Geragnostus spinosus CHIEN, 1961, p. 93, pl. 1, figs. 8-9.
Geragnostus intermedius PALMER, 1968, p. 24, pl. 12, figs. 1-2; ROBISON AND PANTOJA-ALOR, 1968, p. 776, pl. 97, figs. 1-10; STITT, 1977, p. 36, pl. 1, fig. 1.
Geragnostus (Micragnostus) chiushuensis (Kobayashi). ZHOU AND ZHANG, 1978, p. 6, pl. 1, figs. 1-2; LU AND LIN, 1984, p. 48, pl. 1, figs. 4-8; PENG, 1984, p. 315, pl. 1, figs. 3-7; ZHOU AND ZHANG, 1985, p. 65, pl. 1, figs. 6-9; pl. 3, figs. 8-12; pl. 13, figs. 1- 4; pl. 15, figs. 1-5; pl. 18, figs. 1-2; pl. 20, figs. 1-4; pl. 22, figs. 16-18; pl. 17, figs. 8-14; QIAN, 1985a, p. 65, pl. 9, figs. 5- 7, 12b; pl. 19, fig. 3b; pl. 20, fig. 5a; DUAN, AN, AND ZHAO, 1986, p. 30, pl. 1, figs. 1-3, 4a, 5-6; pl. 8, fig. 20b; pl. 21, fig. 3b; pl. 22, fig. 7b; pl. 26, fig. 3b; DEAN, 1989, p. 15, pl. 1, figs. 2- 11; ZHU AND WITTKE, 1989, p. 209, pl. 1, figs. 3-6.
Geragnostus (Micragnostus) sp. ZHOU AND ZHANG, 1978, p. 7, pl. 1, fig. 3.
Homagnostus zhuangliensis QIAN, 1985b, p. 138, pl. 1, figs. 1, 10- 11.
Micragnostus intermedius (Palmer). PRATT, 1988, p. 1597, figs. 81- r.
Micragnostus chiushuensis (Kobayashi). SUN, 1989, p. 72, pl. 2, figs. 1-8; WESTROP, 1995, p. 15, pl. 1, figs. 14-16; RAO AND TORTELLO, 1998, p. 38, figs. 4a-f; PENG, GEYER, AND HAMDI, 1999, p. 12, fig. 3.
Geragnostus (Micragnostus) elongatus CHIEN. LU AND ZHOU, 1990, p. 12, pl. 1, figs. 1-3.
Trilobagnostus chiushuensis (Kobayashi). TORTELLO, RABANO, RAO, AND ACENOLAZA, 1999, p. 9. figs. 3a-c; TORTELLO AND RAO, 2000, p. 69, figs. 3a-c.
Material examined.-Fourteen cephala and 19 pygidia; all but three cephala and three pygidia show ventral surface.
Occurrence.-Pseudokoldinioidia Fauna; Unit SCO29; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-Micragnostus chiushuensis has been known to display a range of morphological variations in degree of glabellar tapering, length and width ratio of pygidial axis, and deliquiateness of border furrows (Lu and Lin, 1984; Peng, 1984; Zhou and Zhang, 1985; Peng et al., 1999). Some specimens even show the vestige of a median preglabellar furrow (Palmer, 1968; Robison and Pantoja-Alor, 1968; Peng et al., 1999). Such a vestige was interpreted to indicate gradual loss of the furrow in transitional populations derived from Homagnostus (Robison and Pantoja-Alor, 1968).
The broad species concept of M. chiushuensis is clearly reflected in the synonymy presented by Peng et al. (1999), which is generally accepted herein. However, some of the species in the synonym list of Peng et al. (1999) should be excluded from M. chiushuensis: Homagnostus comptus Palmer, 1962 from the Glyptagnostus reticulatus Zone of Nevada by wider cranidium and laterally inflated lateral glabellar lobes; Geragnostus (Micragnostus) mutabilis Ergaliev, 1980 from the uppermost Cambrian of Kazakhstan by small and triangular anterior glabellar lobe; Connagnostus lubris Qian, 1994 from the Chuangia Zone (lower Upper Cambrian) of North China by considerably broad pygidial axis; and M. intermedius (Palmer, 1968) by Ludvigsen et al. (1989) from the Sunwaptan of Newfoundland by the presence of distinct median preglabellar furrow. On the other hand, Geragnostus spinosus Chien, 1961 and Geragnostus (Micragnostus) elongatus Chien, 1961 in Lu and Zhou (1990) from the uppermost Cambrian of Guizhou, South China are better assignable to M. chiushuensis.
Order PTYCHOPARIIDA Swinnerton, 1915
Suborder PTYCHOPARIINA Richter, 1932
Family SHUMARDHDAE Lake, 1907
Genus KOLDINIOIDIA Kobayashi, 1931
Type species.-Koldinioidia typicalis Kobayashi, 1931 from the Upper Cambrian of Liaoning Province, North China (by original designation).
Diagnosis.-A shumardiid with parallel-sided or gently tapering glabella; anterolateral lobes absent to weakly developed; preglabellar furrow effaced or well-defined.
Discussion.-The holotype of Koldinioidia typicalis from Liaoning, North China was poorly preserved (Kobayashi, 1931). Subsequent studies (Shergold, 1975; Zhang and Jell, 1987) suggested that lack of preglabellar furrow can serve as a diagnostic feature of the species. Zhou and Zhang (1985) erected a new genus Akoldinioidia to accommodate the forms with well-defined preglabellar furrow among species referred formerly to Koldinioidia, an action that was subsequently endorsed by Qian (1986), Duan et al. (1986), Peng (1992), and Peng et al. (1999). The morphological variability and related taxonomic problems within the Cambrian shumardiids were thoroughly discussed by Shergold (1991), who treated Akoldinioidia as a junior synonym of Koldinioidia. Shergold’s concept of Koldinioidia is followed in this study.
KOLDINIOIDIA TYPICALIS Kobayashi, 1931
Koldinioidia typicalis KOBAYASHI, 1931, p. 187, pl. 22, figs. 8b, 9; LU, CHANO, CHU, CHIEN, AND HSIANG, 1965, p. 155, pl. 25, figs. 11- 12; ZHANG AND JELL, 1987, p. 242, pl. 119, fig. 13.
Koldinioidia infrequens RESSER AND ENDO in ENDO AND RESSER, 1937, p. 229, pl. 57, fig. 14.
Koldinioidia cf. typicalis Kobayashi. PENG, 1984, p. 326-327, pl. 15, figs. 12-14.
Shumardia (Koldinioidia) typicalis (Kobayashi). ZHOU AND ZHANG, 1985, p. 72-73, pl. 1, figs. 15-17; pl. 3, figs. 6-7; pl. 18, figs. 6-7; pl. 20, figs. 9-11; pl. 22, fig. 20; pl. 24, fig. 14; pl. 26, figs. 15-20; pl. 28, fig. 8; DUAN, AN, AND ZHAO, 1986, p. 32-33, pl. 1, figs. 17-24; pl. 9, fig. 6d; pl. 15, fig. lib; ZHU AND WITTKE, 1989, p. 211, pl. 2, figs. 1-5; pl. 3, figs. 1-2.
Diagnosis.-A species of Koldinioidia with moderately to strongly effaced preglabellar furrow on dorsal shield and weakly developed anterolateral glabellar lobes.
Material examined.-Six cranidia including two showing ventral sides.
Occurrence.-Pseudokoldinioidia Fauna; Unit SCO29; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-Although few specimens are available, silicified cranidia reveal important features of dorsal and ventral morphology. The preglabellar furrow is completely effaced on the dorsal surface, but is indicated by sharp contrast in convexity on the ventral side. The ventral surface shows that the glabella is more or less parallel- sided with slightly expanded anterior lobe, which supports the generic concept of Koldinioidia by Shergold (1975, 1991). Order CORYNEXOCHIDA Kobayashi, 1935
Superfamily LEIOSTEGIACEA Bradley, 1925
Family LEIOSTEGIIDAE Bradley, 1925
Leiostegiid genus and species indeterminate
Material examined.-Eleven cranidia, five librigenae, six pygidia, and eight hypostomes.
Occurrence.-Pseudokoldinioidia Fauna; Units SCO29 and SCO30; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-The present material is too poorly preserved to be assigned to the generic level with certainty. Diverse opinions exist on the taxonomy of Cambrian leiostegiids and there seems to be no general agreement on the matter (Kobayashi, 1960; Opik, 1967; Shergold, 1975; Zhou and Zhang, 1978, 1985; Duan et al., 1986). Nevertheless, the specimens on hand fit well with the general morphology of the family in having trapezoidal glabella, no preglabellar field, obsolete glabellar furrows, and semicircular pygidium with a width greater than its length.
Various leiostegiids have been reported from the CambrianOrdovician boundary intervals of the Sino-Korean Block (Zhou and Zhang, 1978, 1985; Kuo et al, 1982; Qian, 1986; Duan et al., 1986; Kim and Choi, 1999). Among these leiostegiids, the present material is most closely comparable to Leiostegium (Leiostegium) granum Kuo and An in Kuo et al., 1982 illustrated by Zhou and Zhang (1985) from the ‘Missisquoia’ perpetis Assemblage Zone of Jilin Province, North China in possessing less rounded anterior glabellar margin, narrow pygidial axis, indistinct pygidial border furrow, and strongly effaced pleural furrows in pygidia. The present hypostomes bear resemblance with those associated with Leiostegium granum and L planilimbatum Kuo and Duan in Kuo et al., 1982 from the lower part of the Richardsonella-Troedssonia Zone (equivalent to the ‘Missisquoia’ perpetis Zone) of Jilin Province, North China.
Family MISSISQUOIIDAE Hupe, 1955
Discussion.-Hupe (1955) erected the family Missisquoiidae under a new superfamily Olenoidae. Shergold (1975) first recognized Parakoldinioidia Endo in Endo and Resser, 1937 as a member of the Missisquoiidae and assigned the Missisquoiidae to the superfamily Leiostegiacea belonging to the Corynexochida, where it has remained in subsequent studies (Ludvigsen, 1982; Fortey and Shergold, 1984; Westrop, 1986; Ludvigsen et al., 1989). Shortly after, a new missisquoiid genus Tangshanaspis was described by Zhou and Zhang (1978) from China. Ludvigsen (1982), however, synonymized Tangshanaspis with Missisquoia, while Fortey (1983) treated Missisquoia as a junior synonym of Parakoldinioidia. Jell and Stait (1985) put Tasmanocephalus Kobayashi, 1936 from Tasmania into the Missisquoiidae and also suggested that Parakoldinioidia has a priority over Missisquoia and Lunacrania Kobayashi, 1955. In this study, Missisquoia is treated as a valid genus distinguished from both Tangshanaspis and Parakoldinioidia in glabellar morphology: i.e., Missisquoia has forward-tapering or elliptical glabella, whereas the latter two genera are characterized by constricted glabella.
In late 1980s and 1990s, missisquoiid trilobites were frequently reported in China. Zhou and Zhang (1985) introduced a new species, Missisquoia perpetis, from North China. Qian (1985b) and Duan et al. (1986) established several new species of Pseudokoldinioidia from North China and allocated them to the Missisquoiidae. Recently Zhang and Peng (1998) proposed a new missisquoiid genus Fuzhouwania from the Kaolishania pustulosa Zone of Shandong and Liaoning Provinces, North China. Duan et al. (2005) added new species of Parakoldinioidia and Pseudokoldinioidia from Hebei Province, North China.
Shergold et al. (1988), in a comprehensive discussion on the Missisquoiidae, included Parakoldinioidia, Missisquoia, Tangshanaspis, Lunacrania, and Pseudokoldinioidia in the family, but preferred familial assignment of Tasmanocephalus to the Styginidae. Jell and Adrain (2003) listed six genera under the family Missisquoiidae: Fuzhouwania, Hardyia Walcott, 1924, Lunacrania, Parakoldinioidia, Pseudokoldinioidia, and Tasmanocephalus; Missisquoia was synonymized with Parakoldinioidia. Missisquoiidae is therefore in dire need of more rigorous taxonomic review, which is unfortunately beyond the scope of this study.
Genus PSEUDOKOLDINIOIDIA Endo, 1944
Pseudokoldinioidia ENDO, 1944, p. 72; QIAN, 1985b, p. 152; DUAN, AN, AND ZHAO, 1986, p. 41; Lu AND ZHOU, 1990, p. 44.
Type species.-Pseudokoldinioidia granulosa Endo, 1944 from the Tsinania canens Zone of the Yenchou Formation, Liaoning Province, China (by original designation).
Diagnosis.-Cranidium convex, semicircular; glabella broad, expanding forward, without longitudinal median glabellar furrow; palpebral lobes moderate in size, centered at or behind glabellar mid-point; eye ridges present; glabellar front and anterior border in contact tightly; anterior border short and broadly arched. Pygidium strongly convex and semicircular; pygidial axis with five to seven axial rings and a terminal piece; pleural and interpleural furrows clearly incised; one to two anterior pleurae marginally spinose; border narrow, convex, and uniform in width.
Discussion.-Pseudokoldinioidia was originally poorly understood due to inadequate illustration and inaccessibility of the type material. Recent studies from China (Duan et al., 1986; Lu and Zhou, 1990) made it possible to characterize its morphological features, which are included in the generic diagnosis. Pseudokoldinioidia has been frequently compared with closely related genera, such as Parakoldinioidia and Missisquoia. Parakoldinioidia is readily distinguished from Pseudokoldinioidia by its constricted glabella, presence of longitudinal median glabellar furrow, bluntly triangular anterior border, and low convexity of cranidium. Zhou and Zhang (1985) interpreted the forwardly expanding glabella of Pseudokoldinioidia as a trait suitable for use at the species level within Missisquoia, citing a broad spectrum of glabellar shapes displayed by species within the genus. Certainly Missisquoia displays a variety of glabellar morphologies; e.g., forwardly tapering (M. typicalis Shaw, 1951) and bulging in the middle (M. inflata Winston and Nicholls, 1967). However, no species displays an anteriorly expanding glabella. Pseudokoldinioidia invariably has a forwardly expanding glabella, by which it can be differentiated from Missisquoia.
FIGURE 5-1-4, Koldinioidia typicalis Kobayashi, 1931 from the Pseudokoldinioidia Fauna, Dongjeom Formation, Seokgaejae section, Taebaeksan Basin, Korea. 1, SNUP3033, slightly distorted cranidium with occipital node, plan view, x 17; 2, antero-lateral view of SNUP3033, x 16; 3, SNUP3034, ventral surface of incomplete cranidium clearly showing the position of preglabellar furrow, x 21; 4, SNUP3035, partly broken isolated specimen showing stout acute genal angle, x 19. 5-77, leiostegiid genus and species indeterminate. 5, SNUP3036, oblique view of partially preserved cranidium showing ventral aspect of anterior border and preocular facial suture which is nearly unobservable in plan view due to steep slope, x 10; 6, SNUP3037, incomplete cranidium showing pustulate dorsal surface, x 6; 7, SNUP3038, incomplete cranidium with abraded dorsal surface, x 3.5; 8, SNUP3039, latex cast of partially exfoliated cranidium, x 3.5; 9, SNUP3040, partly broken isolated hypostome, plan view, x 12; 10, postero-lateral view of SNUP3040, x 12; 11, SNUP3041, nearly complete small hypostome, x 13; 12, SNUP3042, dorsal surface of partly exfoliated librigena, x 2.3; 13, oblique view of SNUP3042 showing lirae on abaxial margin, x 2.8; 14, SNUP3043, oblique view of ventral surface of librigena showing lirae on doublure and pits in genal field, x 5.5; 15, SNUP3044, partly preserved dorsal surface of pygidium showing very faint anterior pleural furrows on exfoliated pleural field, x 2.2; 16, SNUP3045, adaxially exfoliated dorsal surface of incomplete pygidium showing nearly smooth pleura) field, x 2.4; 17, SNUP3046, ventral surface of partly exfoliated incomplete pygidium showing lirae on doublure, x 2.8.
During the last two decades, eight species and one subspecies were added to Pseudokoldinioidia in China: P. perpetis (Zhou and Zhang, 1985), P. bifiircata Qian, 1985b, P. perpetis wennanensis An in Duan et al., 1986, P. huinanensis Duan and An in Duan et al., 1986, P. taiziheensis Duan and An in Duan et al., 1986, P. expansa Lu and Zhou, 1990, P. encrinuroides Lu and Zhou, 1990, P. hemicycla Duan in Duan et al., 2005, and P. funingensis Duan in Duan et al., 2005. However, Pseudokoldinioidia bifiircata from the Upper Cambrian of Anhui Province is too poorly preserved to assess the specific diagnosis. Duan et al. (1986) systematically explored Pseudokoldinioidia and were able to differentiate the genus from other allied genera such as Missisquoia, Parakoldinioidia, and Tangshanaspis. We basically concur with the proposal of Duan et al. (1986) with some modification: Missisquoia perpetis Zhou and Zhang, 1985 is transferred to Pseudokoldinioidia; a new subspecies, P. perpetis wennanensis An in Duan et al., 1986, can be accommodated within the morphological spectrum of P. perpetis; Pseudokoldinioidia huinanensis is difficult to evaluate due to poor illustration and is provisionally retained within the genus; and cranidia of Pseudokoldinioidia taiziheensis Duan and An in Duan et al., 1986 from the Ptychaspis-Tsinania Zone display the morphological features of the genus, but the pygidia assigned to the species cannot be accommodated within Pseudokoldinioidia.
FIGURE 6-Pseudokoldinioidia perpetis (Zhou and Zhang, 1985) from the Pseudokoldinioidia Fauna, Dongjeom Formation, Seokgaejae section, Taebaeksan Basin, Korea. 1, SNUP3024, partly broken and slightly distorted cranidium, x 9; 2, oblique anterior view of SNUP3024, x 10; 3, SNUP3047, incomplete isolated cranidium, x 9; 4, lateral view of SNUP3047, x 10; 5, SNUP3011, ventral surface of cranidium, x 5; 6, SNUP3048, nearly complete librigena, dorsal view, x 7; 7, lateral view of SNUP3048, x 7; 8, enlarged oblique view of SNUP3048 showing eye socle area, x 10; 9, SNUP3049, incomplete pygidium showing pustulate prosopon and distinct interpleural furrows, x 4; 10, SNUP3012, anterior view of ventral surface of partly broken pygidium showing strong convexity, x 9; 11, plan view of SNUP3012, x 9. PSEUDOKOLDINIOIDIA PERPETIS (Zhou and Zhang, 1985)
Leiostegium (Alloleiostegium) punctatum ZHOU AND ZHANO, 1978 (in part), p. 13, pl. 2, fig. 8.
Missisquoia perpetis ZHOU AND ZHANG, 1985, p. 93, pl. 4, figs. 6- 7; pl. 8, figs. 5-7; pl. 18, figs. 8-12; pl. 21, figs. 1-4; pl. 22, figs. 13-15; pl. 23, figs. 13-15; pl. 24, figs. 5-10; pl. 25, figs. 4-6; pl. 27, figs. 1-2; pl. 28, fig. 12; QIAN, 1986, p. 272, pl. 70, figs. 8-9.
Pseudokoldinioidia perpetis (ZHOUAND ZHANG). DUAN, AN, AND ZHAO, 1986, p. 41, pl. 3, figs. 1-14.
Pseudokoldinioidia perpetis wennanensis AN in DUAN, AN, AND ZHAO, 1986, p. 42, pl. 3, fig. 15.
Diagnosis.-A species of Pseudokoldinioidia having palpebral lobes located slightly posterior to glabellar midpoint, relatively wide fixigenal area (ca. two-thirds of glabellar width), strongly convex semicircular pygidium with well denned pleural and interpleural furrows, and pustulate prosopon.
Material examined.-Eleven incomplete cranidia, 18 pygidia, and three librigenae.
Occurrence.-Pseudokoldinioidia Fauna; Unit SCO29; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-Pseudokoldinioidia perpetis is characterized by forwardly less expanding glabella and more anteriorly located palpebral lobes than early forms such as P. hemicycla and P. taiziheensis from the Ptychaspis-Tsinania Zone of North China. These morphological changes with time may represent evolutionary trends within the Pseudokoldinioidia lineage. Pseudokoldinioidia expansa from South China differs from P. perpetis in having narrower fixed cheeks and more transverse pygidium.
Suborder ASAPHINA Salter, 1864
Family CERATOPYGIDAE Linnarsson, 1869
Genus ONYCHOPYGE Harrington, 1938
Type species.-Onychopyge riojana Harrington, 1938 from the Parabolina argentina Zone (uppermost Cambrian to Tremadocian) of La Rioja, Argentina (by original designation).
Diagnosis.-Ceratopygiid characterized by large palpebral lobes with well-defined palpebral furrows. Preglabellar field absent to very short. Glabella slightly expanding or tapering forward; narrow and elongate bacculae located close to glabellar base. Sl abaxially bifurcate and deeply incised. Anterior border upturned. Postocular suture nearly transverse. Pygidial axis with two to seven rings, weakly to strongly tapering rearward; commonly extending into postaxial ridge. Macropleural first anterior segment with wide pleural furrows prolonged into a distinct pair of spines. Posterior pleural fields smooth to faintly segmented.
Discussion.-Since Onychopyge was established in 1938, a total of 19 species have been assigned to the genus: nine species from North China, one from South China, four from Argentina, two from Bolivia, two from Australia, and one from Mexico. Of the Chinese species, O. primitiva, O. cylindnca Lu et al., 1984, and O. brevica Lu et al., 1984 from Nei Mongol share many morphological features such as strongly tapering pygidial axis with blunt terminal piece, distinct postaxial ridge, moderately broad border, smooth pleural field, and rearward-directed stout macropleural spines, and hence are considered to be conspecific. Onychopyge primitiva has a priority over the latter two. Onychopyge sinica Zhou and O. elongata Zhou in Lu et al. (1984) from Gansu Province, northwestern China are also indistinguishable from each other and the latter is considered a junior synonym of the former.
FIGURE 7-1-20, Onychopyge borealis Zhou and Zhang, 1978 from the Pseudokoldinioidia Fauna, Dongjeom Formation, Seokgaejae section, Taebaeksan Basin, Korea. 1, SNUP3050, juvenile cranidium with relatively long preglabellar field, x 15; 2, SNUP3051, slightly distorted early holaspid cranidium showing strong convexity and upturned anterior border, x 10; 3, lateral view of SNUP3051, x 10; 4, SNUP3052, ventral surface of incomplete cranidium, x 9; 5, SNUP3013, nearly complete but slightly distorted cranidium, x 7.5; 6, SNUP3053, incomplete large cranidium, x 5; 7, SNUP3054, laterally compressed isolated cranidium, x 8.8; 8, oblique anterior view of SNUP3054, x 9; 9, SNUP3055, partially preserved large cranidium, x 4.5; 10, SNUP3056, nearly complete librigena, x 5; 11, SNUP3057, dorsal surface of isolated librigena, plan view, x 7; 12, oblique anterior view of SNUP3057, x 8; 13, SNUP3025, partly broken small pygidium with long macropleural spine and no postaxial ridge, x 10; 14, SNUP3058, ventral surface of pygidium showing indented doublure margin medially, plan view, x 8; 75, oblique view of SNUP3058, x 8; 16, SNUP3059, dorsal surface of relatively large pygidium showing less tapering axis with strong convexity and no postaxial ridge, plan view, x 6; 17, oblique lateral view of SNUP3059, x 6; 18, SNUP3060, ventral surface of incomplete pygidium with rapidly tapering axis and relatively broad doublure, x 4.5; 19, SNUP3061, partially preserved pygidium showing low convexity of terminal piece and faint postaxial ridge, x 6; 20, SNUP3062, ventral surface of incomplete pygidium, x 6. 21, Pilekiid genus and species indeterminate from the Pseudokoldinioidia Fauna, Dongjeom Formation, Seokgaejae section, Taebaeksan Basin, Korea. SNUP3063, ventral surface of incomplete cranidium, x 7.
ONYCHOPYGE BOREALIS Zhou and Zhang, 1978
Onychopyge borealis ZHOU AND ZHANG, 1978, p. 17, pl. 1, figs. 24a- b; ZHOU AND ZHANG, 1985, p. 137, pl. 13, figs. 12-14; pl. 24, fig. 12; DUAN, AN, AND ZHAO, 1986, p. 80, pl. 25, figs. 4-7.
Onychopyge depressa QIAN, 1986, p. 299, pl. 80, figs. 1-6, 11, text-fig. 116.
Diagnosis.-A species of Onychopyge having a transversely elliptical pygidium with relatively short macropleural spines directed obliquely rearward.
Material examined.-Sixteen cranidia (including two late meraspid specimens), 15 holaspid pygidia, and nine librigenae.
Occurrence-Pseudokoldinioidia Fauna; Units SCO29 and SCO30; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-Onychopyge borealis was first established based on an incomplete cranidium from the Onychopyge-Leiostegium (Alloleiostegium) Assemblage Zone of Lulong, Hebei Province, and later Zhou and Zhang (1985) assigned several pygidia from the ‘Missisquoia’ perpetis Zone of Hunjiang, Juin Province to the species. Both the type cranidium and pygidia are however poorly preserved so that it is difficult to characterize their morphological features with clarity. Onychopyge depressa Qian, 1986 from the Alloleiostegium latilum- ‘Missisquoia’ perpetis Assemblage Subzone of the Dayangcha section, Hunjiang, Jilin Province was distinguished from O. borealis by its slender glabella and a depression in the preglabellar field. One of the cranidia (Qian, 1986, pi. 80, fig. 6) assigned to O. depressa with reservation is nearly identical to O. borealis. In addition, pygidia of O. depressa cannot be objectively differentiated from those of O. borealis. Therefore O. depressa is treated as a junior synonym of O. borealis. Duan et al. (1986) collected additional material of Onychopyge from the same locality of Qian (1986) and assigned it to O. borealis. It seems appropriate to suggest that all of these specimens from North China and Korea represent a single species, O. borealis, displaying a range of intraspecific variation.
It is also interesting that pygidia illustrated by Qian (1986) can be divided into two groups: one with more rapidly tapering axis and well-defined postaxial ridge (Qian, 1986, pi. 80, figs. 2-3) and the other with gently tapering axis and faint postaxial ridge (Qian, 1986, pl. 80, figs. 4-5,11). Similar dimorphic pygidia were also recognized in the collections of O. austrina (Peng, 1984) and O. borealis (Zhou and Zhang, 1985), respectively. The occurrence of dimorphic pygidia in the three independent collections might reflect sexual dimorphism.
Valid species of Onychopyge in Asia include O. borealis, O. primitiva, O. tricuspis, O. peculiaris, O. sinica, and O. austrina. Onychopyge borealis is easily distinguished from other species by its transversely wider pygidia with comparatively short macropleural spines directing obliquely rearward. Pygidia of O. primitiva and O. tricuspis have backward-directed macropleural spines of moderate length, while those of O. austrina have oblique backward-directed very long macropleural spines. Onychopyge sinica is readily distinguishable from the other species by its slender and long pygidial axis with five to six axial rings.
Order PHACOPIDA Salter, 1864
Suborder CHEIRURINA Harrington and Leanza, 1957
Superfamily CHEIRUROIDEA Harrington and Leanza, 1957
Family PBLEKIIDAE Sdzuy, 1955
Pilekiid genus and species indeterminate
Material examined.-One cranidium.
Occurrence.-Pseudokoldinioidia Fauna; Unit SCO29; Dongjeom Formation, Taebaeksan Basin, Korea.
Discussion.-This incomplete specimen shows ventral side only, but may be assignable to the Pilekiidae based on the forwardly gently tapering glabella. It seems unprofitable to compare it with any pre- existing genera of the family due to its poor preservation.
We are grateful to J. F. Taylor (Indiana University of Pennsylvania) and an anonymous reviewer for providing many insightful and helpful remarks on the manuscript. Thanks are extended to S. R. Westrop (University of Oklahoma) for his constructive suggestions which greatly improved the final version of the manuscript. Financial support for this study has come from the Korea Research Foundation (Grant No. R14-2003-017-01000-0). This paper is a contribution of the BK 21 Project of the School of Earth and Environmental Sciences, Seoul National University. REFERENCES
BRADLEY, J. H. 1925. Trilobites of the Beekmantown in the Philipsburg region of Quebec. Canadian Field Naturalist, 39:5-9.
CHEN, J.-Y, Y-Y. QIAN, J.-M. ZHANG, Y-K. LIN, L.-M. YIN, Z.-H. WANG, Z.-Z. WANG, J.-D. YANG, AND Y-X. WANG. 1988. The recommended Cambrian-Ordovician global boundary stratotype of the Xiaoyangqiao section (Dayangcha, Juin Province), China. Geological Magazine, 125:415-444.
CHIEN, Y. 1961. Cambrian trilobites from Sandu and Duyun, southern Kweichow. Acta Palaeontologica Sinica, 9:91-129.
CHOI, D. K. 1998. The Yongwol Group (Cambrian-Ordovician) redefined: A proposal for the stratigraphic nomenclature of the Choson Supergroup. Geosciences Journal, 2:220-234.
CHOI, D. K. AND S. K. CHOUGH. 2005. The Cambrian-Ordovician stratigraphy of the Taebaeksan Basin, Korea: A review. Geosciences Journal, 9: 187-214.
CHOI, D. K., D. H. KIM, AND J. W. SOHN. 2001. Ordovician trilobite faunas and depositional history of the Taebaeksan Basin, Korea: Implications for palaeogeography. Alcheringa, 25:53-68.
CHOI, D. K., D. H. KIM, J. W. SOHN, AND S.-B. LEE. 2003. Trilobite faunal successions across the Cambrian-Ordovician boundary intervals in Korea and their correlation with China and Australia. Journal of Asian Earth Sciences, 21:781-793.
CHOI, D. K., S. K. CHOUGH, Y. K. KWON, S.-B. LEE, J. Woo, I. KANG, H. S. LEE, S. M. LEE, J. W. SOHN, Y. J. SHINN, AND D.-J. LEE. 2004a. Taebaek Group (Cambrian-Ordovician) in the Seokgaejae section, Taebaeksan Basin: A refined lower Paleozoic stratrigraphy in Korea. Geosciences Journal, 8:125-151.
CHOI, D. K., J. G. LEE, AND B. C. SHEEN. 2004b. Upper Cambrian agnostoid trilobites from the Machari Formation, Yongwol, Korea. Geobios, 37:159-189.
CHOUGH, S. K., S. T. KWON, J. H. REE, AND D. K. CHOI. 2000. Tectonic and sedimentary evolution of the Korean peninsula: A review and new view. Earth-Science Reviews, 52:175-235.
COOPER, R. A., G. S. NOWLAN, AND S. H. WILLIAMS. 2001. Global stratotype section and point for the base of the Ordovician System. Episodes, 24:1928.
DEAN, W T. 1989. Trilobites from the Survey Peak, Outram and Skoki formations (Upper Cambrian-Lower Ordovician) at Wilcox Pass, Jasper National Park, Alberta. Geological Survey of Canada, Bulletin 389, 141 p.
DUAN, J.-Y., S.-L. AN, AND D. ZHAO. 1986. Cambrian-Ordovician Boundary and its Interval Biotas, Southern Jilin, Northeast China. Changchun College of Geology, Changchun, 124 p.
DUAN, J.-Y, S.-L. AN, P.-J. LIU, X.-D. PENG, AND L.-Q. ZHANG. 2005. The Cambrian Stratigraphy, Faunas and Palaeogeography in Eastern Part of North China Plate. Yayuan Publishing Company, Hong Kong, 255 p. (In Chinese)
ENDO, R. 1944. Restudies on the Cambrian formations and fossils in southern Manchoukuo. Central National Museum of Manchoukuo Bulletin, 7:1-100.
ENDO, R. AND C. E. RESSER. 1937. The Sinian and Cambrian formations and fossils of southern Manchoukuo. Manchurian Science Museum Bulletin, 1: 1-474.
ERGALIEV, G. KH. 1980. Trilobites of the Middle and Upper Cambrian of the Maly Karatau. Akademiya Nauk Kazakhskoi SSR, Institut Geologicheskikh Nauk, Alma-Ata, 211 p. (In Russian)
ERGALIEV, G. KH. 1983. Some Upper Cambrian and Lower Ordovician trilobites of Bolyshoi Karatau and Ulutau, p. 35-66. In M. K. Apollonov, S. M. Bandaletov, and N. K. Ivshin (eds.), The Lower Palaeozoic Stratigraphy and Palaeontology of Kazakhstan. Nauka Kazakh SSR Publishing House, Alma-Ata. (In Russian)
FORTEY, R. A. 1980. The Ordovician trilobites of Spitsbergen 3. Remaining trilobites of the Valhallfonna Formation. Norsk Polarinstitutt Skrifter, 171: 1-163.
FORTEY, R. A. 1983. Cambrian-Ordovician trilobites from the boundary beds in western Newfoundland and their phylogenetic significance. Special Papers in Palaeontology, 30:179-211.
FORTEY, R. A. AND J. H. SHERGOLD. 1984. Early Ordovician trilobites, Nora Formation, Central Australia. Palaeontology, 27:315- 366.
GEYER, G. AND J. H. SHERGOLD. 2000. The quest for internationally recognized divisions of Cambrian time. Episodes, 23:188-195.
HARRINGTON, H. J. 1938. Sobre las faunas del Ordoviciano Inferior del norte Argentine. Revista del Museo de La Plata (Buenos Aires), seccion Paleontologia, new series 1:109-289.
HARRINGTON, H. J. AND A. F. LEANZA. 1957. Ordovician trilobites of Argentina. Department of Geology, University of Kansas Special Publication, 1 : 1-276.
HENNBMGSMOEN, G. 1957. The trilobite family Olenidae with descriptions of Norwegian material and remarks on the olenid and Tremadocian Series. Skrifter utgitt av Del Norske Videnskaps- Akademi i Oslo, I, MatematiskNaturvidenskapelig. Klasse, 1957:1- 303.
HOWELL, B. F. 1935. Cambrian and Ordovician trilobites from Herault, southern France. Journal of Paleontology, 9:222-238.
HUPE, P. 1955. Classification des trilobites. Annales de Paleontologie, 41:91325.
JELL, P. A. 1985. Tremadoc trilobites of the Digger Island Formation, Waratah Bay, Victoria. Memoirs of the Museum of Victoria, 46:53-88.
JELL, P. A. AND J. M. ADRAIN. 2003. Available generic names for trilobites. Memoirs of the Queensland Museum, 48:331-553.
JELL, P. A. AND B. STAIT. 1985. Revision of an early Arenig trilobite faunule from the Caroline Creek Sandstone, near Latrobe, Tasmania. Memoirs of the Museum of Victoria, 46:35-51.
KIM, D. H. AND D. K. CHOI. 1999. Occurrence of Leiostegium (Trilobita, Early Ordovician) from the Mungok Formation. Journal of the Paleontological Society of Korea, 15:109-114.
KOBAYASHI, T. 1931. Studies on the stratigraphy and palaeontology of the Cambro-Ordovician formation of Hua-lie-chai and Niu-hsin- tai, South Manchuria. Japanese Journal of Geology and Geography, 8:131-189.
KOBAYASHI, T. 1935. The Cambro-Ordovician formations and faunas of South Chosen, Palaeontology, Pt. III, Cambrian faunas of South Chosen with a special study on the Cambrian genera and families. Journal of the Faculty of Science, Imperial University of Tokyo, Section 2, 4:49-344.
KOBAYASHI, T. 1936. Three contributions to the Cambro-Ordovician faunas. Japanese Journal of Geology and Geography, 13:163-184.
KOBAYASHI, T. 1953. On the Kainellidae. Japanese Journal of Geology and Geography, 23:37-61.
KOBAYASHI, T. 1955. The Ordovician fossils from the McKay Group in British Columbia, western Canada, with a note on the Early Ordovician palaeogeography. Journal of the Faculty of Science, University of Tokyo, Section 2, 9:355-493.
KOBAYASHI, T. 1960. The Cambro-Ordovician formations and faunas of South Korea, Pt. VII, Paleontology VI. Journal of the Faculty of Science, University of Tokyo, Section 2, 12:329-420.
KOBAYASHI, T. 1966. The Cambro-Ordovician formations and faunas of South Korea, Pt. X, stratigraphy of the Chosen Group in Korea and South Manchuria and its relationship to the Cambro-Ordovician formations of other areas. Section A, the Chosen Group of South Korea. Journal of the Faculty of Science, University of Tokyo, Section 2, 16:1-84.
KUO, K.-C., J.-Y. DUAN, AND S.-L. AN. 1982. Cambrian-Ordovician boundary in the North China Platform with descriptions of trilobites. Journal of Changchun College of Geology, 3:9-28. (In Chinese)
LAKE, P. 1906. A Monograph of the British Cambrian Trilobites, Pt. 1, Palaeontological Society, London, Monograph, 1-28.
LAKE, P 1907. A Monograph of the British Cambrian Trilobites, Pt. 2, Palaeontological Society, London, Monograph, 29-48.
LEE, S.-B., B. LEFEBVRE, AND D. K. CHOI. 2005. Latest Cambrian cornutes (Echinodermata: Stylophora) from the Taebaeksan Basin, Korea. Journal of Paleontology, 79:139-151.
LINNARSSON, J. G. O. 1869. Om Vestergotlands Cambriska och Siluriska aflagringar. Konglisa Svenska Vetenskapsakademiens Handlingar, 8:1-89.
LOCH, J. D., J. H. STITT, AND J. R. DERBY. 1993. Cambrian- Ordovician boundary interval extinctions: Implications of revised trilobite and brachiopod data from Mount Wilson, Alberta, Canada. Journal of Paleontology, 67:497-517.
LU, Y.-H. AND H.-L. LIN. 1984. Late Late Cambrian and earliest Ordovician trilobites of Jiangshan-Changshan area, Zhejiang, p. 45- 164. In Nanjing Institute of Geology and Palaeontology (ed.), Stratigraphy and Palaeontology of Systemic Boundaries in China, Cambrian-Ordovician Boundary, 1. Anhui Science and Technology Publishing House, Hefei.
LU, Y-H. AND T.-R. ZHOU. 1990. Trilobites across the Cambrian- Ordovician boundary of the transitional region of Sandu, southwestern Guizhou. Palaeontologia Cathayana, 5:1-84.
LU, Y-H., Z.-Q. ZHOU, AND Z.-Y. ZHOU. 1984. New materials of Onychopyge faunas, with a discussion on the evolution of Onychopyge (Trilobita). Nanjing Institute of Geology and Palaeontology, Bulletin, 7:69-126. (In Chinese with English abstract)
LU, Y-H., W.-T. CHANG, C.-L. CHU, Y-Y CHIEN, AND L.-W. HSIANG. 1965. Fossils of Each Group of China, Chinese Trilobites. Science Press, Beijing, 766 p. (2 volumes in Chinese)
LUDVIGSEN, R. 1982. Upper Cambrian and Lower Ordovician biostratigraphy of the Rabbitkettle Formation, western District of Mackenzie. Life Science Contributions, Royal Ontario Museum, 134, 188 p.
LUDVIGSEN, R., S. R. WESTROP, AND C. H. KINDLE. 1989. Sunwaptan (Upper Cambrian) trilobites of the Cow Head Group, western Newfoundland, Canada. Palaeontographica Canadiana, 6:1-175.
M’COY, F 1849. On the classification of some British fossil Crustacea with notices of some new forms in the university collections at Cambridge. Annals and Magazine of Natural History, 4:161-179, 330-335, 392-414.
MILLER, J. F. 1969. Conodont fauna of the Notch Peak Limestone (CambroOrdovician), House Range, Utah. Journal of Paleontology, 43:413-439.
MILLER, J. E, K. R. EVANS, J. D. LOCH, R. L. ETHDMGTON, J. H. STITT, L. HOLMER, AND L. E. POPOV. 2003. Stratigraphy of the Sauk IU Interval (Cambrian-Ordovician) in the Ibex Area, western Millard County, Utah and central Texas. Brigham Young University Geology Studies, 47:23-118.
NICOLL, R. S., J. F. MILLER, G. S. NOWLAN, J. E. REPETSKI, AND R. L. ETHDMGTON. 1999. lapetonudus (new genus) and Iapetognathus Landing, unusual earliest Ordovician multielement conodont taxa and their utility for biostratigraphy. Brigham Young University Geology Studies, 44:27-101. NIELSEN, A. T. 1997. A review of Ordovician agnostid genera (Trilobita). Transactions of the Royal Society of Edinburgh, Earth Sciences, 87:463-501.
OPIK, A. A. 1967. The Mindyallan fauna of north-western Queensland. Bulletin of the Bureau of Mineral Resources, Geology and Geophysics 74, 1: 1-404, 2:1-167.
PALMER, A. R. 1962. Glyptagnostus and associated trilobites in the United States. U.S. Geological Survey Professional Paper, 374F:l- 49.
PALMER, A. R. 1968. Cambrian trilobites of East-Central Alaska. U.S. Geological Survey Professional Paper, 559B:1-115.
PENG, S.-C. 1984. Cambrian-Ordovician boundary in the Cili- Taoyuan border area, northwestern Hunan, with descriptions of relative trilobites, p. 285405. In Nanjing Institute of Geology and Palaeontology (ed.), Stratigraphy and Paleontology of Systemic Boundaries in China. Cambrian-Ordovician Boundary 1, Anhui Science and Technology Publishing House, Hefei.
PENG, S.-C. 1990. Tremadoc stratigraphy and trilobite faunas of northwestern Hunan 2. Trilobites from the Panjiazui Formation and the Madaoyu Formation in Jiangnan Slope Belt. Beringeria, 2:55-171.
PENG, S.-C. 1992. Upper Cambrian biostratigraphy and trilobite faunas of the Cili-Taoyuan area, northwestern Hunan, China. Memoir of the Association of Australian Palaeontologists, 13:1-119.
PENG, S.-C., G. GEYER, AND B. HAMDI. 1999. Trilobites from the Shahmirzad section, Alborz Mountains, Iran: Their taxonomy, biostratigraphy and bearing for international correlation. Beringeria, 25:3-66.
PRATT, B. R. 1988. An Ibexian (Early Ordovician) trilobite faunule from the type section of the Rabbitkettle Formation (southern Mackenzie Mountains, Northwest Territories). Canadian Journal of Earth Science, 25:1595-1607.
PRATT, B. R. 1992. Trilobites of the Marjuman and Steptoean stages (Upper Cambrian), Rabbitkettle Formation, southern Mackenzie Mountains, northwest Canada. Palaeontographica Canadiana, 9:1-179.
PRIVYL, A. AND J. VANEK. 1980. Ordovician trilobites of Bolivia. Rozpravy Ceskoslovenske Akademie ved, Rada Matematickych a priodnfch ved, 90: 3-90.
QIAN, Y.-Y. 1985a. Trilobites, p. 65-83. In J.-Y. Chen, Y-Y. Qian, Y-K. Lin, J.-M. Zhang, Z.-H. Wang, L.-M. Yin, and B. D. Erdtmann (eds.), Study on Cambrian-Ordovician Boundary Strata and its Biota in Dayangcha, Hunjiang, Jilin, China. China Prospect Publishing House, Beijing.
QIAN, Y-Y. 1985b. Late Late Cambrian trilobites from the Tangcun Formation of Jingxian, southern Anhui. Palaeontologia Cathayana, 2:137-167.
QIAN, Y-Y. 1986. Trilobites, p. 255-313. In J.-Y. Chen (ed.), Aspects of Cambrian-Ordovician Boundary in Dayangcha, China. China Prospect Publishing House, Beijing.
QIAN, Y-Y 1994. Trilobites from middle Upper Cambrian (Changshan Stage) of North and northeast China. Palaeontologia Sinica, 183, new series B, no. 3,190 p. (In Chinese with English summary)
RAO, R. I. AND M. F. TORTELLO. 1998. Tremadoc conodonts and trilobites from the Cardonal Formation, Incamayo Creek, Salta Province, northwestern Argentina. Palaeontologia Polonica, 58:31- 45.
RICHTER, R. 1932. Crustacea, p. 840-863. In Handworterbuch der Naturwissenschaften (Second edition), Jena.
ROBISON, R. A. AND J. PANTOJA-ALOR. 1968. Tremadocian trilobites from the Nochixtlan region, Oaxaca, Mexico. Journal of Paleontology, 42:767-800.
ROSS JR., R. J., L. F. HINTZE, R. L. ETHINGTON, J. F. MILLER, M. E. TAYLOR, AND J. E. REPETSKI. 1997. The Ibexian, lowermost series in the North American Ordovician. U.S. Geological Survey Professional Paper, 1579:1-50.
SALTER, J. W. 1864. A Monograph of British Trilobites, Pt. 1, Palaeontographical Society, London, Monograph, 1-80.
SDZUY, K. 1955. Die Fauna der Leimitz-Schiefer (Tremadoc). Abhandlungen der Senckenbergischen Untercarbon. Zeitschrift der Deutschen Geologischen Gesellschaft, 52:1-20.
SHAW, A. B. 1951. The paleontology of northwestern Vermont. I. New Late Cambrian trilobites. Journal of Paleontology, 25:97-114.
SHERGOLD, J. H. 1972. Late Cambrian trilobites from the GoIa Beds, western Queensland. Bureau of Mineral Resources, Geology and Geophysics, Bulletin, 112:1-126.
SHERGOLD, J. H. 1975. Late Cambrian and Early Ordovician trilobites from the Burke River structural belt, western Queensland, Australia. Bureau of Mineral Resources, Geology and Geophysics, Bulletin, 153:1-251.
SHERGOLD, J. H. 1988. Review of trilobite biofacies distributions at the Cambrian-Ordovician boundary. Geological Magazine, 125:363- 380.
SHERGOLD, J. H. 1991. The Pacoota Sandstone, Amadeus Basin, Northern Territory: Stratigraphy and palaeontology. Bureau of Mineral Resources, Geology and Geophysics, Bulletin, 237:1-93.
SHERGOLD, J. H. AND K. SDZUY. 1984. Cambrian and early Tremadocian trilobites from Sultan Dag, central Turkey. Senckenbergiana lethaea, 65: 51-135.
SHERGOUJ, J. H., J. R. LAURIE, AND X.-W. SUN. 1990. Classification and review of the trilobite order Agnostida Salter, 1864: An Australian perspective. Bureau of Mineral Resources, Geology and Geophysics Report, 296:1-93.
SOHN, J. W. AND D. K. CHOI. 2002. An uppermost Cambrian trilobite fauna from the Yongwol Group, Taebaeksan Basin, Korea. Ameghiniana, 39:59-76.
STITT, J. H. 1971. Late Cambrian and earliest Ordovician trilobites, Timbered Hills and lower Arbuckle groups. West