A synopsis of Paleocene stratigraphy and vertebrate paleontology in the Qianshan Basin, Anhui, China

wANG Yuan-QingLI Chuan-KuiLI QianLI Ding-Sheng

(1Key Laboratory of Vertebrate Evolution and Human Origins of Chinese Academy of Sciences,Institute of Vertebrate Paleontology and Paleoanthropology,Chinese Academy of SciencesBeijing 100044 wangyuanqing@ivpp.ac.cn)

(2Qianshan County MuseumQianshan, Anhui 246300)

A synopsis of Paleocene stratigraphy and vertebrate paleontology in the Qianshan Basin, Anhui, China

wANG Yuan-Qing1LI Chuan-Kui1LI Qian1LI Ding-Sheng2

(1Key Laboratory of Vertebrate Evolution and Human Origins of Chinese Academy of Sciences,Institute of Vertebrate Paleontology and Paleoanthropology,Chinese Academy of SciencesBeijing 100044 wangyuanqing@ivpp.ac.cn)

(2Qianshan County MuseumQianshan, Anhui 246300)

The Mesozoic and Cenozoic redbeds in the Qianshan Basin comprise a set of monocline clastic rocks and are subdivided into the Late Cretaceous Gaohebu Formation, the Paleocene wanghudun Formation (including the Lower, Middle, and Upper members) and Doumu Formation (including the Lower and Upper members). Continuous investigations in the Qianshan Basin since 1970 have resulted in discovery of a lot of vertebrate specimens. Up to date, 61 species (including 9 unnamed ones) in 45 genera of vertebrates, representing reptiles, birds and mammals, have been reported from the Paleocene of the Qianshan Basin. Among them, mammals are most diverse and have been classi fi ed into 46 species (7 unnamed) of 33 genera, representing 16 families in 10 orders. According to their stratigraphic occurrence, seven fossiliferous horizons can be recognized in the Qianshan Paleocene. Based on the evidence of mammalian biostratigraphy, the strata from the Lower Member through the lower part of the Upper Member of wanghudun Formation could be roughly correlated to the Shanghu Formation of the Nanxiong Basin (Guangdong Province) and the Shizikou Formation of the Chijiang Basin (Jiangxi Province), corresponding to the Shanghuan Asian Land Mammal Age (ALMA). Both the upper part of the Upper Member of wanghudun Formation and the Doumu Formation could be correlated to the Nongshan Formation of the Nanxiong Basin and the Chijiang Formation of the Chijiang Basin, corresponding to the Nongshanian ALMA. Paleomagnetic results from several Chinese Paleocene basins suggest that the Shanghuan is roughly correlative to the Puercan and Torrejonian North American Land Mammal Ages (NALMA), while the Nongshanian correlative to the early to middle Tiffanian (Ti1-4a). The Shanghuan and the Nongshanian are probably correlated to the Danian and the Selandian of the Global Geologic Time Scale. Therefore, all the fossil vertebrates collected in the Qianshan Basin are the Early and Middle Paleocene in age.

Qianshan, Anhui; Paleocene; vertebrates; stratigraphy; correlation

1 Introduction

The Qianshan Basin, located in southwestern Anhui Province, China, is a small foreland basin on the east side of the Dabie Mountains, and comprises parts of Qianshan, Tongcheng, Taihu, Huaining, Zongyang and Lujiang counties (Chen, 1974). The basin, with northeastly extension, is about 100 km long in east-west direction and no more than 25 km in northsouth direction. It is bordered by a fault northwestward with the mountainous area formed by metabolic rocks and is ful fi lled by the Late Cretaceous-Paleocene fl uvio-lacustrine deposits that are mainly reddish colored clastic rocks. In 1950s when the nation-wide geological survey was initiated in China, the Hefei University of Technology carried out the fi rst investigation to the Mesozoic and Cenozoic deposits in the Qianshan Basin. Later in 1960s when they carried out geological mapping in this area, the geologists of the Geological Survey Team No. 311 of the Bureau of Geology and Mineral Resources of Anhui Province first found Paleocene vertebrates at Dinghuawu, Xiaoshi, Huaining County in 1966 (RGSBGA, 1988b). These fossil vertebrates were later identi fi ed as a turtleAnhuichelys siaoshihensisYeh (1979) and an alligatoridEoalligator huiningensisYoung (1982). Such discovery attracted great attention of researchers from the Institute of Vertebrate Paleontology and Paleoanthropology (IVPP), the Chinese Academy of Sciences, Beijing. with the assistance of colleagues of the Geological Survey Team No. 311, the Qianshan County Museum (= former the Administrative Office of Cultural Relics of Qianshan County), and recently the Tianzhushan Global Geopark, the IVPP colleagues carried out a long term investigation that has continuously been lasting nearly half a century since 1970. Up to date, 61 species (including 9 unnamed ones) in 45 genera of Paleocene vertebrates, representing reptiles, birds and mammals, have been reported at 42 localities in the Qianshan Basin.

2 Stratigraphy

Paleocene deposits in the Qianshan Basin was fi rst investigated by a group from the Hefei University of Technology in 1950’s1)) Hefei University of Technology, 1959. Report of the geological survey in Taihu-Susong area, southeastern Dabie Mountains (1:200000).. They fi rst mentioned the presence of possible Paleogene deposits, though the age determination was inferred on the basis of the nature of sedimentary rocks. The Regional Geological Survey Team No. 311 of the Bureau of Geology of Anhui Province fi rst provided a systematic subdivision of the Paleocene in the Qianshan Basin in a report accomplished in 1970, which was later informally published (Chen,1974). Chen and Xia (1981) formally published the section measured by the geological survey team with some revisions. Their section is as follows:

The wanghudun Section in the Qianshan County

Doumu Formation

14. Purplish red and very thick matrix-supported conglomerats intercalated with coarse sandstone 184.68 m

13. Grayish purple thick matrix-supported conglomerates intercalated with medium-coarse sandstone 140.22 m

12. Purplish red and thick matrix-supported conglomerates interbedded with purplish red coarse sandstone, containing fossil vertebrates:Sinostylops promissusTang & Yan,Archaeolambda tabiensisHaung,Heomys orientalisLi,MimotonawanaLi,Hsuiannaniasp.,TinosaurusdoumuensisHou,Anhuisaurus huainanensisHou 117.78 m

11. Purplish red and thick conglomerate-containing medium-coarse sandstone intercalated with a few thin layers of grayish white arkose 102.58 m

10. Purplish red and thick medium-coarse sandstone interbedded with conglomerates and shales, containing fossil vertebrates:Allictops inserrataQiu,Hsiuannania tabiensisXu,MimotonarobustaLi,Obtususdon hanhuaensisXu,Agama sinensisHou,Anhuicheleys tsienshanensisYeh 76.12 m

wanghudun Formation

9. Purplish red and thick medium- fi ne sandstone intercalated with dark purple muddy shales and few thick conglomerates 157.32 m

8. Covered 307.08 m

7. Fresh purplish red and thick fi ne sandstone intercalated with thin arkose 179.4 m

6. Grayish purple thin to medium thick conglomerates and coarse sandstone interbedded with purplish red fine sandstone, rich in fossil vertebrates:Anictops tabiepedisQiu,Decoredon elongetusXu,Diacronus anhuiensisXu,D.wanghuensisXu,Huaiyangale chianshanensisXu,Harpyodus eurosChiu & Li,MimotonawanaLi,Mimotonasp.,Obtusudon hanhuaensisXu,Paranictops majusculaQiu,Pappictidops orientalisChiu & Li,Zeuctherium nitelesTang & Yan,Heomyssp.,Qianshanosaurus huangpuensisHou 287 m

Haixingdi Formation

5. Purplish red thick medium-fine sandstone interbedded with fine muddy sandstone, intercalated with white arkose and thin conglomerates, containing fossil vertebrates:Bemalambdasp.,Yantanglestes convexusYen & Tang 496.4 m

4. Covered 27.24 m

3. Fresh purplish red thick fi ne sandstone, intercalated with grayish white thin feldspar and quartz sandstone, containing fossil vertebrates:Anictops tabiepedisQiu,AnchilestesChiu & Li,Anaptogale wanghoensisXu,Bemalambdasp.,Wanogale hodungensisXu,Chianshania gianghuaiensisXu,Anqingosaurus breviocephalusHou 418.52 m

2. Purplish red medium-thick coarse sandstone interbedded with thin to medium-thick conglomerates 83.6 m

1. Brick red thick blocky fi ne sandstone, containing fossil vertebrates: primitive pantodont and lizards 268.92 m

——- conformity ——-

Underlying Upper Cretaceous Gaohebu Formation

Qiu et al. (1977) redefined the wanghudun and Doumu formations based on the investigation of the IVPP fi eld crew. According to Qiu et al. (1977), the wanghudun Formation, which is about 1800 m thick, overlies the Cretaceous wanghe Formation (see discussion below) and was subdivided into the Lower, Middle, and Upper members. The Lower Member is composed of purplish red medium-fine sandstone intercalated with conglomerates and grayish white arkose sandstone. The Middle Member consists of mainly interbedded purplish red conglomerates, coarse sandstone, and fine sandstone. No fossil mammals have been recorded from this member. The Upper Member is the most fossiliferous unit in the formation, comprising purplish and brownish red fi ne sandstone intercalated with grayish white arkose sandstone. The Doumu Formation disconformably or conformably overlies the wanghudun Formation and is about 600 m in total thickness. The lower part of the formation, the Lower Member, comprises thick, purplish red medium- fi ne sandstone intercalated with thin conglomerates and silty mudstone, while its upper part, the Upper Member, is composed of mainly interbedded thick conglomerates and sandstone (Qiu et al., 1977). Such subdivision has been widely accepted for Paleocene strata in the Qianshan Basin (e.g. Zheng and Qiu, 1979; Chow and Zheng, 1980; Li and Ting, 1983; Russell and Zhai, 1987; wang et al., 1998).

what should be noted here is the correlation between Chen and Xia’s (1981) and Qiu et al.’s (1977) subdivisions. The Lower and Middle members of wanghudun Formation in Qiu et al.’s subdivision are roughly correlated to the Chen and Xia’s Haixingdi Formation, while the Middle Member of wanghudun Formation roughly corresponds to the upper part of Chen and Xia’s Layer 5. The boundary between the wanghudun Formation and the Doumu Formation of Qiu et al.’s subdivision is roughly located between layers 8 and 9 in Chen and Xia’s. Qiu et al. (1977) adopted the wanghe Formation from an unpublished data of the local geological survey team and used it for the underlying Late Cretaceous deposits. Later, the deposits equivalent to the wanghe Formation was named Gaohebu Formation based on a new section with better exposures2)) Regional Geological Survey of the Bureau of Geology of Anhui Province, 1974. Report of the regional geological survey: Liu’an and Yuexi (1:200000).and the name was cited in some publications (e.g. Chen and Xia, 1981; RGSBGA, 1988a). Here we suggest to replace the wanghe Formation with the Gaohebu Formation.

3 Localities of fossil vertebrates

The Paleocene deposits in the Qianshan Basin have produced a lot of fossil vertebrates at many localities. Forty two localities have been recorded in formally published references (Fig. 1). According to their stratigraphic position, these localities can be grouped in seven fossiliferous horizons recognized in the Qianshan Basin. Five of the horizons are in the wanghudun Formation and the other two are in the Doumu Formation. The localities and fossil vertebrates therefrom are listed as follows (the original locality numbers are in brackets):

Fig. 1 Localities of Paleocene vertebrates in the Qianshan Basin, Anhui Province, China A. A sketch map showing the general location of Anhui Province (shaded) in China; B. A map of Anhui Province showing the location of boxes C and D; C, D. More detailed maps showing the Paleocene vertebrate localities in the Qianshan Basin.Open symbols refer to the Shanghuan localities, while solid ones for the Nongshanian localities. Triangles and circles refer to the localities in the wanghudun and the Doumu formations, respectively.1. Haixingdi (71002); 2. Fanglaowu (71003); 3. wangdawu (71001); 4. wanhuawu (71005); 5. Chidoukan (71006); 6. Dingxiawu (70020); 7. Zhangchong; 8. Sanliantang (70023); 9. Zhongjialaowu; 10. Taowu (70022); 11. Yangwu Southwest (71014); 12. Yangwu west (71019); 13. Lijialaowu (70021); 14. Shangxialou (71016); 15. Zhangjiawu Southwest (71010); 16. Zhangjiawu South (71008); 17. Zhangjiawu Southeast (71011); 18. Zhangjiawu East (71009); 19. Zhangxinwu (71007); 20. wanghudun Northeast; 21. Chenxiawu (71012); 22. Lianhuatang Southeast; 23. Lianhuatang; 24. Fujiashanzui; 25. Xudawu South; 26. Xudawu; 27. Hanhuawu South (71079); 28. Hanhuawu west (71020); 29. Hanxindongwu (71015); 30. Hanjiashanbao; 31. Chongliwu (71018); 32. Zhugongtang west; 33. Meiyuan; 34. Yangxiaowu (71017); 35. Yangxinwu (71071); 36. Dinghuawu (71080); 37. Chenjiachuanmenkou; 38. Mao’an (71075); 39. Jinshi; 40. wangjiazha; 41. Huanghetang Reservoir; 42. Yanglaowu

(1) Localities in the basal part of the Lower Member of wanghudun Formation

Two localities are in this horizon, and represent the lowest vertebrate-bearing bed in the Qianshan Paleocene.

Haixingdi (71002): Bemalambdidae gen. et sp. indet.,QianshanosaurushuangpuensisHou, 1974

Fanglaowu (71003):Astigale wanensisZhang & Tong, 1981,Benaius qianshuiensiswang & Jin, 2004

(2) Localities in the middle part of the Lower Member of wanghudun Formation

Three localities are included in this horizon. Two of them, wangdawu and wanhuawu, are close to the main section, their inclusion is thus credible. Another locality, Dinghuahu, is somewhat far from the main section. Its geographic position and lithologic feature show the possibility in correlation with the other two localities.

wangdawu (71001):Wanogale hodungensisXu, 1976,Chianshania gianghuaiensisXu, 1976,Anaptogale wanghoensisXu, 1976,AnictopstabiepedisQiu, 1977,Anchilestes impolitusChiu & Li, 1977,PlethorodonchienshanensisHuang & Zheng, 1987,Bemalambdasp.,Anqingosaurus brevicephalusHou, 1976,Changjiangosaurus huananensisHou, 1976

wanhuawu (71005):Cartictops caninaDing & Tong, 1979

Dinghuawu (71080):Anhuichelys siaoshihensisYeh, 1979,Eoalligator huiningensisYoung, 1982

(3) Localities in the upper part of the Lower Member of wanghudun Formation Only one locality with fossil vertebrates reported can be referred to this horizon.

Chidoukan (71006):Yantanglestes conexus(Yan & Tang, 1976),Bemalambdasp.,Cartictops caninaDing & Tong, 1979

(4) Localities in the lower part of the Upper Member of wanghudun Formation

This horizon is most fossiliferous in the Qianshan Paleocene. A number of localities were discovered in the horizon. All the localities are near the main section, and their inclusion in the horizon is fairly certain.

Lijialaowu (70021):Anictops tabiepedisQiu, 1977,A.wanghudunensisZheng et al., 1999,Pappictidops orientalisChiu & Li, 1977,QianshanosaurushuangpuensisHou, 1974,Qianshanornis rapaxMayr et al., 2013

Zhangxinwu (71007):Anictops tabiepedisQiu, 1977

wanghudun Northeast:Paranictopsaff.P.maiuscula

Dingxiawu (70020):Huaiyangale chianshanensisXu, 1976,Huaiyangalesp.,Anictops tabiepedisQiu, 1977,Obtususdon hanhuaensisXu, 1977

Zhangjiawu East (71009):Huaiyangale chianshanensisXu, 1976,Diacronus anhuiensisXu, 1976,Anictops tabiepedisQiu, 1977,Zeuctherium nitelesTang & Yan, 1976,Decoredon elongetusXu, 1977,Anhuichelys siaoshihensisYeh, 1979

Zhangjiawu Southeast (71011):Anictops tabiepedisQiu, 1977

Zhangjiawu South (71008):Anictops tabiepedisQiu, 1977,MimotonaliiDashzeveg & Russell, 1988,Pappictidops orientalisChiu & Li, 1977

Zhangjiawu Southwest (71010):Paranictops maiusculaQiu, 1977,Heomyssp.

Shangxialou (71016):Diacronus wanghuensisXu, 1976,Anictops tabiepedisQiu, 1977,MimotonawanaLi, 1977, ?Altilambda tenuisChow & wang, 1978

Chenxiawu (71012):Anictops tabiepedisQiu, 1977,Harpyodus eurosChiu & Li, 1977

Zhangchong:Anhuichelys siaoshihensisYeh, 1979

Yangwu Southwest (71014): ?Paranictopssp.

Yangwu west (71019):Anictops tabiepedisQiu, 1977

Taowu (70022):Anictops tabiepedisQiu, 1977,Anictopsaff.A.tabiepedis,Paranictops majusculaQiu, 1977

Sanliantang (70023):Wania chowiwang, 1995,Bemalambdasp. cf.B.crassaChow et al., 1973

Zhongjialaowu:Archaeoryctes wangiMissiaen et al., 2013

(5) Localities in the upper part of the Upper Member of wanghudun Formation

Eight localities are included in this horizon. Four of them, Fujiashanzui, Lianhuatang Southeast, Lianhuatang, and Xudawu South, are close to the main section and can be referred to the horizon with certainty. However, the other four localities, Chenjiachuanmenkou, Mao’an, Jinshi, and wangjiazha, are less certain to be included in the horizon, because they are in some distance from the main section. They are referred to the horizon mainly based on the biostratigraphic data.

Fujiashanzui:Eosigale yujingensisHu, 1993,Mina huiLi et al., 2016,Anhuichelys tsienshanensisYeh, 1979

Lianhuatang Southeast:Simplodon qianshanensisHuang & Zheng, 2003

Lianhuatang:Anhuichelys tsienshanensisYeh, 1979

Xudawu South:Qipania yuiHu, 1993

Chenjiachuanmenkou:Altilambda yujingensiswang et al., 1992

Mao’an (71075):Altilambda pactusChow & wang, 1978

Jinshi:Anhuichelys tsienshanensisYeh, 1979

wangjiazha:Anhuichelys tsienshanensisYeh, 1979

(6) Localities in the Lower Member of Doumu Formation

Among the fossil localities listed below, the first five can be included in the horizon with certainty, since they are near the main section. The last one is tentatively included in the horizon, mainly based on the lithological features, because the only reported vertebrate fossil is a calcaneus of Glires that cannot be currently identi fi ed at lower taxonomic level (Zhang et al., 2016).

Xudawu:Anhuichelys tsienshanensisYeh, 1979

Hanhuawu South (71079):Hsiuannania tabiensisXu, 1976,Allictops inserrataQiu, 1977,Mimotona robustaLi, 1977,Obtususdon hanhuaensisXu, 1977,Agama sinensisHou, 1974,Anhuichelys tsienshanensisYeh, 1979

Hanxindongwu (71015):Allictops inserrataQiu, 1977

Hanhuawu west (71020):Anhuichelys tsienshanensisYeh, 1979

Hanjiashanbao:Anhuichelys tsienshanensisYeh, 1979

Huanghetang Reservoir: Glires gen. et sp. indet.

(7) Localities in the Upper Member of Doumu Formation

Among the six localities listed below, only Yanglaowu is not near the main section. The lithology of the deposits and fossil turtle together with the geographic location clearly show that it should be in this horizon.

Yangxiaowu (71017):Hsiuannaniasp.,Heomys orientalisLi, 1977,MimotonawanaLi, 1977,Hyracolestes ermineusMatthew & Granger, 1925,Wanolestes liiHuang & Zheng, 2002,Sinostylops promissusTang & Yan, 1976,Archaeolambda tabiensisHuang, 1977,Anhuisaurus huainanensisHou, 1974, Varaniformes gen. et sp. indet.,Anhuichelys tsienshanensisYeh, 1979,A.doumuensisTong et al., 2016

Chongliwu (71018):Tinosaurus doumuensisHou, 1974

Yangxinwu (71071):Anhuichelys doumuensisTong et al., 2016

Zhugongtang west:WanshuinaliiHou, 1994

Meiyuan:Anhuichelys doumuensisTong et al., 2016

Yanglaowu:Anhuichelys doumuensisTong et al., 2016

4 Fossil vertebrates

From the above mentioned localities, different kinds of fossil vertebrates have been found during the past half a century. Up to date, 52 species plus 9 unnamed ones of reptiles, birds, and mammals were reported from the Paleocene of the Qianshan Basin. A complete faunal list of fossil vertebrates reported from the Paleocene of the Qianshan Basin is provided in Appendix 1.

4.1 Reptilia

The reptilian fossils recovered from the Qianshan Paleocene represent three major groups, Testudines, Squamata, and Crocodilia.

4.1.1 Testudines

Fossil turtles are relatively common in the Qianshan Basin, and have been found in many localities (for details, see Tong et al., 2016). All the specimens were referred to a single genusAnhuichelysYeh, 1979. when Yeh (1979) fi rst reported the fossil turtles of the basin, he referredAnhuichelysto Emydidae, with two new species,A.siaoshihensisandA.tsienshanensis, and an unnamed species,Anhuichelyssp. After that, a number of additional specimens were collected by the colleagues of the Qianshan County Museum, but no further research has been done, except Chen (1983) described a new species ofAnhuichelys,A.xinzhouensis, from the Paleocene deposits of the Xinzhou Basin, Hubei Province.

Recently, Tong et al. (2016) comprehensively studied all the available specimens of Paleocene turtles from both the Qianshan and Xinzhou basins. In addition to referring somenew specimens toA.siaoshihensisandA.tsienshanensis, they synonymizedA.xinzhouensiswithA.tsienshanensis, and named a new species,A.doumuensis, using the specimen of Yeh’sAnhuichelyssp. as the holotype. Meanwhile, they described four specimens under an unnamed species,Anhuichelyssp. Based on these materials, Tong and her colleagues conducted a phylogenetic analysis. Their result suggests thatAnhuichelysis a member of the stem Testudinidae. “Anhuichelysis likely a land turtle and also the fi rst testudinoid to develop the hinge on the shell” (Tong et al., 2016).

According to the current stratigraphical information, specimens ofAnhuichelys siaoshihensiswere found from the Lower Member and the lower part of the Upper Member of the wanghudun Formation;A. tsienshanensisspecimens were collected from the upper part of the Upper Member of the wanghudun Formation through the Upper Member of the Doumu Formation;A.doumuensisis only present in the Upper Member of the Doumu Formation; andAnhuichelyssp. was from the upper part of the Upper Member of the wanghudun Formation and possibly the Lower Member of the Doumu Formation. The occurrence of fossil turtles in the Qianshan Basin shows clearly the biostratigraphical signi fi cance.A.siaoshihensisis a turtle member of the Shanghuan Asian Land Mammal Age (ALMA) that is Early Paleocene in age and can be correlated to both the Puercan and Torrejonian North American Land Mammal Ages (NALMA). All the other three species are the members of the Nongshanian ALMA that is Middle Paleocene in age and can be correlated to early-middle Tiffanian NALMA (see further discussion below).

4.1.2 Squamata

The fossil lizards from the Paleocene of Qianshan Basin were fi rst reported by Hou (1974). He named two new genera and four new species,Qianshanosaurus huangpuensis,Anhuisaurus huainanensis,Tinosaurus doumuensis, andAgamasinensis, and referredQ.huangpuensisto Iquanidae and the other three to Agamidae (Hou, 1974). Two years later, Hou (1976) described two new genera and species,AnqingosaurusbrevicephalusandChangjiangosaurus huananensis, and referred them to Chamaelenantidae and Changjiangosauridae respectively. The systematic position of these lizard taxa has been long debated (for details, refer to Dong et al., 2016). Dong et al. (2016) reexamined all the reported lizard specimens from the Paleocene of the Qianshan Basin and revised their taxonomic position. Under the current classi fi cation of Squamata, they referredAgama sinensis(nomen dubium),Qianshanosaurus huangpuensis, andTinosaurus doumuensisto Acrodonta, and consideredAnhuisaurus huainanensis,Anqingosaurusbrevicephalus, andChangjiangosaurus huananensisas Squamataincertae sedis(Dong et al., 2016). In addition, they recognized the fi rst varaniform from the Qianshan Paleocene that were represented by a nearly complete right dentary, a series of six articulated vertebrae, and a sacrum with the last presacral (Dong et al., 2016), which were originally identi fi ed asAnhuisaurus huainanensis(Hou, 1974).

According to the stratigraphical information,Anqingosaurus brevicephalusandChangjiangosaurus huananensiswere collected from the Lower Member of wanghudun Formation, andQianshanosaurus huangpuensiswas found in both the Lower Member and the lower part of the Upper Member of wanghudun Formation. These three taxa represent the squamate members of the Early Paleocene Shanghuan ALMA.Agama sinensiswas only reported from the Lower Member of the Doumu Formation (recorded as wanghudun Formation by mistake in the original report, i.e. Hou, 1974:199).Tinosaurus doumuensis,Anhuisaurus huainanensis, and Varaniformes gen. et sp. indet. were all from the Upper Member of the Doumu Formation. These four taxa are squamate representatives of the Middle Paleocene Nongshanian ALMA. Readers can refer to Dong et al. (2016) for detailed information about the lizard-bearing localities.

4.1.3 Crocodilia

The first crocodilian fossil from the Qianshan Paleocene deposits was found by the geological survey team at Dinghuawu, Huaining County in 1966 (RGSBGA, 1988b). It was not formally described until 1982 when Young (1982) named itEoalligatorhuiningensis. The species was originally referred to Alligatorinae (Young, 1982), which was later questioned (whiting and Hastings, 2015). Here we follow Young (1982) and listE.huiningensisas a member of Alligatorinae, before its taxonomic position is restudied.

Another crocodilian was reported by Zhang (1981). It was possibly collected from the Paleocene of the Qianshan Basin. Zhang (1981) named itWanosuchus atresuswithin its own family, wanosuchidae.

Eoalligatorhuiningensiswas from the Lower Member of the wanghudun Formation at Dinghuawu (Qiu et al., 1977), which is Early Paleocene Shanghuan in age (see discussion below). However, the locality and horizon ofWanosuchus atresusremains unknown.

4.2 Aves

Two fossil birds have been reported from the Qianshan Paleocene.Wanshuina liiwas represented by the shaft of a right humerus, the distal end of a left tibiotarsus, and the associated left tarsometatarsus lacking distal end, and was originally referred to Rallidae (Hou, 1994). It was later considered to have some similarities toWalbeckornisfrom the Paleocene of Germany (Mayr, 2009; Mayr et al., 2013). Since further examination is required to clarify its taxonomic position, we tentatively follow Hou (1994) to listW.liias a member of Rallidae. Another fossil bird,Qianshanornisrapax, was considered similar toStrigogypsand assigned to its own family Qianshanornithidae (Mayr et al., 2013).

Wanshuina liiwas collected from the Upper Member of the Doumu Formation at Zhugongtang west, which is considered to be the deposits of the Nongshanian ALMA. The specimens ofQianshanornisrapaxwere found from the lower part of the Upper Member of the wanghudun Formation at Lijialaowu (Mayr et al., 2013), which is considered to be the Shanghuan ALMA (see discussion below).

4.3 Mammalia

Fossil mammals are relatively common and highly diverse in the Paleocene deposits of the Qianshan Basin. Up to date, twenty eight localities have been reported to produce fossil mammals. These fossils form the Qianshan Paleocene mammal fauna that comprises 39 named species together with eight indeterminate ones.

4.3.1 Anagalida

Anagalida, an Asian endemic mammalian group, has the most diverse record among the Paleocene mammals reported in the Qianshan Basin. Three families, Anagalidae, Pseudictopidae and Astigalidae, have been found there.

Anagalidae Qianshan Paleocene anagalids were first reported by Xu (1976). He described seven species and two unnamed ones of six genera:Huaiyangale chianshanensis,Huaiyangalesp.,Hsiuannania tabiensis,Hsiuannaniasp.,Wanogalehodungensis,Chianshaniagianghuaiensis,Diacronus wanghuensis,D.anhuiensis, andAnaptogale wanghoensis. He assignedHuaiyangaleandHsiuannaniato Anagalidae, while tentatively referred the other four genera to the same family (Xu, 1976).

Hu (1993) reported two new genera and species,EosigalegujingensisandQipania yui, based on so far the best preserved anagalid material from the Qianshan Basin. He also discussed the phylogenetic relationships of Anagalidae. As a result of the phylogenetic analysis, he con fi rmed the attribution to Anagalidae ofHuaiyangale,Eosigale,Qipania, andHsiuannaniaand tentatively referredDiacronusandAnaptogaleto the family. In addition, he assignedChianshaniato Astigalidae and consideredWanogaleto be a member of family indet. (Hu, 1993).

Szalay and Li (1986) combinedDiacronusanhuiensisXu (1976) withDecoredon elongetusXu (1977) into a single species,Decoredonanhuiensis, and proposed it as “the oldest recognized member of euprimates, either an omomyid or a member of the common stock which gave rise to Adapidae and Omomyidae” (Szalay and Li, 1986:387). This assignment has received little support (Rose, 1994) and was considered to be questionable (Rose et al., 1994) or unlikely (Gingerich et al., 1991). Because of the conspecific assignment suspect of the holotypes (and only known specimens) of both taxa (Rose et al., 1994), it might better consider them as separate species and tentatively assignDiacronusanhuiensisto Anagalidae at present.

AnaptogaleandWanogalewere collected from the Lower Member of the wanghudun Formation, and bothHuaiyangaleandDiacronuswere discovered from the lower part of the Upper Member of the wanghudun Formation. According to the current information, these four genera are members of Early Paleocene Shanghuan ALMA. BothEosigaleandQipaniawere found from the upper part of the Upper Member of the wanghudun Formation, andHsiuannaniawas from the Doumu Formation. They are anagalid representatives of Middle Paleocene Nongshanian ALMA. Locality information of fossil anagalids in the Qianshan Basin can be found in Xu (1976) and Hu (1993).

Pseudictopidae Pseudictopids are also common in the Paleocene of the Qianshan Basin. Qiu (1977) made a relatively comprehensive study on pseudictopids on the basis of available materials by then. He described three new species of three new genera as well as one unnamed and one affinis species:Anictopstabiepedis,Anictopsaff.A.tabiepedis,Paranictopsmajuscule,Paranictopssp., andAllictopsinserrata. Two years later, Ding and Tong (1979) namedCartictopscaninabased on an anterior portion of left lower jaw (IVPP V 4307) that was referred toParanictopssp. by Qiu (1977) and a left m2 or m1 (IVPP V 4318) that was described as indeterminate genus and species by Chiu and Li (1977). Zheng et al. (1999) reported some new specimens from the Qianshan Paleocene. They named a new species,Anictops wanghudunensis, and referred the rest specimens toAnictopstabiepedisandParanictopsaff.P.majuscule, respectively.

CartictopsandParanictopswere collected from the Lower Member and the lower part of the Upper Member of wanghudun Formation, respectively, andAnictopswas found from both horizons. They are representatives of the Early Paleocene Shanghuan pseudictopids.Allictops, from the Lower Member of Doumu Formation, represents the only pseudictopid form of the Middle Paleocene Nongshanian ALMA in the Qianshan Basin.

Astigalidae Up to date, two species of Astigalidae have been reported from the Qianshan Paleocene.Astigalewanensiswas named by Zhang and Tong (1981) based on a right lower jaw found at Fanglaowu.Chianshaniagianghuaiensis, collected at wangdawu, was originally assigned to Anagalidae (Xu, 1976), but was later considered to be a member of Astigalidae (Hu, 1993). Both taxa were collected from the Lower Member of wanghudun Formation, and are of Early Paleocene Shanghuan ALMA.

4.3.2 Simplicidentata

Fossil simplicidentates from the Qianshan Basin were represented by some eurymylids. Li (1977) first reportedHeomys orientalisand clearly pointed out thatHeomysis a remote ancestor form of rodents, based on its similarities to primitive rodents. Such opinion received new evidence from the further examination on the materials ofHeomysand primitive rodents (Dawson et al., 1984; Li et al., 1987; Li and Ting, 1985, 1993; Li and Chow, 1994) and was supported by studies on related forms (Meng and wyss, 1994, 2001; Meng et al., 1994b, 2003). Some researchers even consideredHeomysas primitive rodents (Flynn, 1994; McKenna and Bell, 1997), but recent phylogenetic analysis did not suggest thatHeomyshas a closer relationship with typical rodents than the other eurymylids do (Meng and wyss, 2001; Meng et al., 2003; Meng, 2004). Currently, it might be better to assignedHeomysas a member of Eurymylidae. In addition, Li (1977) identi fi ed the poorly preserved anterior portion of a skull asHeomyssp.

Heomys orientaliswas collected from the Upper Member of Doumu Formation at Yangxiaowu (Li, 1977). It is a representative of the Middle Paleocene Nongshanian ALMA.Heomyssp. was found from the lower part of the Upper Member of wanghudun Formationat Zhangjiawu Southwest. It represents a eurymylid record in the Early Paleocene Shanghuan ALMA.

4.3.3 Mimotonida

Mimotonida was proposed by Li et al. (1987) to include the basal Glires that have two pairs of incisors in both upper and lower dentitions. Although some recent phylogenetic analyses showed that Mimotonida is a paraphyletic group (Meng and wyss, 2001; Meng, 2004; Asher et al., 2005), it may be convenient to keep using Mimotonida until a better phylogenetic relationship of the basal Glires becomes available (Li et al., 2016). Two genera of mimotonidans,MimotonaandMina, have been reported from the Qianshan Basin and represent two different families, Mimotonidae and Mimolagidae (Li, 1977; Li et al., 2016).

Mimotonidae Li (1977) proposed Mimotonidae to include only the type genus,Mimotona, but several genera were referred to the family later (for details, see Li et al., 2016). with the new data being accumulated, it becomes more likely that Mimotonidae is a monophyletic group only containingMimotona(Li et al., 2016).

when he first reported the fossil mimotonids from the Qianshan Paleocene, Li (1977) described two named and one unnamed species ofMimotona,M.wana,M.robusta, andMimotonasp. He also noticed the difference ofMimotonasp. from the other two species and mentioned that it might represent a new species, but it was not formally named until Dashzeveg and Russell (1988) named itM.lii.

The holotype and referred two left lower molars ofMimotona wanawere found from the Upper Member of Doumu Formation at Yangxiaowu (Li, 1977). The type and only specimen ofM.robustawas from the Lower Member of Doumu Formation at Hanhuawu South. Biostratigraphic correlation indicates both are in the Nongshanian ALMA, Middle Paleocene in age. The type and only specimen ofM.liiwas collected from the lower part of Upper Member of wanghudun Formation at Zhangjiawu South. Its stratigraphic level is in the Early Paleocene Shanghuan ALMA. A right premaxilla with alveoli for I2-3 (IVPP V 4326) from the lower part of the Upper Member of wanghudun Formation at Shangxialou was referred toM.wanaas paratype (Li, 1977), but the recent discovery ofMina hui(Li et al., 2016) may raise the doubt about its assignment toMimotona. The occurrence ofM.wanain Early Paleocene thus requires further evidence.

Mimolagidae In the Qianshan Basin, Mimolagidae was represented by a recently reported basal duplicidentateMina hui. The type specimens, found from the upper part of the Upper Member of wanghudun Formation at Fujiashanzui, include a partial right rostrum with dI2 and I3 and a fragmentary left maxilla with M1, M2 and alveoli of P2-4 (IVPP V 7509) (Li et al., 2016). It is a member of Qianshan mammals of the Middle Paleocene Nongshanian ALMA.

4.3.4 Mesonychia

Mesonychia was represented by a single species of Mesonychidae in the Qianshan Basin. Yan and Tang (1976) reported the only mesonychid of the Qianshan Paleocene and named itLestes conexus. The genus name was later replaced withYantanglestesbecauseLesteswas preoccupied by a zygopteran insect (Ideker and Yan, 1980).Yantanglestes conexuswas collected from the Lower Member of wanghudun Formation at Chidoukan (originally called 150 meters northwest of Jiangjiawu) (Yan and Tang, 1976; Qiu et al., 1977). The fossil-bearing level at this locality can be assigned to the Early Paleocene Shanghuan ALMA.

4.3.5 Pantodonta

Pantodonta is one of the most common mammalian groups in the Chinese Paleocene. Four families, Bemalambdidae, Harpyodidae, Pantolambdodontidae and Pastoralodontidae, have been recorded in the Qianshan Basin. All of them are Asian endemic forms.

Bemalambdidae Compared to the fossil bemalambdids from the contemporaneous Nanxiong and Chijiang basins in southern China, specimens of Bemalambdidae found in the Qianshan Basin are much less and poorly preserved. The reported Qianshan Paleocene bemalambdids,Bemalambdasp. and Bemalambdidae gen. et sp. indet., were represented by fragmentary material and were not able to be further identi fi ed (Huang, 1978). Both taxa were found from the Lower Member of wanghudun Formation. The specimens referred toBemalambdasp. were collected at Chidoukan and wangdawu, which are stratigraphically higher than Haixingdi where Bemalambdidae gen. et sp. indet. was discovered. The strata producing both taxa can be assigned to the Early Paleocene Shanghuan ALMA.

Harpyodidae Chiu and Li (1977) namedHarpyodus eurosbased on a fragmentary left maxilla with M1-3 and referred it to an indeterminate family of Deltatheridia Van Valen, 1966. Two years later, wang (1979) proposed Harpyodidae for the genus and suggested its pantodont af fi nities, when she described a new species ofHarpyodusfrom the upper part of the Lannikeng Member of Chijiang Formation in the Chijiang Basin, Jiangxi, southern China. The assignment ofHarpyodusto Pantodonta has been widely accepted (e.g. de Muizon and Marshall, 1992; McKenna and Bell, 1997; wang et al., 1998; de Muizon et al., 2015).

Harpyodus euroswas found from the lower part of the Upper Member of wanghudun Formation at Chenxiawu (Chiu and Li, 1977), which is within the Early Paleocene Shanghuan ALMA.

Pantolambdodontidae The only pantolambdodontid from the Qianshan Basin is represented byArchaeolambda tabiensis. It was reported by Huang (1977) based on a nearly completed skeleton that is so far the only known skeleton of the genus and family. Huang (1977) referredA.tabiensisto Archaeolambdidae, but noted the possibility of synomizing Archaeolambdidae with Pantolambdodontidae. Chow and Qi (1978) pointed out thatPantolambdodonandArchaeolambdaobviously belong to one family, and all the taxa previously referred to Archaeolambdidae should be reassigned to Pantolambdodontidae.Such opinion was accepted by the latter researchers (e.g. Huang, 1995; Huang and Chen, 1997; Huang and Zheng, 1997, 2003b; McKenna and Bell, 1997; Tong and wang, 2006). The specimen ofA.tabiensiswas collected from the Upper Member of Doumu Formation at Yangxiaowu (Huang, 1977). It is considered to be the Middle Paleocene Nongshanian ALMA.

Pastoralodontidae Pastoralodontids are the most common pantodonts in the Qianshan Paleocene. They are represented by three species of one genus,Altilambda pactus,A.tenuis, andA.yujingensis(Chow and wang, 1978; wang et al., 1992). The specimens ofA.tenuis(two fragmentary lower jaws) are not well-preserved, and their assignment toAltilambdaremains somehow questionable. All the three species were found from the Upper Member of wanghudun Formation. ?A.tenuiswas collected from the lower part of the Upper Member of wanghudun Formation at Shangxialou (Chow and wang, 1978). It is an Early Paleocene Shanghuan mammal. The other two species, discovered respectively at Mao’an and Chenjiachuanmenkou, are morphologically more derived than ?A.tenuis. They may be stratigraphically higher than ?A.tenuisand are possibly of the Middle Paleocene Nongshanian ALMA.

4.3.6 Tillodontia

Three mammalian genera and species, reported from the Qianshan Basin, can be referred to Tillodontia (wang and Jin, 2004).Plethorodon chienshanensiswas described by Huang and Zheng (1987) based on a partial skull with complete cheek tooth dentition of both sides.P.chienshanensiswas tentatively assigned to the order Pantodonta under its own family Plethorodontidae in the original paper (Huang and Zheng, 1987). Later, de Muizon and Marshall (1992) considered it to be a tillodont instead of a pantodont. This opinion was followed by McKenna and Bell (1997) and wang et al. (1998), but disputed by Ting (1998) and Tong et al. ( 2003). However, after a detailed comparison and a phylogenetic analysis, wang and Jin (2004) consideredP.chienshanensisto be a tillodont.

Huang and Zheng (2003a) named another tillodont,Simplodon qianshanensis, on the basis of a right maxilla with P3-M3, and questionably referred it to Esthonychidae.Simplodonhas some similarities to tillodonts, but no sufficient evidence supports its assignment to Esthonychidae. It might be reasonable to referSimplodonto indeterminate family of Tillodontia.

wang and Jin (2004) described a left lower jaw with c-m3 from the Paleocene of the Qianshan Basin and named itBenaius qianshuiensis. The species was classi fi ed as a tillodont but not assigned to a special family.

BothPlethorodon chienshanensisandBenaius qianshuiensiswere collected from the Lower Member of wanghudun Formation at wangdawu and Fanglaowu respectively (Huang and Zheng, 1987; wang and Jin, 2004). The wangdawu locality is stratigraphically higher than the Fanglaowu laocality, but they both are in the Early Paleocene Shanghuan ALMA.Simplodon qianshanensiswas found from the upper part of the Upper Member of wanghudunFormation southeast to Lianhuatang (Huang and Zheng, 2003a). It is a member of the Middle Paleocene Nongshanian mammals.

4.3.7 Arctostylopida

Arctostylopida contains only one family Arctostylopidae (Cifelli and Schaff, 1998). Fossil arctostylopids were originally thought to have close relationships to the South American notoungulates (Matthew, 1915) and had been referred to the family Arctostylopidae of the order Notoungulata for many years (Schlosser, 1923; Matthew and Granger, 1925; Matthew et al., 1929; Patterson, 1934; Tang and Yan, 1976; Chow and Qi, 1978; Zheng, 1979; Rose, 1981; Gingerich, 1985; Zheng and Huang, 1986; Nessov, 1987; Huang and Chen, 1997). Cifelli et al. (1989) considered that Arctostylopidae was not related to Notoungulata and proposed a new order, Arctostylopida, for the family. This opinion has been widely accepted (e.g. McKenna and Bell, 1997; Huang and Zheng, 1997, 2003b; Huang et al., 2001; Kondrashov and Lucas, 2004a; Zack, 2004; Tong and wang, 2006; Missiaen and Smith, 2008; Secord, 2008; wang et al., 2008; Missiaen et al., 2012).

Only one arctostylopid species,Sinostylopspromissus, has been reported from the Upper Member of Doumu Formation at Yangxiaowu, Qianshan (Tang and Yan, 1976). It is of the Middle Paleocene Nongshanian ALMA.

4.3.8 Carnivora

The only species of Carnivora,Pappictidops orientalis, was described by Chiu and Li (1977). The specimens include a right maxilla with canine and P2-M2 (holotype), and the horizontal ramus of a juvenile left lower jaw (referred specimen).Pappictidopswas originally referred to the Viverravinae of Miacidae (Chiu and Li, 1977). It was considered to be most similar to North American PaleoceneIctidopappus(Chiu and Li, 1977; wang, 1978). Flynn and Galiano (1982) resurrected the family Viverravidae wortman & Matthew, 1899 and it has been widely used (e.g. Eaton, 1985; Gingerich and winkler, 1985; Gingerich, 1989; Gunnell et al., 1992; Polly, 1997; Gunnell, 1998; Eberle and McKenna, 2002; Meehan and wilson, 2002; Huang and Zheng, 2005; Gingerich and Smith, 2006; Tong and wang, 2006; Beard and Dawson, 2009; Friscia and Rassmussen, 2010; Scott et al., 2013). It is reliable to assignPappictidopstogether withIctidopappusto Viverravidae. A couple of papers mentioned that the Asian viverravidPappictidopswas recorded in Late Paleocene and earliest Eocene (Gingerich and winkler, 1985; Polly, 1997), but this genus has only been found in the Paleocene of both Qianshan and Nanxiong basins (Chiu and Li, 1977; wang, 1978). The specimens of QianshanPappictidopswere discovered from the lower part of the Upper Member of wanghudun Formation at Zhangjiawu and Lijialaowu respectively (Chiu and Li, 1977), which is of the Early Paleocene Shanghuan ALMA.

4.3.9 Cimolesta

Chiu and Li (1977) described a fragmentary right lower jaw with p3-m1 and identi fi ed asHyracolestes ermineusunder Deltatheridia.H.ermineuswas fi rst named from the Paleocene of Mongolia and questionably referred to Creodonta by Matthew and Granger (1925). Van Valen (1966) placed it in Erinaceoidea of Insectivora, while Szalay and McKenna (1971) referred it to Deltatheridiidae of Insectivora. McKenna et al. (1984) movedH.ermineusto Micropternodontidae of Soricomorpha. Currently,Hyracolestesis included in Sarcodontidae of the mirorder Cimolesta (Lopatin and Kondrashov, 2004; Missiaen and Smith, 2008).

The species was found from the Upper Member of Doumu Formation at Yangxiaowu, which is in the Middle Paleocene Nongshanian ALMA.

4.3.10 Didymoconida

The taxonomic position of Didymoconidae varies greatly. It has been placed in different orders, e.g. Insectivora (Meng et al., 1994a; wang et al., 2001), Deltatheridia (Mellett and Szalay, 1968; Tang and Yan, 1976), Leptictida, Mesonychia (Lopatin, 1997), Condylarthra (Gingerich, 1981), Didymoconida (Lopatin, 2001; Morlo and Nagel, 2007), and Order indet. (Li et al., 1979; Meng, 1990). Here, we tentatively use Didymoconida as higher-level taxon.

Tang and Yan (1976) reportedZeuctherium nitelesas a didymoconid on the basis of a partial skull. Missiaen et al. (2013) described another didymoconidArchaeoryctes wangibased on a pair of lower jaws. Huang and Zheng (2002) namedWanolestes liibased on a pair of incomplete lower jaws and referredWanolestesto ?Micropternodontidae of Soricomorpha. Lopatin (2006) considered thatWanolestesis similar toArchaeoryctesand placedWanolestesin Didymoconidae.

ZeuctheriumandArchaeoryctes wangiwere found from the lower part of the Upper Member of wanghudun Formation at Zhangjiawu East and Zhongjialaowu, respectively. Both taxa are of the Early Paleocene Shanghuan ALMA. The specimens ofWanolestes liiwere found from the Upper Member of Doumu Formation at Yangxiaowu, which is in the Middle Paleocene Nongshanian ALMA.

4.3.11 Order indet.

Several mammal species, named on the basis of Qianshan Paleocene materials, are not able to be assigned to a taxonomically higher group with certainty. They are listed here under indeterminate order.

Anchilestes impolituswas named by Chiu and Li (1977) based on incomplete left upper and lower jaws with P3-M2 and p4-m3 of the same individual. It was originally referred to Zalambdalestidae within Anagalida (Chiu and Li, 1977). Ting and Zheng (1989) reevaluated its af fi nity and assigned it to the order Tillodontia. However, the morphology of both the upper and lower dentitions ofAnchilestesis distinct from those of tillodonts and zalambdalestids, providing little evidence to support a special relationship to either tillodonts or zalambdalestids(wang et al., 1998; wang and Jin, 2004).Anchilestesimpolituswas found from the Lower Member of wanghudun Formation at wangdawu, which is in the Early Paleocene Shanghuan ALMA.

Decoredon elongetuswas reported on the basis of a left and a right lower jaws both with p4-m3, and originally referred to Hyopsodontidae within Condylarthra (Xu, 1977). Szalay and Li (1986) combinedDecoredonelongetuswithDiacronusanhuiensisinto a single species,Decoredonanhuiensis. They consideredDecoredonanhuiensisas a member of ?Omomyidae within Euprimates and named a new subfamily, Decoredontinae. This assignment has received little support and was considered to be questionable (Rose, 1994; Rose et al., 1994) or unlikely (Gingerich et al., 1991). Kondrashov and Lucas (2004b) considered thatDecoredonanhuiensisdid not exhibit features typical of either archaic ungulates or omomyid primates, but accepted the synonymy ofDiacronus anhuiensisandDecoredon elongetus. As noted before, due to the conspecific assignment suspect of the holotypes (and only known specimens) of both taxa (Rose et al., 1994), it might better consider them as separate species and tentatively leaveDecoredonelongetusas Order and Family incertae sedis at present. The specimens ofDecoredon elongetuswere collected from the lower part of the Upper Member of wanghudun Formation at Zhangjiawu East (Xu, 1977), which suggest its occurrence in the Early Paleocene Shanghuan ALMA.

Obtususdon hanhuaensiswas described by Xu (1977) based on a fragmentary right lower jaw with p4-m3 (holotype) and a fragmentary left lower jaw with p4-m3. Its taxonomic position was considered indeterminate and requires further study with the finding of some better specimens. The holotype was collected from the Lower Member of Doumu Formation at Hanhuawu South, which is in the Middle Paleocene Nongshanian ALMA. The referred specimen was found from the lower part of the Upper Member of wanghudun Formation at Dingxiawu, which is of the Early Paleocene Shanghuan ALMA.

Waniachowiwas based on two fragments of a left maxilla and a pair of lower jaws of the same individual (wang, 1995). It was originally referred to the family Zhelestidae in the order Mixotheridia, but Nessov et al. (1998) argued thatWaniachowi“is not a zhelestid but may have anagalidan af fi nities.” Because determination of its phylogenetic position requires further study,Waniachowiis temporarily classi fi ed as Order and Family indeterminate (wang et al., 1998). The specimens ofWania chowiwere collected from the lower part of the Upper Member of wanghudun Formation, which is of the Early Paleocene Shanghuan ALMA.

5 Correlation and age determination

Of all the Chinese Paleocene basins, the Nanxiong, Qianshan, Chijiang, and Erlian (Nei Mongol) basins have yielded particularly important records of fossil mammals. The first three basins mainly produce fossil mammals spanning the Early-Middle Paleocene, whilethe Erlian Basin documents relatively later Paleocene faunas. The records from these basins were used as a baseline in correlating the Chinese mammal-bearing Paleocene. On the basis of the mammalian fossil record then available, previous researchers proposed correlations of Paleocene strata within China. They considered that the Shanghu, Shizikou, and wanghudun formations were correlatives and correlated the Nongshan Formation with the Chijiang and Doumu formations (South China “Redbeds” Research Group, 1977; Zheng and Qiu, 1979; Li and Ting, 1983; Ting, 1998; Ting et al., 2011). After careful review of the occurrence of fossil mammals in the Nanxiong, Qianshan, and Chijiang basins, wang et al. (1998) tentatively correlated the boundary between the Shanghu and Nongshan formations (Nanxiong Basin) with that between the Shizikou and Chijiang formations (Chijiang Basin), and within the Upper Member of the wanghudun Formation (Qianshan Basin). The mammalian faunas from strata below this boundary are dominated byBemalambda, while faunas from strata above the boundary are characterized by the co-occurrence ofArchaeolambdaandAltilambda, withoutBemalambda(Fig. 2). Such a correlation fi rst appeared in wang’s (1993) Ph.D. dissertation and was in accordance with Tong et al.’s (1995) opinion.

Fig. 2 Correlation of the Paleocene in the Qianshan Basin with that in the Nanxiong and Chijiang basins, and with Geological Time Scale and NALMAs Polarity Chrons and NALMAs are modi fi ed from Vandenberghe et al. (2012)

Like in other Chinese Paleocene basins, great endemism of mammalian fauna hampered the intercontinental biostratigraphic correlation of the Qianshan Paleocene. No radiometric dates and failed attempt of paleomagnetic study further obstruct to correlate the Paleocene in the Qianshan Basin directly to the Global Geologic Timescale. The age determination of the Qianshan Paleocene mammalian fauna and fossil-bearing strata relies on the biostratigraphic correlation with other Paleocene basins, where the Paleocene could be correlated to those of other continents or the Timescale by certain means.

Early biostratigraphic studies considered mammalian faunas known from the Shanghu, Shizikou, and wanghudun formations and their correlatives to represent the Early-Middle Paleocene, while those from the Nongshan, Chijiang, Doumu, as well as Nomogen (Erlian Basin) formations and their correlatives were considered as Late Paleocene (South China“Red Beds” Research Group, 1977; Zheng and Qiu, 1979; Chow and Zheng, 1980; Li and Ting, 1983; Russell and Zhai, 1987). Li and Ting (1983) proposed two provincial mammal ages, the Shanghuan and the Nongshanian, to represent the Early-Middle and Late Paleocene respectively in correlation with Europe and North America. They tentatively correlated the Shanghuan with the North American Puercan and Torrejonian and the Nongshanian (including present Gashatan) with the North American Tiffanian in their correlation chart. Sloan (1987) followed the use of two mammal ages, but favored Gashatan over Nongshanian as a stage (age) name for the Asian Late Paleocene on the basis of priority of the former. He correlated the Shanghuan with the Torrejonian and part of the Tiffanian (To1-Ti4), and considered the Gashatan (=Nongshanian of Li and Ting, 1983) to be the late Tiffanian-Clarkforkian (Ti5-Cf3) equivalent. Tong et al. (1995) continued to use the Shanghuan and Nongshanian (the latter including some Gashatan correlatives) as Early and Late Paleocene provincial mammal ages of China. They correlated the Shanghuan with North American Puercan and early-middle Torrejonian, and the Nongshanian with the late Torrejonian through Clarkforkian in their correlation chart. In the same year, Lucas and williamson (1995) proposed a correlation of the Shanghuan with the North American Puercan, based on their comparison of the evolutionary stages of certain mammal taxa, including Mesonychidae, Carnivora, Tillodontia, and Pantodonta, but wang et al. (1998) disagreed with their opinion. Both wang et al. (1998) and Ting (1998) used three ages to represent Chinese Paleocene: the Shanghuan, the Nongshanian and the Gashatan, but their correlation with North American Land Mammal Ages were slightly different. Ting (1998) correlated the Shanghuan, Nongshanian and Gashatan with Torrejonian, Tiffanian and Clarkforkian, respectively, while wang et al. (1998) considered the three Chinese mammal ages to be respectively correlative with Puercan through middle Torrejonian (Pu1-To2), late Torrejonian through middle Tiffanian (To3-Ti4) and late Tiffanian through Clarkforkian (Ti5-Cf3).

Recent paleomagnetic results from the Nanxiong Basin indicate that the boundary between the Shanghu Formation and the underlying Pingling Formation lies within the upper half of Chron C29R, consistent with all the other precisely constrained K/Pg boundaries in the world (Clyde et al., 2010). Paleomagnetic results from both the Chijiang and Nanxiong basins clearly show that the Shanghuan is Early Paleocene in age (Danian) and corresponds to North American Puercan and Torrejonian. The placement of the Shanghuan/Nongshanian boundary near the top of Chron C27N implies that it is synchronous with the Torrejonian/ Tiffanian boundary (Clyde et al., 2008; 2010). In combination with those from the Erlian Basin (Sun et al., 2009), the paleomagnetic results indicate that the Nongshanian/Gashatan boundary lies somewhere between the upper part of Chron C26R and Chron C26N, corresponding to theupper part of the Tiffanian. Therefore, the Shanghuan and the Nongshanian can be probably correlated to the Early Paleocene Danian and the Middle Paleocene Selandian of the Global Geologic Time Scale (Vandenberghe et al., 2012). Such a correlation shows that both the wanghudun and Doumu formations and fossil vertebrates therefrom are the Early and Middle Paleocene in age.

6 Concluding remarks

The Mesozoic and Cenozoic redbeds in the Qianshan Basin consist of a set of monocline clastic rocks, and are subdivided into the Late Cretaceous Gaohebu Formation, the Paleocene wanghudun and Doumu formations. The wanghudun Formation is further subdivided into the Lower, Middle, and Upper members, while the Doumu Formation falls into the Lower and Upper members.

Continuous investigations in the Qianshan Basin resulted in discovery of a lot of vertebrate specimens. Sixty one species (including 9 unnamed ones) in 45 genera of vertebrates, representing reptiles, birds and mammals, have been reported from the Paleocene of the Qianshan Basin. Among them, mammals are most diverse and have been classi fi ed into 46 species (7 unnamed) of 33 genera, representing 16 families in 10 orders. According to the stratigraphic distribution of fossil vertebrates, 7 fossiliferous horizons can be recognized in the Qianshan Paleocene: 1) The basal part of the Lower Member of wanghudun Formation; 2) the middle part of the Lower Member of wanghudun Formation; 3) the upper part of the Lower Member of wanghudun Formation; 4) the lower part of the Upper Member of wanghudun Formation; 5) the upper part of the Upper Member of wanghudun Formation; 6) the Lower Member of Doumu Formation; and 7) the Upper Member of Doumu Formation.

Based on the evidence of fossil mammals, the strata from the Lower Member through the lower part of the Upper Member of wanghudun Formation could be roughly correlated to the Shanghu Formation of the Nanxiong Basin and the Shizikou Formation of the Chijiang Basin, corresponding to the Shanghuan ALMA. Both the upper part of the Upper Member of wanghudun Formation and the Doumu Formation could be correlated to the Nongshan Formation of the Nanxiong Basin and the Chijiang Formation of the Chijiang Basin, corresponding to the Nongshanian ALMA. Paleomagnetic results from both the Chijiang and Nanxiong basins suggest that the Shanghuan is roughly correlative to the Puercan and Torrejonian NALMA, while the Nongshanian correlative to the early to middle Tiffanian (Ti1-4a). The Shanghuan and the Nongshanian can be probably correlated to the Early Paleocene Danian and the Middle Paleocene Selandian of the Global Geologic Time Scale.

Acknowledgments we are grateful to Yu Ben’ai, Chen Limin, Li Tao, Yu Shuhua, Xiong Yuansheng and Xu Yiping of the Qianshan County Museum, wang Zongwu, Xu Lizhi, Deng Guolai and Zhou Min of the Bureau of Cultural Relics of Qianshan County, Yu Guosheng andCheng Xiaoqing of the Tianzhushan Global Geopark, and Xie Shuhua, Zhou Xiaoyuan, Zhou wei, Bai Bin, Gao wei, Li Shijie, Li Qi and wang Yongxing of IVPP for their assistance in the field. This work was supported by the Major Basic Research Projects of MST of China (No. 2012CB821900), the National Natural Science Foundation of China (Nos. 41572013, 41572021) and the Conservation Program of the Geological Heritage Sites of the Ministry of Finance and the Ministry of Land and Resources, People’s Republic of China.

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Appendix 1 Faunal list of Paleocene vertebrates in the Qianshan Basin

In the bracket behind the taxa, 1.1 refers to the Lower Member of the wanghudun Formation, 1.3a refers to the lower part of the Upper Member of the wanghudun Formation, 1.3b refers to the upper part of the Upper Member of the wanghudun Formation, 2.1 refers to the Lower Member of Doumu Formation, and 2.2 refers to the Upper Member of the Doumu Formation.

安徽潛山盆地古新世地層和脊椎動物概述

王元青1李傳夔1李 茜1李丁生2

(1中國科學院古脊椎動物與古人類研究所，中國科學院脊椎動物演化與人類起源重點實驗室 北京 100044)
(2 潛山縣博物館 安徽潛山 246300)

潛山盆地中、新生代紅層由一套單斜的碎屑巖組成，劃分為上白堊統(tǒng)高河埠組、古新統(tǒng)望虎墩組(分為上、中、下三段)和痘姆組(分上、下兩段)。1970年以來，在潛山盆地的持續(xù)調查發(fā)現(xiàn)了大量脊椎動物化石。迄今為止，潛山盆地古新統(tǒng)共報道了45屬61種(含9個未命名的種)脊椎動物，包括爬行類、鳥類和哺乳類。其中哺乳動物最為豐富，共有33屬46種(含7個未命名種), 分屬10個目16個科。根據(jù)化石產出的層位，可以在潛山古新統(tǒng)中識別出7個化石層位?；诓溉閯游锷锏貙訉W證據(jù)，望虎墩組下段至上段下部可以大致與廣東南雄盆地上湖組和江西池江盆地獅子口組對比，對應于亞洲陸相哺乳動物分期的上湖期；望虎墩組上段上部和痘姆組可以與南雄盆地濃山組以及池江盆地的池江組對比，與濃山期相對應。綜合我國幾個古新世盆地的古地磁研究結果顯示，上湖期可以大致與北美陸相哺乳動物分期的Puercan和Torrejonian對比，濃山期則與Tiffanian早中期(Ti1-Ti4a)相當。上湖期和濃山期還可以進一步與國際地質年表中的丹尼期(Danian)和塞蘭特期(Selandian)對比。因此，潛山盆地發(fā)現(xiàn)的脊椎動物化石的時代屬于早、中古新世。

安徽潛山，古新世，脊椎動物，地層，對比

Q915.873, P534.612

A

1000-3118(2016)02-0089-32

2016-03-10

wang Y Q, Li C K, Li Q et al., 2016. A synopsis of Paleocene stratigraphy and vertebrate paleontology in the Qianshan Basin, Anhui, China. Vertebrata PalAsiatica, 54(2): 89-120

國家重點基礎研究發(fā)展計劃項目(編號: 2012CB821900)、國家自然科學基金(批準號: 41572013, 41572021)和財政部、國土資源部地質遺跡保護項目資助。