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Stratigraphic subdivision and correlation of theCarboniferous System in South ChinaYang Shena & Xun-Lian Wanga

a School of Earth Sciences and Resources, China University of Geosciences (Beijing), Beijing,ChinaPublished online: 12 Feb 2015.

To cite this article: Yang Shen & Xun-Lian Wang (2015): Stratigraphic subdivision and correlation of the Carboniferous Systemin South China, International Geology Review, DOI: 10.1080/00206814.2015.1008591

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REVIEW ARTICLE

Stratigraphic subdivision and correlation of the Carboniferous System in South China

Yang Shen* and Xun-Lian Wang

School of Earth Sciences and Resources, China University of Geosciences (Beijing), Beijing, China

(Received 14 October 2014; accepted 13 January 2015)

The Carboniferous System of South China is famous for its well-developed rock sequence, variety of depositional types,and abundant fossils. Three established Global Boundary Stratotype Section and Point (GSSP) markers have been identifiedin several sections in South China. Of these sections, the Pengchong section is the GSSP for the base of the Visean Stage,whereas the Dapoushang and Naqing (Nashui) sections are excellent reference sections for the bases of the Tournaisian andBashkirian stages, respectively. Other sections have good potential for the four unestablished GSSPs and the Devonian–Carboniferous boundary in South China. The Naqing (Nashui) section is a candidate for the GSSPs of four stages: theSerpukhovian, Moscovian, Kasimovian, and Gzhelian stages. The regional stages of China include the Tangbagouan,Jiusian, Shangsian, Dewuan, Luosuan, Huashibanian, Dalaun, and Xiaodushanian. The history, definitions, referencesections, sedimentary characteristics, biostratigraphy, and correlations of these Chinese regional stages are summarized. ACarboniferous stratigraphic chart of South China is provided, showing the correlation of global chronostratigraphic andbiostratigraphic units with those in South China and the lithostratigraphic units of various areas in South China. The chart ispresented as a new practical framework for the stratigraphic subdivision and correlation of the Carboniferous System inSouth China.

Keywords: Carboniferous; Chinese regional stage; GSSP; stratigraphic chart; South China

1. Introduction

The Carboniferous period experienced critical transitionsin Earth history, but it is challenging to precisely establishthe timing of events. This is because Gondwana super-glaciation and the consequent drastic climatic changes,sea-level fluctuations, and significant biogeographic differ-entiation make it difficult to establish a global timescalebased on marine biostratigraphy and correlations of regio-nal strata. Although the Carboniferous was one of the firstgeological periods to be defined, it is one of the mostcomplicated and confusing in terms of stratigraphic clas-sification and correlation (Davydov et al. 2012). To date,only three Global Boundary Stratotype Section and Points(GSSPs) – the bases of the Tournaisian, Visean, andBashkirian stages – have been officially ratified for theCarboniferous System.

South China was located at a subequatorial–equatorialposition near the eastern border of the Palaeo-TethysOcean during Carboniferous time (Scotese 2002; Wanget al. 2013; Figure 1). The region is well known for itscomplete marine Carboniferous sequence and abundantfossils. All three established GSSPs markers are identifiedin South China. The base of the Visean Stage is fixed witha GSSP in the Pengchong section, South China (Devuystet al. 2003; Hou et al. 2013). In addition, South China haspotential for defining the stages that are currentlywithout GSSPs, including the Serpukhovian, Moscovian,

Kasimovian, and Gzhelian. Thus, South China will playan important role in improving our understanding of theglobal Carboniferous System.

The main purpose of this paper is to present the strati-graphic subdivision and correlation of the Carboniferousin South China. First, the research status of theCarboniferous GSSPs and their recognition in SouthChina are introduced. Second, the regional chronostrati-graphic units and a stratigraphic chart of South China arepresented. It is hoped that this paper will provide a betterunderstanding of the Carboniferous System in SouthChina.

2. Carboniferous GSSPs and their recognition inSouth China

The primary objective of the International Commission onStratigraphy (ICS) is to define precisely the global units(systems, series, and stages) of the InternationalChronostratigraphic Chart. All the efforts of theSubcommission on Carboniferous Stratigraphy (SCCS)are now focused on selecting events and GSSPs for stageboundaries (Richards 2013).

The Carboniferous System has been subdivided intotwo subsystems, the Mississippian and the Pennsylvanian,and contains seven global stages, the Tournaisian, Visean,Serpukhovian, Bashkirian, Moscovian, Kasimovian, and

*Corresponding author. Email: shenybj@126.com

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Gzhelian, in ascending order (Figure 2). To date, only theGSSPs for the bases of the Tournaisian, Visean, andBashkirian stages have been approved by the SCCS andICS (Paproth et al. 1991; Lane et al. 1999; Devuyst et al.2003), whereas the bases of the Serpukhovian, Moscovian,Kasimovian, and Gzhelian stages are not defined byGSSPs, and some markers for the definitions of theirboundaries have not yet been selected. In addition, thereare serious problems with the Devonian–Carboniferous(D–C) boundary GSSP (Ji et al. 1989; Kaiser 2009),which requires further research.

2.1. Tournaisian Stage

2.1.1. GSSP for the base of the Tournaisian Stage

The GSSP for the base of the Tournaisian Stage,Mississippian Subsystem, and Carboniferous System hasbeen defined at the base of bed 89 in the La Serre section,Montagne Noire, southern France (Paproth et al. 1991).The boundary is defined by the first appearance datum(FAD) of the conodont Siphonodella sulcata, within theSiphonodella praesulcata–S. sulcata evolutionary lineage(Paproth et al. 1991). At present, the boundary definitionneeds restudy.

Figure 1. (a) Global palaeogeographical reconstruction for the early Carboniferous (after Scotese 2002); (b) location of South Chinawithin China; (c) Mississippian palaeogeography of South China (after Feng et al. 1998); (d) Pennsylvanian palaeogeography of SouthChina (after Feng et al. 1998); (e) locations of the reference sections in South China: 1, Dapoushang section; 2, Pengchong section; 3,Naqing section; 4, Qilinzhai section; 5, Jiusi section; 6, Liuzhai section; 7, Yashui section; 8, Huashiban section; 9 Dala section; 10,Xiaodushan section.

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Studies by Ji et al. (1989) and further work(Kaiser 2009) indicate there are problems with the D–CBoundary GSSP (Paproth et al. 1991) at La Serre, France,and with the conodont lineage used for boundary defini-tion. The GSSP level at the base of bed 89 in the La Serresection seems to fall in the upper part of the Siphonodellasulcata Zone or even in the overlying Siphonodella dupli-cata Zone (Kaiser 2009). There is no record of the phylo-genetic transition from Siphonodella praesulcata to S.sulcata at La Serre (Kaiser 2009). Some studies showthat the determination of S. sulcata is subjective and thespecies is not a suitable marker for the base of theCarboniferous (Kaiser and Corradini 2011). TheDevonian and Carboniferous subcommissions of the ICShave formed a task group to work on the D–C boundaryproblem (Richards 2009). At present, the primary tasks forthe D–C boundary task group are to locate an appropriateevent marker to define the boundary and to find a suitablesection for the GSSP (Aretz 2014).

There is still no general agreement for the criteria ofthe D–C boundary definition, but there are some guide-lines for further activities and discussions (Aretz 2014). Amultidisciplinary approach should be used for boundarydefinition. The new boundary definition does not need tobe a conodont. The major late Famennian extinction(Hangenberg Event) is a good potential candidate for anew definition of the boundary (Aretz 2014).

2.1.2. Reference section for the base of the TournaisianStage in South China

The D–C boundary has been identified in several sectionsof pelagic or outer shelf facies in South China, includingthe Nanbiancun section in Guangxi (Yu 1988), which isthe auxiliary stratotype section for the D–C boundary, andthe Muhua and Dapoushang sections in Guizhou (Houet al. 1985; Ji et al. 1988, 1989). A biostratigraphicallywell-constrained tuff near the D–C boundary in theDapoushang section provides an excellent opportunity todate this important boundary (Liu et al. 2012). Herein, the

Dapoushang section is introduced as a reference section inSouth China.

(1) Location. The Dapoushang section is located inMuhua village, 25 km south of ChangshunCounty in Guizhou Province, South China(Figure 1).

(2) Geological background. The strata of theDapoushang section across the D–C boundary arecontinuous and well exposed. The section containsthe Upper Devonian Daihua Formation (beds 029–0) and the uppermost Devonian to lowerCarboniferous Wangyou Formation (beds 1–29),which are mainly composed of bioclastic lime-stone of pelagic facies (Ji et al. 1989; Liuet al. 2012).

(3) Biostratigraphy. In the D–C boundary section, fiveconodont zones have been identified: the MiddleSiphonodella praesulcata, Upper S. praesulcata,S. sulcata, Lower S. duplicata, and Upper S. dupli-cata zones (Ji et al. 1989; Figure 3). In addition,the section contains an abundance of other micro-and macrofossils (ammonoids, trilobites, ostra-codes, brachiopods, corals, and vertebratemicrofossils). Two vertebrate microfossil zones(the Phoebodus politus–Petalodus daihuaensisand Acanthodes guizhouensis zones) and twoammonoid zones (the Parawocklumeria andGattendorfia zones) have been identified acrossthe D–C boundary interval (Ji et al. 1989).

(4) U–Pb zircon age. Approximately 5–10 cm ofbrownish-yellow bentonite (tuff) directly under-lies bed 0, which is in the Upper praesulcataconodont Zone and located nearly 30 cm belowthe D–C boundary (base of bed 1) in theDapoushang section (Liu et al. 2012; Figure 4).U–Pb SHRIMP analyses of zircons from thetuff yielded a 206Pb/238 U concordia age of359.6 ± 1.9 Ma (Liu et al. 2012). Based on thisnew single-zircon SHRIMP age and previouslypublished work on the biostratigraphy andsequence stratigraphy of the D–C transition inter-val, the age of the D–C boundary at Dapoushang,Guizhou, China, is estimated to be 359.58 Ma(Liu et al. 2012).

In Muhua area, there are several D–C boundary sec-tions. Of these sections, the Muhua II and Dapoushangsections are suitable as the candidate section for the D–Cboundary GSSP (Hou et al. 1985; Ji et al. 1989). First,they have continuous limestone development across theD–C boundary. Second, they have continuous conodontzones and other significant fossil groups near the D–Cboundary. Third, they have more than one bed of volca-nic ash near the D–C boundary. The studies around the

Figure 2. Global subdivisions of the Carboniferous System(after Cohen et al. 2013).

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D–C boundary are now under way, including geochem-ical profiles and volcanic ash beds, which have the poten-tial for defining the boundary. The first volcanic ash bedyielding radiometric age around the Hangenberg equiva-lent beds in Muhua area may be a good marker for theD–C boundary.

2.2. Visean Stage

2.2.1. GSSP for the base of the Visean Stage

The GSSP for the base of the Visean Stage has beendefined at the base of bed 83 in the Pengchong section,Guangxi, South China (Devuyst et al. 2003; Houet al. 2013; Figure 1). The boundary is defined by theFAD of the benthic foraminifer Eoparastaffella simplexwithin the Eoparastaffella ovalis–E. simplex evolutionarylineage (Devuyst et al. 2003; Hou et al. 2013; Figure 5).

Figure 3. Distribution of conodonts in the Dapoushang section (after Ji et al. 1989). 1–2, Siphonodella praesulcata; 3–6, Siphonodellasulcata; 7–8, Siphonodella duplicata.

Figure 4. Devonian (D)–Carboniferous (C) boundary intervalin the Dapoushang section. The star indicates the location of thebentonite dated at 359.6 Ma.

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2.2.2. Pengchong GSSP in South China

(1) Location. The Pengchong section is located nearthe village of Pengchong, 15 km NNE of LiuzhouCity, and about 130 km SW of Guilin City, SouthChina (Figure 1).

(2) Geological background. Palaeogeographically, thePengchong area was located in an intraplatformbasin or on a basin slope during Mississippiantime (Devuyst et al. 2003). In this area, theCarboniferous lithostratigraphic sequence isdivided into, in ascending order, the Luzhai,

Bei’an, and Simen formations (Shen andTan 2009). The Luzhai Formation contains threemembers: the lower and upper members are com-posed of thin-bedded dark siliceous mudstoneinterbedded with thin-bedded chert, and the middlemember (the Pengchong Member) consists of darkgrey limestone beds of various thicknesses withsubordinate thin- to medium-bedded dark calcar-eous shales (Devuyst et al. 2003). The GSSPboundary horizon is located within thePengchong Member.

Figure 5. Tournaisian (T)–Visean (V) boundary interval in the Pengchong section (modified from Hou and Zhou 2008).

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(3) Biostratigraphy. The Pengchong Member in thePengchong section contains abundant and diversi-fied foraminifers and some important index con-odonts (Figures 5 and 6; Devuyst et al. 2003;Tian 2005; Hou et al. 2008, 2013). Three forami-niferal zones can be recognized: the UpperEoparastaffella rotunda Zone (from the base ofthe Pengchong Member to bed 82), theEoparastaffella simplex Zone (from the base ofbed 83 to bed 181), and the Pojarkovella nibelis

Zone (from the base of bed 182). The Tournaisian–Visean (T–V) boundary is placed at the firstappearance of E. simplex, at the base of bed 83.In addition, conodonts can be used as an auxiliarymarker. The FAD of the conodont Gnathodushomopunctatus is 5 m above the T–V boundary,and the last appearance datum (LAD) ofScaliognathus anchoralis europensis is 30 mbelow the T–V boundary (Hou and Zhou 2008;Hou et al. 2013).

Figure 6. Distribution of conodonts in the Tournaisian–Visean boundary interval in the Pengchong section (modified from Houet al. 2013).

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2.3. Serpukhovian Stage

The Visean–Serpukhovian boundary is not yet defined bya GSSP. An index for boundary definition has beenselected but has not been voted on by the task group andSCCS for final approval (Richards 2014).

For boundary definition, the task group uses theFAD of the conodont Lochriea ziegleri in the evolution-ary lineage Lochriea nodosa–L. ziegleri (Richards2014). This lineage, along with the associated faunasand strata, is being studied in several areas. The Naqing(Nashui) section in South China and the VerkhnyayaKardailovka section in the southeastern Urals ofRussia have the best potential as GSSP candidates(Richards 2010; Qi et al. 2013b).

2.4. Bashkirian Stage

2.4.1. GSSP for the base of the Bashkirian Stage

The GSSP for the base of the Pennsylvanian and of theBashkirian Stage has been fixed in the lower BirdSpring Formation at Arrow Canyon, in the GreatBasin, Nevada, USA, and is defined by the FAD of theconodont Declinognathodus noduliferus sensu lato withinthe evolutionary lineage Gnathodus girty simplex–Declinognathodus noduliferus s.l. (Lane et al. 1999).

2.4.2. Reference section for the base of the BashkirianStage in South China

The FAD of the conodont Declinognathodus noduliferushas been identified in many sections in South China,including the Baping section in Guangxi (Xu et al. 1987)and the Dianzishang and Naqing (formerly called theNashui or Luosu section) sections in Guizhou (Ruiet al. 1987; Wang et al. 2004; Qi et al. 2014). The latteris a reference section in South China.

(1) Location. The Naqing section is exposed on the sideof the Wangmo–Luodian highway (S312), 45 kmSWof Luodian county, 7 km SWof Luosu townshipand 2 km SWof the village of Naqing. The section iseasily accessible by car from Guiyang, the capital ofGuizhou Province (Figure 1).

(2) Geological background. The Naqing section is arelatively deeper-water carbonate-slope facies sec-tion that contains thin- to medium-bedded greywackestone and packstone beds intercalated withchert beds (Qi et al. 2013b).

(3) Biostratigraphy. The FADs of the conodontDeclinognathodus noduliferus and the fusulina-cean Millerella marblensis are at the base of bed6(B), which is the Mississippian–Pennsylvanian

boundary (Rui et al. 1987; Wang et al. 2004;Figure 7). The Gnathodus bilineatus bollandensisand Eostaffella mosqensis zones are belowthe boundary, and the Declinognathodus noduli-ferus and Millerella marblensis–Eostaffella post-mosquensis zones are above the boundary (Ruiet al. 1987; Wang et al. 2004).

The Naqing section is also the stratotype section ofChinese Luosuan Stage. This section has several advan-tages compared with other sections (Rui et al. 1987). First,it is well exposed, and composed of continuous sequencesof marine carbonates containing abundant and highlydiverse conodont and foraminiferal faunas. Second, it hasa transitional conodont fauna characterized by shallow anddeeper water types of conodonts, with a complete cono-dont sequence. Third, the conodont Declinognathodusnoduliferus made its first occurrence at the base ofLuosuan in association with the fusulinacean Millerellamarblensis.

2.5. Moscovian Stage

The base of the Moscovian Stage is not defined by aGSSP, and an index for the boundary definition has notbeen selected (Richards 2013; Alekseev 2014).

Several conodonts and fusulinids have been proposedas potential indices for the GSSP. Currently only twoconodont species, Declinognathodus donetzianus andDiplognathodus ellesmerensis, are considered to have sub-stantial potential for definition of a boundary positionclose to the original base of the type Moscovian(Alekseev 2014). If a morphologic chronocline could bedemonstrated from the ancestral species to Dip. ellesmer-ensis at Naqing, this would provide an almost ideal levelfor the GSSP (Qi et al. 2010; Groves 2011; Wanget al. 2011; Alekseev 2014).

Several candidate sections for the GSSP are beingstudied, but the Naqing section in southern GuizhouProvince, South China, appears to have the greatest poten-tial (Qi et al. 2010; Wang et al. 2011; Richards 2013;Alekseev 2014).

2.6. Kasimovian Stage

The base of the Kasimovian Stage is not defined by aGSSP, but the SCCS task group studying this boundaryhas concluded that the FADs of the conodontsIdiognathodus sagittalis and Idiognathodus turbatushave good potential as markers for the base of theKasimovian (Ueno et al. 2011; Richards 2013).Recently, the FAD of Idiognathodus heckeli, the

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precursor species to I. turbatus, has been considered asanother potential boundary marker (Ueno and TaskGroup 2014).

If the FAD of I. turbatus or I. heckeli is to be used forboundary definition, the Naqing (Nashui) section in south-ern Guizhou Province, South China, would be an excellentcandidate for the GSSP (Barrick et al. 2010; Qiet al. 2013a; Ueno and Task Group 2014).

2.7. Gzhelian Stage

The base of the Gzhelian Stage is not yet defined by aGSSP, but is defined by the FAD of the conodontIdiognathodus simulator sensu stricto in the potential evo-lutionary lineage Idiognathodus eudoraensis–I. simulator(Heckel et al. 2008; Villa et al. 2009).

In South China, the I. simulator fauna is moderatelyabundant and diverse across the Kasimovian–Gzhelian

Figure 7. Distribution of conodonts and foraminifers in the Naqing section (after Rui et al. 1987). 1–2, Millerella marblensis; 3,Millerella pressa; 4–5, Declinognathodus noduliferus noduliferus.

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boundary in the Naqing (Nashui) section (Barricket al. 2010; Ueno and Task Group 2014). The Naqingsection has promise as a potential GSSP candidate.

3. Regional chronostratigraphic units of China

The Carboniferous of China is well known for its well-developed strata, variety of depositional types, and abun-dant fossils. More than a century has passed since the firstpaper was published on the Chinese Carboniferous(Richithofen 1882). Since that time, extensive researchhas been carried out, and the regional chronostratigraphicframework of China has been established and improved(e.g. Yang et al. 1962; Hou et al. 1982; Zhang 1987; Wang1990b; Jin et al. 2000; Wang and Jin 2003).

The Carboniferous System in China was divided intotwo subsystems, four series, and eight stages in theCarboniferous volume of the Stratigraphic Lexicon ofChina (Jin et al. 2000; Figure 8); this scheme has beenwidely accepted (e.g. Wang and Jin 2000, 2003, 2005;Heckel and Clayton 2006; Menning et al. 2006; Davydovet al. 2012; Wang et al. 2013). The eight regional stagesare, in ascending order, the Tangbagouan, Jiusian,Shangsian, Dewuan, Luosuan, Huashibanian, Dalaun, andXiaodushanian. The traditional Carboniferous regionalstages of China used the unit stratotype concept, whichstrengthens the importance of rock units and of faunaassemblages, but have no clear definition for its basalboundaries, such as the Jiusi and Shangsi stages. At present,most Chinese stages, especially of the Upper Carboniferous,have clear boundary definitions using the FAD of the spe-cies of foraminifers or conodonts. The type sections of theregional stages in China are located in shallow-water facies,except for the Luosuan Stage, which is in a relatively

deeper-water facies. All the stratotypes of these regionalstages are located in South China, and are described below.

3.1. Tangbagouan Stage

(1) History. The stage was suggested by Jin et al.(2000) as a chronostratigraphic extension of theTangbagou Formation, which was named by Ting(1931).

(2) Definition. The boundary definition for the base ofthe Tangbagouan Stage is the same as that of theTournaisian. The stage corresponds roughly to thecoral Pseudouralinia Zone.

(3) Reference section. The Qilinzhai section is thestratotype, and is located 4 km W of DushanCounty, Guizhou Province, South China(Figure 1).

(4) Sedimentary characteristics. In type area, the stageincludes the Tangbagou Formation, which is com-posed of limestone, sandstone, and mudstone ofinner shelf facies (Jin et al. 2000).

(5) Biostratigraphy. In shallow-water facies, the fossilcontent of the Tangbagouan beds is dominated bythe rugose coral Pseudouralinia Zone, which canbe subdivided into three subzones: the Ps. tangpa-kouensis, Koninckophyllum sp.–Ps. tangpakouen-sis, and Ps. gigantea subzones (Jin et al. 2000).In addition, the stage contains three brachiopodzones (the Unispirifer–Yanguania, Martiniella–Eochoristites, and Finospirifer shaoyangensiszones) and six foraminiferal zones (theBisphaera, Chernyshinella, Palaospiroplectam-mina, Tuberendothyra, Spinoendothyra, andDainella zones). The conodont succession of thisstage consists of six zones, which are found inpelagic facies. These are the Siphonodella sulcata,S. duplicata, S. sandbergi, S. crenulata, S. isosti-cha, and Ganthodus typicus zones. The goniatitesGattendorfia spp., Initoceras folliformis, andI. simile are found in the S. duplicata Zone (Houet al. 1985; Ji 1987; Ji et al. 1988).

(6) Correlation. This stage can be correlated to thelower and middle parts of the Tournaisian Stage.In type area, the uppermost part of the TangbagouFormation, near the beds below the XiangbaiSandstone, contains foraminifers Dainella,Spinobrunsiina, Septabrunsiina, Planoendothyra,Paraendothyra, and others, and represent a begin-ning of the Dainella Zone (Hou et al. 2011). TheDainella Zone is in the upper Tournaisian (Hanceet al. 2011).

Figure 8. Chinese subdivisions of the Carboniferous System(after Jin et al. 2000).

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3.2. Jiusian Stage

(1) History. The name of this stage is taken from theJiusi Sandstone, which was established by Ting(1931).

(2) Definition. The stage is a chronostratigraphicextension of the Xiangbai and Jiusi formations. Ithas no clear lower boundary definition, which maybe within the foraminifer Dainella Zone.

(3) Reference section. The Jiusi section is the strato-type, and is located 4 km SW of what was pre-viously known as Datang County (now part ofLuodian County), Guizhou Province, SouthChina (Figure 1).

(4) Sedimentary characteristics. In the type area, thestage includes stratigraphic sequences composedof the Xiangbai and the Jiusi formations. TheXiangbai Formation contains sandstone and shaleof littoral facies. The Jiusi Formation consistsmainly of limestone, sandstone, and mudstone ofopen-platform deposits.

(5) Biostratigraphy. In shallow-water facies, thecoral and brachiopod faunas of this stage aregrouped into the Thysanophylloides Zone and theLevitusia humerusa–Delepinae subcarinata andVitiliproductus groeberi–Pugilis hunanensisassemblages (Zhang 2000). In pelagic facies, theJiusian Stage contains three conodont zones, theScaliognathus anchoralis, Gnathodus texanus–G.homopunctatus, and Lochriea commutata zones(Xiong and Zhai 1985; Wang 1990a).

(6) Correlation. This stage can be correlated to theupper part of the Tournaisian Stage and thelower part of the Visean Stage. The base ofJiusian Stage is placed at the base of theXiangbai Sandstone without any palaeontologi-cal marker. Based on foraminifer fromTangbagou Formation, the lower boundary maybe within the foraminifer Dainella Zone in theupper Tournaisian Stage.

3.3. Shangsian Stage

(1) History. The stage was first proposed by Zhang(1988) as the time equivalent of the ShangsiFormation or the Shangsi Limestone (Ting 1931).

(2) Definition. The stage has no clear lower boundarydefinition, but corresponds roughly to the coralYuanophyllum Range Zone.

(3) Reference section. The Liuzhai section is the stra-totype, and is located in the town of Baijin,Huishui County, Guizhou Province, South China(Figure 1).

(4) Sedimentary characteristics. In the type area, thestage includes most of the Shangsi Formation,which is mainly composed of open-platform lime-stone deposits.

(5) Biostratigraphy. In shallow-water facies, thecorals of this stage are recognized as being ofthe Yuanophyllum Range Zone, characterized byPalaeosmilia and Kueichouphyllum heishihkua-nense in the lower part, Aulina carinata inthe middle part, and Palastraea in the upperpart (Wang 1990b; Wang and Jin 2003).The foraminiferal succession consists ofthe Koskinotextularia, Neoarchaediscus, andEostaffella tenebrosa zones. In pelagic facies,the Jiusian Stage contains three conodont zones(the Gnathodus bilineatus bilineatus, Lochrieanodosa, and L. ziegleri zones).

(6) Correlation. This stage can be correlated to theupper part of the Visean Stage. The upperboundary of the Shangsian Stage is slightlyabove the top of the Visean Stage, and it iscorrelated to the base of the conodont Lochrieacruciformis Zone.

3.4. Dewuan Stage

(1) History. The stage was defined by Yang et al.(1980) as the time span of the Dewu Formation.

(2) Definition. The lower boundary of the stage isdefined by the FAD of the foraminifer‘Millerella’ pressula (Wu 2008a).

(3) Reference section. The Yashui section is the stra-totype, and is located in the town of Yashui,Huishui County, Guizhou Province, South China(Figure 1).

(4) Sedimentary characteristics. The Dewuan Stageincludes the uppermost Shangsi Formation to thelower Baizuo Formation in the Yashui section,which is dominated by carbonate rocks of shal-low-water facies.

(5) Biostratigraphy. The Dewuan beds contain the for-aminiferal ‘Millerella’ pressula and Eostaffellinaparaprotvae zones in the type Yashui section(Wu 2008a, 2008b). The stage also contains thebrachiopod Striatifera striata–Gigantoproductusedelburgensis Assemblage Zone and the coralKoninckophyllum–Dibunophyllum bipartitumZone. In pelagic facies, two conodont zones canbe discerned: the Lochriea cruciformis andGnathodus bilineatus bollandensis zones (Qi andWang 2005).

(6) Correlation. This stage can be correlated approxi-mately to the Serpukhovian Stage. The lower

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boundary of the Dewuan Stage is correlated to thebase of the conodont Lochriea cruciformis Zone,which is the second conodont zone above the baseof the Serpukhovian Stage.

3.5. Luosuan Stage

(1) History. The Luosuan Stage was named by Ruiet al. (1987) and its type section is at Luosutownship.

(2) Definition. The lower boundary of this stage ismarked by the FAD of the conodontDeclinognathodus noduliferus noduliferus or thefusulinaceanMillerella marblensis (Rui et al. 1987).

(3) Reference section. The Luosu section is the stra-totype, and is located about 7 km SW of Luosu,Luodian County, Guizhou Province, South China(Figure 1). The Luosu section is also called theNashui section or the Naqing section in theliterature.

(4) Sedimentary characteristics. The rock sequenceof the Lusuan Stage in the type section is com-posed mainly of planar-laminated wackestoneinterbedded with packstones, grainstones, andcherty beds, representing slope deposits (Ruiet al. 1987).

(5) Biostratigraphy. Five conodont zones have beenidentified. In ascending order, they are theDeclinognathodus noduliferus, Idiognathoides sul-catus sulcatus, I. sinuatus, I. corrugatus–I. pacifi-cus, and Neognathodus symmetricus zones in thetype section (Wang and Qi 2002; Wanget al. 2004). The Luosuan beds also contain thefusulinacean Millerella marblensis–Eostaffellapostmosquensis Zone (Rui et al. 1987) and theammonoid Homoceras Zone (Ruan 1981).

(6) Correlation. This stage can be correlated to thelower part of the Bashkirian Stage. The lowerboundaries of the Luosuan and Bashkirian stagesare coincident and defined by the FAD of theconodont Declinognathodus noduliferus (Ruiet al. 1987; Lane et al. 1999). And the upperboundary of the Luosuan Stage is coincidentwith the base of the fusulinacean Pseudostaffellaantiqua Zone, which is in the lower part ofBashkirian Stage (Zhang et al. 2004; Davydovet al. 2012).

3.6. Huashibanian Stage

(1) History. This stage was first named by Yang et al.(1980) after the Huashiban Formation.

(2) Definition. The lower boundary of the HuashibanStage is defined by the FAD of the fusulinaceanPseudostaffella antiqua, within the Eostaffellinaprotvae–Pseudostaffella antiqua evolutionary line-age (Zhang et al. 2004, 2008a).

(3) Reference section. The stratotype is situated atHuashiban village, about 30 km E of PanxianCounty, Guizhou Province, South China(Figure 1).

(4) Sedimentary characteristics. In the type section,the stage is represented by the HuashibanFormation, which is mainly composed of open-platform limestone deposits.

(5) Biostratigraphy. In the type section, two fusulinaceanzones are present, the Pseudostaffella antiqua–P.antiqua posterior and the Pseudostaffella compo-sita–P. paracompressa zones. The stage containstwo ammonoid zones: the Reticuloceras guiz-houense and Branneroceras branneri–Gastriocerascf. cumbriensis zones (Zhang et al. 2008a). Theassociated corals and brachiopods are assigned tothe Lithostrotionella stylaxis–Carinthiaphyllumexquisitum–Acrosyathus Assemblage Zone and theChoristites mansuyi–Plicatifera chaoi AssemblageZone, respectively (Jin et al. 2000).

(6) Correlation. This stage can be correlated to themiddle part of the Bashkirian Stage, because thefusulinacean Pseudostaffella antiqua–P. antiquaposterior Zone of the lower part of theHuashibanian is correlated to the Psedostaffellaantiqua Zone of the middle part of theBashkirian Stage (Zhang et al. 2004; Davydovet al. 2012).

3.7. Dalaun Stage

(1) History. The stage name was derived from theDala Formation, which was established by Jinet al. (1962).

(2) Definition. The lower boundary of the DalaunStage is marked by the first appearance of thefusulinacean Profusulinella (e.g. P. priscoidea orP. parva; Zhang et al. 2008b).

(3) Reference section. The stratotype is situated atDala village, about 30 km E of Panxian County,Guizhou Province, South China (Figure 1).

(4) Sedimentary characteristics. In the type section,the stage is represented by the Dala Formation,which mainly consists of limestone deposited inan open-platform environment.

(5) Biostratigraphy. There are six fusulinacean zones inthe type section: the Profusulinella priscoidea–P.parva, Profusulinella aljutovica–Taitzehoella

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taitzehoensis extensa, Fusulinella obesa–Fusulinella eopulchra, Fusulina lanceolata–Fusulinella vozhgalensis, Fusulina pakhrensis–Pseudostaffella paradoxa, and Fusulina cylin-drica–Fusulina quasifusulinoides zones. In westernGuizhou and eastern Yunnan, the Dalaun beds con-tain rugose corals of the Arachnastraea–Kionophyllum Zone. The stage also contains twobrachiopod assemblage zones: the Semicostellapanxianensis–Linoproductus planata and Buxtoniagrandis assemblage zones (Zhang 2000).

(6) Correlation. This stage can be roughly correlatedto the upper part of the Bashkirian Stage and theMoscovian Stage, because the fusulinaceanProfusulinella priscoidea–P. parva Zone of thelower part of the Dalaun Stage is correlated tothe Profusulinella parva–Ozawainella pararhom-boidalis Zone of the upper part of the BashkirianStage, and the fusulinacean Fusulina cylindrica–F.quasifusulinoides Zone of the upper part of theDalaun Stage is correlated to the Fusulinellabocki–Fusulina cylindrica Zone of the upper partof the Moscovian Stage (Zhang et al. 2004;Davydov et al. 2012).

3.8. Xiaodushanian Stage

(1) History. The name Xiaodushan Stage was given byZhou et al. (1987), with the type section situated atXiaodushan village.

(2) Definition. The lower boundary of this stage isdefined by the first appearance of the fusulinaceanProtriticites (Zhou et al. 1987).

(3) Reference section. The Xiaodushan section is thestratotype, and is located in Xiaodushan village,Guangnan County, Yunnan Province, South China(Figure 1).

(4) Sedimentary characteristics. The Xiaodushanianbeds in the type section are mainly composed ofopen-platform limestone deposits.

(5) Biostratigraphy. Five fusulinacean zones havebeen identified in the type section (in ascendingorder): the Protriticites subschwagerinoides,Triticites montiparus, T. schwageriniformis, T.dictyophorus, and T. shikhanensis compactuszones (Zhou et al. 1987). In most areas of SouthChina, the fusulinaceans of this stage are usuallygrouped into two genozones, the Montiparus andTriticites zones (Wang and Jin 2003). The coraland brachiopod faunas of this stage aregrouped into the Nephelophyllum–Pseudotimania–Pseudocarniaphyllum Zone and the Choristites

jigulensis–Protanidanthus Assemblage Zone,respectively (Zhang 2000).

(6) Correlation. This stage can be roughly correlatedto the Kasimovian and Gzhelian stages, becausethe fusulinacean Protriticites subschwagerinoidesZone of the lower part of the Xiaodushanian Stageis correlated to the Protriticites ovoides–Praeobsoletes burkemensis Zone of the uppermostpart of the Moscovian Stage or the Protriticitespseudomontiparus Zone of the lower part of theKasimovian Stage (Zhou et al. 1987; Davydovet al. 2012).

4. Carboniferous stratigraphic chart of South China

Figures 9 and 10 and the Supplemental Figure at http://dx.doi.org/10.1080/00206814.2015.1008591 show a compre-hensive Carboniferous stratigraphic correlation chart forSouth China. Some of the major features of the chart areexplained below.

The international Carboniferous time scale and bios-tratigraphic zonation (ammonoids, foraminifers, andconodonts) were taken from The Geologic Time Scale2012 (Davydov et al. 2012), with minor modifications,including moving the conodont Scaliognathus anchoralisZone from the lower Visean to the uppermost Tournaisian,which is widely supported (Lane et al. 1980; Belka 1985;Webster and Groessens 1991; Perret and Delvolvé 1994;Perri and Spalleta 1998; Tian 2005), and is consistent withthe Pengchong GSSP.

The numerical ages for the stage boundaries in theCarboniferous are taken from The Geologic Time Scale2012 (Davydov et al. 2012) and the 2014 version of theICS International Stratigraphic Chart (Cohen et al. 2013).

The Carboniferous chronostratigraphic framework ofChina is from the Carboniferous volume of theStratigraphic Lexicon of China (Jin et al. 2000). Theregional stages in China are based on successions inSouth China.

In South China, 39 conodont zones (Wang andQi 2003; Wang et al. 2004, 2011; Qi and Wang 2005;Qi 2008; Qi et al. 2014), 26 foraminiferal zones (Rui et al.1987; Zhou et al. 1987; Ji et al. 2000; Wu and Liao 2001;Zhang et al. 2004, 2005, 2008a, 2008b; Wu 2008a, 2008b;Hance et al. 2011; The National Commission onStratigraphy of China 2012), 11 ammonoid zones (Wang1990b; Jin et al. 2000; Wang and Jin 2003), 7 rugose coralzones (Wang 1990b; Jin et al. 2000), and 12 brachiopodzones (Jin et al. 2000; Zhang 2000) have been established.

Based on tectonic setting, lithofacies associations, andbiotic assemblages, South China can be divided into twodepositional provinces: the Yangtze Province and the

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Figure9.

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Figure10

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Southeast Province (Wang et al. 2013). Twenty-three typi-cal lithostratigraphic successions of South China areshown in the chart (Figures 9 and 10), and the locationsof these successions are marked by numbers in Figure 11.The thicknesses of Carboniferous units in different areasof South China are variable and the typical ones aresummarized in Figure 12.

5. Conclusions

(1) GSSPs for the bases of the Tournaisian, Visean,and Bashkirian stages have been officiallyratified for the Carboniferous System. All threeestablished GSSPs markers have been identifiedin several sections in South China. The baseof the Visean Stage is fixed with a GSSP in thePengchong section, South China. The Dapoushangand Naqing sections are excellent reference sec-tions for the bases of the Tournaisian andBashkirian stages, respectively.

(2) The Carboniferous of South China has goodpotential to study the four unestablished GSSPsand the D–C boundary. Moreover, the Naqing(Nashui) section is a candidate for GSSPs for theSerpukhovian, Moscovian, Kasimovian, andGzhelian stages. In the future, South China willplay a significant role in improving the globaldefinition of the Carboniferous System.

(3) Regional Carboniferous stages in China are theTangbagouan, Jiusian, Shangsian, Dewuan,Luosuan, Huashibanian, Dalaun, andXiaodushanian stages. All the type sections ofthe Chinese stages are located in South China,and most of the stratotypes of those stages arewell studied in terms of biostratigraphy and sedi-mentary characteristics.

(4) The Carboniferous stratigraphic chart of SouthChina provides a comprehensive summary of thecurrent status of the Carboniferous in South China.It represents a new practical framework forCarboniferous subdivision and correlation inSouth China.

Figure 11. Distribution of Carboniferous outcrops and lands in South China (base map modified from Wang et al. 2013). I, Yangtzeprovince; I1, Longmenshan subprovince; I2, Ninglang–Dali subprovince; I3, Dian–Qian–Gui subprovince; I4, Upper Yangtze subpro-vince; I5, Lower Yangtze subprovince; II, Southeast Province; II1, Qinzhou subprovince; II2, Xiang-Gui subprovince; II3, Zhe–Min–Gan–Yue subprovince. The circled numbers (1 to 23) indicate the locations of typical lithostratigraphic successions in South China, and theycorrespond to those in Figures 9 and 10.

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Figure12

.Thickness

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AcknowledgementsThe authors thank Professor Hou Hong-fei, Jin Xiao-chi, Shi Yu-kun, Wu Xiang-he, Yin Bao-an, Yao Jian-xin, Robert J. Stern,and Dr Xi Dang-peng for their support and valuable suggestions.

Disclosure statementNo potential conflict of interest was reported by the authors.

FundingThis research was supported by China Geological Survey[1212011120116].

Supplemental dataSupplemental data for this article can be accessed at 10.1080/00206814.2015.1008591.

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