Le YAO, Markus ARETZ, Yue LI & Xiangdong WANG

Gigantoproductid brachiopod storm shell beds in the Mississippian of South China: implications for their palaeoenvironmental and palaeogeographical significances

Document(s) associé(s)

Annexes

• GB 19-1-2 Yao et al_Low-Res (11M)
• GB 19-1-2 Yao et al_High-Res (41M)

Abstract

Late Viséan to Serpukhovian (Mississippian, Carboniferous) storm shell beds of Gigantoproductus (Brachiopoda) are documented for the first time in South China. The shell beds are characterized by sharp and erosional base, internal accumulations of amalgamated shells with erosional structure, and parallel lamination and ripple bedding structures in the uppermost part, indicating obvious characteristics of tempestites. In the shell beds, three taphonomic and sedimentologic types have been distinguished, which are: type A: mostly articulated and convex-down shells in wackestone and packstone, which are developed in distal tempestites with weak water energy around the storm wave-base; type B: dominated disarticulated and convex-up shells in packstone that occur between distal and proximal tempestites in medium hydrodynamic force between the storm wave-base and fair-weather wave-base; and type C: highly fragmented shells in grainstone formed in proximal tempestites under strong hydrodynamic energy above the fair-weather wave-base. The occurrences of proximal and distal tempestites suggest that they were formed by winnowing and transporting under storm surges. During the late Viséan to Serpukhovian, the widely distributed storm shell beds in South China reflect that the South China Block was located in hurricane zone between latitude 10° and 30° during this time interval, when ice caps formed on the Gondwana continent.

Table des matières

1. Introduction

1Storm beds are distinct facies criteria on shelves and ramps, which are generated by storm winds, such as cyclones and hurricanes in tropical latitudes and blizzards in middle and high latitudes (Tucker & Wright, 1990; Flügel, 2004). Ager (1973) defined storm beds as tempestites that are commonly characterized by sharp and erosional base, internal structures including accumulations of shells, graded and flat bedding and parallel and cross lamination, and ripple bedding and burrowing presented at the top part (Aigner, 1985; Flügel, 2004; Dattilo et al., 2012). Tempestites are abundant and widely distributed in carbonate environments during the Phanerozoic (e.g. Einsele & Seilacher, 1982; Flügel, 2004). The sedimentary patterns and biotic distributions of tempestites could provide important information in aspects of their depositional process, palaeoenvironment, palaeogeographical location and even stratigraphic comparison (Johnson, 1989; Lehman & Pope, 1989; Flügel, 2004; Jin et al., 2013).

2Storm shell beds, which are one common type of tempestites and featured by accumulation of shells, were documented during the icehouse periods of the late Ordovician (Lehman & Pope, 1989; Davis, 1999; Jin et al., 2013), early Silurian (Johnson, 1989; Li & Rong, 2007; Jin, 2008) and early Carboniferous (Jeffery & Aigner, 1982; Butts, 2005) and during greenhouse climate, as in the middle Ordovician (McFarland et al., 1999), late Permian (Simões & Kowalewski, 1998), early Triassic (Boyer et al., 2004), late Jurassic (Fürsich, 1982) and late Early Cretaceous (Fürsich & Kauffman, 1984). Common to all is that their formation is connected to hurricane formation in the tropical belt of the respective timeslice. In storm shell beds, taphonomic characteristics of shells are generally characterized by amalgamation of articulated, disarticulated and fragmented shells with non-directional distribution (Aigner, 1985; Jin et al., 2013), ranging from proximal tempestites with more disarticulated and fragmented shells to distal tempestites with more articulated and less fragmented shells (Johnson, 1989; Lehman & Pope, 1989). Sedimentologic features of tempestites also vary from proximal tempestites to distal tempestites dominated by grainstone and mudstone respectively, implying different hydrodynamic energy driven by storm surges and water depths (Aigner, 1985; Butts, 2005; Dattilo et al., 2012). In addition, a comprehensive study on the relationships between taphonomy of shell beds and their palaeogeographical locations was conducted in the late Ordovician (Jin et al., 2013). It was found that non-amalgamated shell beds were located in hurricane-free zone within 10° of the equator because of the weak Coriolis force. Whereas, amalgamated shell beds occurred in hurricane zone between latitude 10° and 30° (Jin et al., 2013). Thus, a relatively precise position of a palaeoequator could be proposed when mapping the spatial distributions of non-amalgamated shell beds and storm shell beds. When the temperature gradient between pole and equator should have been similar to those of the Recent, the zones in which most modern hurricanes occur north and south of the equator (10°-30°), could be transferred into the deep time.

3In South China, storm beds were extensively recorded during the Phanerozoic (Liu et al., 1986; Zhang et al., 1993; Li & Rong, 2007; Zhang, 2013). However, storm shell beds have been rarely documented and only a few cases were described in the early Silurian (Li & Rong, 2007). In the Mississippian, brachiopods were globally distributed and one of the dominant benthic fossil groups (Qiao & Shen, 2014). Especially, a great number of large-sized species, belonging to the genus Gigantoproductus of subfamily Gigantoproductinae, have been recorded during the Viséan-Serpukhovian around the world (Qiao & Shen, 2015). Besides, Mississippian is the initial stage of the late Palaeozoic glaciation with prominent glacial deposits on the Gondwana continent (Isbell et al., 2003, 2012; Fielding et al., 2008; Yao et al., 2015). They all provide suitable conditions for the development of storm shell beds. However, to date, no storm shell beds have been reported in the Mississippian strata in South China.

4In this paper, brachiopod shell beds have been studied in Huishui County of Guizhou Province in the Yashui (YS) (26°00′47.6″N, 106°45′28.0″E) and Duanshan (DS) (25°50′07.6″N, 106°36′17.9″E) sections located at about 4 km north of Yashui town and about 3 km east of Duanshan town respectively, and in Tianlin County of Guangxi Province in the Gandongzi (GDZ) (24°31′55.2″N, 106°21′36.9″E) section located at about 1 km west of Gandongzi village (Fig. 1a, b). The main purposes of this study are (1) to describe taphonomic and sedimentologic characteristics of the shell beds; (2) to interpret mechanism of the shell bed formation; (3) to provide implications of the shell beds for their palaeoenvironmental and palaeogeographical significances.

5Figure 1. (a) Location of Guizhou and Guangxi provinces, and their capital cities in China. GZ: Guizhou Province, GX: Guangxi Province. (b) Location of the studied sections, the map of Fig. 1 (b) is the amplification of the shadow area of Fig. 1 (a). (c) Global palaeogeography map for the middle-late Mississippian (340 Ma) (after Blakey, 2011). The black rectangle represents the Fig. 1 (d); note that the South China craton was rotated ~90° counter-clockwise relative to its modern orientation. (d) The Viséan-Serpukhovian palaeogeography of the South China Block (after Feng et al., 1998) and location of the studied sections. DQGX: Dian-Qian-Gui-Xiang platform, LP: Langping isolated platform, QG: Qian-Gui basin.

2. Geological setting

2.1. Palaeogeography

6During Viséan to Serpukhovian times, the South China Block (SCB) was located in the Southern Hemisphere near the equator in the northeastern Palaeotethys. It consists of Yangtze and Cathaysia Old Lands (Fig. 1c). Between these two topographical emerged highs, the marine facies realm is highly differentiated (Fig. 1d) (Feng et al., 1998). Narrow nearshore siliciclastic belts border the southern Yangtze and western Cathaysia Old Lands. Most parts of the SCB are covered by shallow water carbonates of the Dian-Qian-Gui-Xiang carbonate platform. This platform is dissected by several basins and the largest one, the Qian-Gui basin includes the isolated Langping carbonate platform. The basins are NE-SW and NW-SE trending rifts and lithologically dominated by black shales, thin-bedded limestones and siliceous rocks (Jiao et al., 2003). Deep-basin facies are located in the eastern part of the SCB (southern in present day) (Fig. 1c, d) (Feng et al., 1998). In this study, the Yashui and Duanshan sections, and the Gandongzi section are located on the margins of the Dian-Qian-Gui-Xiang platform and Langping platform, respectively (Fig. 1d).

2.2. Lithostratigraphy

7Correlations of Mississippian strata in South China were summarized by Wang & Jin (2000), Hance et al. (2011) and Wang et al. (2013). In the upper Viséan to Serpukhovian, the Shangsi and Baizuo formations are separated in the Huishui area, whereas the Du’an Formation comprises the entire interval in Tianlin area (Hance et al., 2011; Wang et al., 2013). In the Yashui section, the upper Shangsi Formation (30 m thick) consists of light-grey to dark-grey, middle- to thick-bedded (c. 0.2 to c. 1.0m) mudstone, wackestone and packstone interbedded with shale, nodular limestone and dolomitic limestone, yielding abundant corals and brachiopods (Lin et al., 2012). One distinct palaeokarst surface occurs at the top of this formation. The Baizuo Formation (88 m thick) contains light-grey to dark-grey, medium- to thick-bedded wackestone, packstone and grainstone intercalated with shale, muddy limestone, dolomitic limestone and breccia rich in brachiopod and coral faunas (Lin et al., 2012)(Fig. 2). The shale deposits in Yashui section result from carbonate dissolution (karstification) and siliciclastic sediment input, which implies a very shallow water (Chen et al., 2016). According to Groves et al. (2012) “pervasive lime mud, calcispheres, and a variety of skeletal calcareous algae suggest a relatively quiet setting within the euphotic zone”. In the Duanshan section, the Shangsi Formation (30 m thick) is mainly composed of dark-grey thick-bedded (c. 1.0m) wackestone and packstone including abundant brachiopods and corals. The absence of shallow-water shale deposits, dolomitic limestone and palaeokarst surface from this section indicates a relatively deeper shallow marine environment, compared with the Yashui section (Fig. 2). In the Gandongzi section, the Du’an Formation (60 m thick) contains light-grey to dark-grey thick massive packstone and grainstone interbedded with mudstone and wackestone. They are rich in brachiopods, crinoids and oncolites, implying a shallow marine turbulent environment (Fang & Hou, 1986) (Fig. 2).

8Figure 2. Lithologic columns of the upper Viséan-Serpukhovian strata and location of Gigantoproductus shell beds in the Yashui, Duanshan and Gandongzi sections. S: Shale, M: Muddy limestone/Mudstone, W: Wackestone, P: Packstone, G: Grainstone, R: Rudstone, B: Brachiopod shell bed, DSB: The shell bed in the Duanshan section, GSB: The shell bed in the Gandongzi section, YSB: The shell bed in the Yashui section.

9Brachiopod shell beds have been studied from the upper Shangsi and Baizuo formations in the Yashui section, the Shangsi Formation in the Duanshan section and the Du’an Formation in the Gandongzi section (Fig. 2). The taxonomic composition of the brachiopods in the shell beds is dominated by one genus (Gigantoproductus), which is identified based on their characteristics of large shells with large width (adult individual usually more than 10 cm wide), strong curved trail and shell line, small body cavity and concave-convex shell type (Prentice, 1950) (Fig. 3a, b). At the Yashui section, two Gigantoproductus shell beds (YSB₁ in the lower part and YSB₂ in the upper part) are developed in the Shangsi Formation and Baizuo Formation with thin thicknesses of 0.3 m and 0.5 m, respectively (Fig. 2). Most Gigantoproductus shells are concordant (disarticulated and convex-up) with loosely packed in the YSB₂ (Fig. 3c). Two Gigantoproductus shell beds (DSB₁ in the lower part and DSB₂ in the upper part) are present in the Shangsi Formation in the Duanshan section and their thicknesses are medium and vary from 1 m to 1.5 m (Fig. 2). Gigantoproductus shells are majorly concordant (disarticulated and convex-up) and densely packed, with coral fragments horizontally preserved in the DSB₁ (Fig. 3b, d). At the Gandongzi section, four Gigantoproductus shell beds have been recognized in the Du’an Formation (Fig. 2). At the base of the Gandongzi section, a Gigantoproductus shell bed (GSB₁) is very thick (about 13 m) with vertical changes of the Gigantoproductus shell abundances. These are concordant dominated by articulation and convex-down (Fig. 3e). The other three shell beds (GSB₂, GSB₃ and GSB₄) of the upper Gandongzi section are medium in thickness of 0.5 m to 2 m, comprising high-breakage and densely packed Gigantoproductus shells (Fig. 3f).

10Figure 3. Field photographs of Gigantoproductus and their shell beds. (a) Ventral valve of Gigantoproductus in the shell bed at the base of the Gandongzi section (GSB1). Gi: Gigantoproductus. (b) Gigantoproductus and solitary rugose corals in the lower Gigantoproductus shell bed in the Duanshan section (DSB1). Gi: Gigantoproductus, SR: Solitary rugose coral. (c) Upper Gigantoproductus shell bed in the Yashui section (YSB2). Gi: Gigantoproductus. (d) Lower Gigantoproductus shell bed in the Duanshan section (DSB1), the area of the yellow rectangle is Fig. 3 (b). Gi: Gigantoproductus. (e) Gigantoproductus shell bed at the base of the Gandongzi section (GSB1). Gi: Gigantoproductus, HA: High abundance, LA: Low abundance. (f) Gigantoproductus shell bed in the upper part of the Gandongzi section (GSB3). Gi: Gigantoproductus.

2.3. Biostratigraphy

11A rough age determination is due to the stratigraphic distribution of the genus Gigantoproductus from the middle Viséan to the Serpukhovian (Qiao & Shen, 2015). Carbonate microfossils, especially foraminifers indicate more precise ages. In the Yashui section, Wang (2011) and Groves et al. (2012) conducted high-precision foraminifer biostratigraphy. The lower part of the Yashui section yields abundant typical late Viséan foraminifers such as Eostaffella, Endothyra, Archaediscus, Earlandia, Pseudoendothyra and Endothyranopsis, and is equivalent to the MFZ15 foraminiferal Zone in Europe (Poty et al., 2006). The Viséan-Serpukhovian boundary is determined at 49 m based on the lowest occurrence of rare ‘‘tortula-like’’ specimens, a potential Serpukhovian marker (Groves et al., 2012) (Fig. 2). The foraminifers Biseriella, Zellerinella, Globoendothyra, Globivalvulina and Paraarchaediscus indicate a Serpukhovian age for the upward part (Wang, 2011). In the Duanshan section, the occurrences of the foraminifer assemblage including Endothyranopsis, Eostaffella, Endothyra, Koskinobigenerina and Climacammina, indicate a late Viséan age (Poty et al., 2006; Groves et al., 2012). At the Gandongzi section,the presence of Endothyranopsis, Koskinobegenerina and Climacammina also suggests a late Viséan age (Poty et al., 2006; Groves et al., 2012). Thus, the shell beds are late Viséan in age, except the shell bed YSB₂, which is Serpukhovian in age.

3. Materials and methods

12A total of 57 samples were collected from the underlying limestones of Gigantoproductus shell beds to the overlying limestones of the shell beds in the Gandongzi section, and from the shell beds in the Yashui and Duanshan sections. For each sample, at least one orientated thin section was made, and a total of 76 thin sections (about 40×50 mm sized) are available for microfacies analysis. Description of the shell beds is based on the conceptual framework provided by Kidwell et al. (1986) and Kidwell & Holland (1991). Quantitative analysis of the contents of disarticulated, articulated, and convex-up and -down shells by counting relevant shells based on a well exposed, relatively flat and smooth surface (about 50×50 cm sized) was done at the YSB₂ and GSB₁ following the method of Chen et al. (2013). Identification of microfacies types follows the classification schemes proposed by Dunham (1962) and Embry & Klovan (1971).

4. Results

4.1. Taphonomy

13Three distinct taphonomic types of Gigantoproductus shells are distinguished in terms of articulation or disarticulation, orientation (convex-up or -down) and fragmentation degree of the shells in the studied shell beds (Fig. 4, Table 1). Type A (TA) is characterized by articulated and convex-down shells with low fragmentation, which is rare and only present in the GSB₁ at the base of the Gandongzi section (Fig. 4a, Table 1). Type B (TB) is featured by disarticulated and convex-up shells with medium fragmentation (Fig. 4b, Table 1), and commonly occurs in the shell beds in the Yashui and Duanshan sections. Type C (TC) is represented by high-breakage shells, and developed in the GSB₂, GSB₃ and GSB₄ in the upper part of the Gandongzi section (Fig. 4c, Table 1). Quantitative analysis of disarticulated, articulated, convex-up and -down and fragmented shells is carried out in the TA and TB shell beds (Fig. 5a, b). It is not done for the TC shell beds due to the almost exclusiveness of highly fragmented shells in these beds (Fig. 5c, d).

14Figure 4. Sketch of taphonomic types and sedimentary characteristics of Gigantoproductus shell beds. Type A is characterized by articulated and convex-down shells with low fragmentation, much micrite and few sparry calcite. Type B is dominated by disarticulated and convex-up shells with medium fragmentation, medium micrite and sparry calcite. Type C is featured by high-breakage shells, cemented by sparry calcite.

15….

16Table 1. Comparison of the three taphonomic types of Gigantoproductus shell beds in South China.

17Figure 5. Field photographs and polished slab of three different taphonomic types in Gigantoproductus shell beds. (a) Mostly articulated and convex-down shells (Black triangle) in the shell bed at the base of the Gandongzi section (GSB1). (b) is the enlargement of the area of the yellow rectangle in Fig. 3 (c) and displays the dominated disarticulated and convex-up shells (White triangle) in the shell bed in the upper part of the Yashui section (YSB2). (c) is the amplification of the yellow rectangle area in Fig. 3 (f) and shows the high-breakage shells (White triangle) in the shell bed in the upper part of the Gandongzi section (GSB3). (d) Highly broken shells (White triangle), polished slab in the GSB3, Gandongzi section.

4.1.1. Disarticulated or articulated shells

18In the GSB₁ (TA shell bed), the shells include 44 articulated shells (52%) of the 85 counted shells (Fig. 5a, Table 2), which implies a relatively weak hydrodynamic energy (Johnson, 1989; Lehman & Pope, 1989; Chen et al., 2013). The low proportion of shell fragments (9%) supports this hypothesis (Table 2). The shells in the YSB₂ (TB shell bed) comprise 74 disarticulated shells (88%) relative to 10 articulated shells (Fig. 5b, Table 2). The high amounts of disarticulated shells indicate a strong hydrodynamic force, driven by storm surges and water currents (Johnson, 1989; Lehman & Pope, 1989; Chen et al., 2013). The content of shell fragmentation is medium high (31%) in the YSB₂, compared with the GSB₁ (Table 2).

19….

20Table 2. Quantitative data of Gigantoproductus shells from the shell beds in South China.

4.1.2. Convex-up or -down shells

21Among the 58 convex-up and -down shells examined on the surface of the GSB₁, 41 shells (71%) are arranged in convex-down orientation with 17 shells (29%) convex-up (Fig. 5a, Table 2). Taphonomic studies revealed that the shell assemblage dominated by convex-down and -up shells was caused by low and high water energy, respectively (Jeffery & Aigner, 1982; McFarland et al., 1999; Butts, 2005; Chen et al., 2013). Hence, in the GSB₁, the high contents of shells in convex-down orientation indicate that the shells were affected by low hydrodynamic energy before they were buried (Jeffery & Aigner, 1982; Butts, 2005). According to the observation of 45 convex shells on the surface of the YSB₂, 35 shells (78%) are convex-up and 10 shells (22%) are convex-down (Fig. 5b, Table 2).

4.2. Microfacies characteristics

22From the systematic studies on the microfacies of Gigantoproductus shell beds in the Yashui, Duanshan and Gandongzi sections, sedimentary structures, including sharp and erosional base, erosional surface, parallel and ripple lamination/bedding and geopetal structures, and microfacies types, containing mudstone, wackestone, packstone and grainstone, are identified (Fig. 6, Table 1).

4.2.1. Base of the shell bed

23The base of tempestites is generally characterized by a sharp and erosional surface (Flügel, 2004), which is found at the base of the GSB₃ in the upper Gandongzi section (Fig. 6a). The underlying bed is a peloidal packstone mainly composed of medium to well sorted peloids. Bioclastic grains include crinoids, which are rare and make up about 5% of the total components. The spaces between the peloids and bioclasts are filled with micrite and sparry calcite (Fig. 6a). A distinct sharp and erosional boundary is present at the base of the shell bed and characterized by a sparry calcite belt, which suggests high water energy (Yao et al., 2016). This hypothesis was also supported by the highly fragmented shells and rounded and well sorted peloids in the sparry calcite (Fig. 6a). Above this boundary lay grainstones mainly composed of brachiopods, crinoids and peloids cemented by sparry calcite. The brachiopods show high breakage and non-directional distribution, and the peloids are generally well sorted (Fig. 6a).

24Figure 6. Microfacies types and sedimentary structures in Gigantoproductus shell beds. (a) Sharp and erosional base (White triangle) in Gigantoproductus shell bed in the upper part of the Gandongzi section (GSB3). Bra: Brachiopod, C: Crinoid, F: Foraminifer, P: Peloid, SC: Sparry calcite. (b) Wackestone with geopetal structure in Gigantoproductus shell bed at the base of the Gandongzi section (GSB1). DS: Dorsal valve, Gi: Gigantoproductus, M: Micrite, SC: Sparry calcite, VS: Ventral valve. (c) Packstone in Gigantoproductus shell bed at the base of the Gandongzi section (GSB1). C: Crinoid, Gi: Gigantoproductus, P: Peloid. (d) Packstone with erosional surface (White line) in Gigantoproductus shell bed in the lower part of the Duanshan section (DSB1). Bra: Brachiopod, C: Crinoid, F: Foraminifer, G: Gastropod, Gi: Gigantoproductus, M: Micrite, P: Peloid, SC: Sparry calcite. (e) Packstone with geopetal structure in Gigantoproductus shell bed in the upper part of the Yashui section (YSB2). Bra: Brachiopod, C: Crinoid, Gi: Gigantoproductus. (f) Grainstone in Gigantoproductus shell bed in the upper part of the Gandongzi section (GSB3). Bra: Brachiopod, C: Crinoid, CA: Calcareous algae, F: Foraminifer, ME: Micrite envelope, O: Oncoid, P: Peloid, SC: Sparry calcite. (g) Ripple boundary (White line) between different components in the mudstone at the uppermost part of Gigantoproductus shell bed in the upper part of the Gandongzi section (GSB3). Bra: Brachiopod, C: Crinoid, M: Micrite, SC: Sparry calcite. (h) Parallel lamination structure in the mudstone at the uppermost part of Gigantoproductus shell bed at the base of Gandongzi section (GSB1). Bra: Brachiopod, C: Crinoid, PL: Parallel lamination.

4.2.2. Interior of the shell beds

Type A shell bed

25The microfacies of the GSB₁ consist of wackestone and packstone, which are featured by articulated Gigantoproductus shells (Fig. 6b, c). The shells are the main constitutions with up to 25-35% and 55-65% of the total components in wackestone and packstone, respectively. Other grains include crinoids and peloids. Internal spaces between the grains are filled with micrite and with some sparry calcite (Fig. 6b, c). Geopetal structures also occur in some skeletons of the articulatedshells (Fig. 6b).

Type B shell bed

26In the DSB₁ and YSB₂, the microfacies are composed of packstone with abundant reworked Gigantoproductus shells (Fig. 6d, e). The shells are mostly disarticulated comprising 45-55% of the total components. Besides, crinoids, foraminifers and gastropods also occur around the shells. The spaces between the bioclasts are full of micrite, peloids and sparry calcite (Fig. 6d, e).

27Erosional surface as one common structure of tempestites (Flügel, 2004) is recognized in the internal DSB₁ (Fig. 6d). The erosional surface is characterized by irregular boundary between two different constitutions, with dark micrite in the lower part and abundant bioclasts and sparry calcite in the upper part (Fig. 6d). Besides, geopetal structures also occur in the articulated brachiopod shells (Fig. 6e).

Type C shell bed

28The microfacies of GSB₃ are comprised of grainstone with abundant highly broken Gigantoproductus shells cemented by sparry calcite (Fig. 6f). The shells are in contact with each other and sometimes coated by micrite, taking account for 50-60% of the total components. Other grains include crinoids, foraminifers, calcareous algae, peloids and oncoids (Fig. 6f).

4.2.3. Top of the shell beds

29The microfacies in the top part of the shell beds are characterized by micritic carbonates with few bioclasts (mudstone texture), and are present at the uppermost parts of the GSB₁ and GSB₃ (Fig. 6g, h). Bioclasts contain brachiopods and crinoids with up to 5-8% of the total components. Sparry calcite also occurs in the space between the bioclasts, but it is not abundant (Fig. 6g, h).

30Ripple bedding and parallel lamination are common characteristics at the top of tempestites (Flügel, 2004). These sedimentary structures were identified in the GSB₁ and GSB₃ (Fig. 6g, h). Ripple bedding occurs in the mudstone at the uppermost part of the GSB₃ that is composed of grainstone (Fig. 6g). It is represented by ripple boundaries between different compositions, including more micrite, micrite and sparry calcite, and more sparry calcite (Fig. 6g). Parallel lamination is present in the mudstone at the uppermost part of the GSB₁, comprised of wackestone and packstone (Fig. 6h).

5. Discussion

5.1. Mechanism of the shell bed formation

31Mechanisms of shell accumulations in sedimentary rocks have been shown by a number of workers who have proposed diverse origins (Kidwell et al., 1986), including biologic origin (e.g. Kidwell, 1982), sedimentologic origin (e.g. storm surges (Aigner, 1979, 1985), currents (Futterer, 1978; Wilson, 1982), relative sea-level changes (Dattilo et al., 2012) and sedimentation changes (Kidwell, 1985)) and diagenesis (e.g. Wanless, 1979). In this study, multiple lines of evidence suggest that the accumulation of shells in Gigantoproductus shell beds is related to winnowing and transporting driven by storm surges, which is the principle agent of shell accumulation (Aigner, 1985; Flügel, 2004). First, the taphonomy of Gigantoproductus shells is usually characterized by disarticulation, convex-up and high fragmentation (Figs 3, 5), which are obvious characteristics in storm shell beds (Jeffery & Aigner, 1982; McFarland et al., 1999; Butts, 2005; Jin et al., 2013). Second, the occurrences of sedimentary structures of tempestites in the shell beds, including sharp and erosional base, internal erosional surface and uppermost parallel lamination and ripple bedding (Fig. 6), also indicate that they were formed under strong hydrodynamic energy triggered by storms. Third, different and distinct sedimentary facies were developed in the shell beds, which are one distinct feature of tempestites and absent in the shell beds formed by relative sea-level changes (Dattilo et al., 2012). At the base of the Gandongzi section, articulated and convex-down shells with much micrite, low fragmentation and parallel lamination in the mudstone of its uppermost part dominate the GSB₁, suggesting that it is a distal tempestite (Aigner, 1985; Flügel, 2004) (Figs 4a, 5a, 6h). In the upper Gandongzi section, the GSB₃ is characterized by high-breakage shells in grainstone and ripple bedding in the mudstone at the uppermost part, implying it is a proximal tempestite (Aigner, 1985; Flügel, 2004) (Figs 4c, 5c, d, 6f, g). In the Yashui and Duanshan sections, the YSB₂ and DSB₁ are composed of disarticulated and convex-up shells in packstones, indicating they occur between the proximal and distal tempestites (Figs 4b, 5b, 6d, e). Furthermore, during the Viséan to Serpukhovian, the epicontinental sea of South China was surrounded by Yangtze Old Land from north and west and Cathaysia Old Land in the east (Fig. 1c). Such a great bay setting is also suitable for the development of tempestites, which is similar to the Silurian case in northern Guizhou, South China (Li & Rong, 2007).

5.2. Palaeoenvironmental implications

32Several storm shell beds have been documented in the United States and southwest England in the Mississippian (Jeffery & Aigner, 1982; Butts, 2005). In these shell beds, the shells are characterized by different taphonomic types varying from articulated, convex-down and low fragmented shells to disarticulated, convex-up and high-breakage shells, which indicate that they are formed under low and high water energy respectively, driven by storms (Jeffery & Aigner, 1982; Butts, 2005).

33Similar to the other Mississippian storm shell beds, the late Viséan to Serpukhovian Gigantoproductus shell beds in South China also have different shell types in various sedimentary facies, implying different burial environments (Figs 4-6). At the base of the Gandongzi section, the GSB₁ includes mostly articulated and convex-down shells with low fragmentation in wackestone and packstone (Figs 5a, 6b, c), which is similar to the shell bed in the United States with in situ shells deposited in very low energy under the storm wave-base (Butts, 2005). However, the occurrences of disarticulated and fragmented shells with sparry calcite between them in the GSB₁ suggest that it was buried around the storm wave-base (Figs 5a, 6b, c). At the upper Gandongzi section, the GSB₃ contains highly fragmented shells in grainstone (Figs 5c, d, 6f), implying they were formed under very strong water energy above the fair-weather wave-base (Dattilo et al., 2012). At the Yashui and Duanshan sections, the YSB₂ and DSB₁ shell beds are mainly composed of disarticulated and convex-up shells with medium fragmentation in packstones (Figs 5b, 6d, e), indicating a relatively high hydrodynamic energy between the storm wave-base and the fair-weather wave-base (Butts, 2005). From the late Viséan to Serpukhovian, widely glacial deposits developed on the Gondwana continent (Isbell et al., 2003, 2012; Fielding et al., 2008), which are similar to the glacial distribution pattern in the Late Ordovician, early Silurian and recent times (Jin et al., 2013). Hence, hurricanes between the polar and tropical areas, which are similar to modern times (Jin et al., 2013) (Fig. 7a), would occur during late Viséan and Serpukhovian, and then induce the formation of the brachiopod storm shell beds in South China.

34Figure 7.(a) Modern frequency and intensity map of hurricane tracks (from National Oceanic and Atmospheric Administration, 2011). H1-H5: Category 1-5 hurricanes; TS: Tropical storm; TD: Tropical depression. (b) Location of amalgamated shell beds and non-amalgamated shell beds in South China (red solid circle) and northern England (green solid circle) respectively, hurricane and hurricane-free zones and palaeo-latitudes (blue dashed lines) during the late Viséan to Serpukhovian.

5.3. Palaeogeographical implications

35Nowadays, tropical hurricanes are usually absent within 10° north and south of the equator due to the weak Coriolis force (Jin et al., 2013). In contrast, strong hurricanes or cyclones chiefly occur between latitude 10° and 30° on both sides of the equatorial zone (Jin et al., 2013). Consistent with the present day situation, a hurricane-free zone was also constrained within latitude 10° on each side of the equator in the United States and Greenland during the late Ordovician, where non-amalgamated brachiopod shell beds were developed (Jin et al., 2013). Whereas, hurricane zone was present between latitude 10° and 30° on both of the equator in South China and United States during the late Ordovician and early Silurian respectively, with amalgamated shell beds formed (Li & Rong, 2007; Jin et al., 2013).

36On palaeogeographical maps of the Viséan to Serpukhovian times, different positions have been proposed for the SCB (e.g. Scotese and McKerrow, 1990; Golonka et al., 1994; Stampfli & Borel, 2002; Blakey, 2011). Overall, the SCB was consistently located very near the equator, but its precise location was still unclear. Because the Gondwana continent (south polar) was covered by prominent ice caps from the late Viséan to Serpukhovian (Isbell et al., 2003, 2012; Fielding et al., 2008) (Fig. 7b), it is plausible that this time had similar temperature gradient and hurricane pattern to the modern and late Ordovician periods when ice caps also widely occurred on the south polar area (Jin et al., 2013) (Fig. 7). Thus, it can be assumed that the modern hurricane pattern can be applied to the Mississippian. In Mississippian times, Gigantoproductus shell beds of northern England were characterized by all shells preserved in situ and convex-down (non-amalgamated shell beds), indicating that they occurred in hurricane-free zone within latitude 10° (Ferguson, 1978) (Fig. 7b). This hypothesis is consistent with the palaeogeographical position of northern England, which is very close to the equator (Scotese & McKerrow, 1990; Qiao & Shen, 2015). During the late Viséan to Serpukhovian, in South China, Gigantoproductus shell beds are featured by disturbed and amalgamated shells generated by storms, implying that the SCB was located between latitude 10° and 30° where strong hurricanes or cyclones chiefly occurred (Li & Rong, 2007; Jin et al., 2013) (Fig. 7b). On the first view the position of the SCB in the reconstruction of the aforementioned palaeogeographical studies seem to be reasonable. However, precisely locating the palaeo-latitudes of the SCB and the boundary between hurricane and hurricane-free zones needs the further study of taphonomic types of the storm shell beds located in the same latitudes of the other areas.

6. Conclusions

37(1) Late Viséan to Serpukhovian storm shell beds of Gigantoproductus are reported for the first time in the Yashui, Duanshan and Gandongzi sections in South China. The shell beds have the characteristics of tempestites, including sharp and erosional base, internal accumulations of amalgamated shells with erosional structure, and parallel lamination and ripple bedding structures in the uppermost part of the shell beds. Four microfacies types are identified in the shell beds, which are wackestone, packstone and grainstone, and mudstone in the uppermost part of the shell beds.

38(2) Three taphonomic and sedimentologic types are differentiated for the shell beds. Type A majorly comprises articulated and convex-down shells with low fragmentation in wackestone and packstone, which are developed in distal tempestites under weak hydrodynamic energy around the storm wave-base. Type B is dominated by disarticulated and convex-up shells with medium fragmentation in packstone that are present between proximal and distal tempestites in medium water energy between the storm wave-base and fair-weather wave-base. Type C mainly consists of highly fragmented shells in grainstone, formed in proximal tempestites with strong water energy above the fair-weather wave-base.

39(3) Shell accumulation of the shell beds is caused by winnowing and transporting driven by storm-induced bottom flows, evidenced from the amalgamated shells, basal and internal erosional structures, uppermost parallel lamination and ripple bedding structures, and development of proximal and distal tempestites.

40(4) During the late Viséan to Serpukhovian, the occurrences of storm shell beds in South China reflect that the South China Block was located in hurricane zone between latitude 10° and 30° during this time. The climatic gradient between equatorial and polar regions should have been important with ice caps on the Gondwana continent.

7. Acknowledgements

41This manuscript was greatly improved from the comments by Axel Munnecke (Erlangen) and Bernard Mottequin (Brussels). We would like to sincerely thank Prof. Zhuoting Liao of Nanjing Institute of Geology and Paleontology for his help in the fieldwork and identification of brachiopods, Prof. Xianghe Wu for his identification of foraminifers, and Dr. Jitao Chen for his valuable discussion. This work was financially supported by National Natural Science Foundation of China (grant Nos.: 41290260, 41290262), the Strategic Priority Research Program (B) of the Chinese Academy of Sciences (XDB18030400) and the Ministry of Science and Technology Foundation Project.

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100Manuscript received 07.09.2015, accepted in revised form 16.12.2015, available on line 13.05.2016.

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