Advertisement

Palaeobiodiversity and Palaeoenvironments

, Volume 99, Issue 1, pp 129–142 | Cite as

Hangenberg Black Shale with cymaclymeniid ammonoids in the terminal Devonian of South China

  • Meiqiong Zhang
  • R. Thomas Becker
  • Xueping MaEmail author
  • Yubo Zhang
  • Pu Zong
Original Paper
  • 128 Downloads

Abstract

The Hangenberg Crisis at the end of the Devonian is marked by a sudden global mass extinction (main Hangenberg Event), which was especially severe for ammonoids. Among the order Clymeniida, only the cymaclymeniids survived for a short time. We report the first discovery of Postclymenia cf. evoluta in South China in equivalents of the Hangenberg Black Shale (the regional Changshun Shale) at the Jiarantang section in Guizhou. The South China plate was far away and completely different from the Euramerica continent, where the Hangenberg Event/Crisis was first recognised. The presence of similar ammonoids as in contemporaneous beds of the Rhenish Massif, Germany, suggests close faunal relationship through the Palaeotethys Ocean. It agrees with a sudden spread of opportunistic extinction survivors with the initial Hangenberg Transgression. The regional facies and faunal succession at Jiarantang confirms previous concepts of a eustatically driven, significant transgressive-regressive couplet in the lower/middle crisis interval. The near-global distribution of cymaclymeniid survivors shows that their extinction at the end of the extended crisis interval must have been caused by a so far neglected, small-scale global extinction event in the open marine realm.

Keywords

Hangenberg Crisis Changshun Shale Ammonoids Guizhou Famennian 

Introduction

The end-Devonian bio-crisis, which has often been referred to as the Hangenberg Event, represents one of the major Phanerozoic global extinction intervals (e.g. Walliser 1984; Caplan and Bustin 1999). It shows extinction patterns and magnitudes as in the scale of the well-known “Big Five” (Kaiser et al. 2016). During the polyphase Hangenberg Biocrisis (see Kaiser et al. 2011), ammonoids suffered severe extinctions, especially during its initial and main phase (e.g. Price and House 1984; Becker 1993a, b, 1996; Korn 1993, 2000; House 1993). A species-level extinction rate of 87% was noted at the base of the Hangenberg Black Shale and its global equivalents (Kaiser et al. 2016) and no species at all is known to have survived through all of the extended biocrisis time (Becker et al. 2016a). Nevertheless, three lineages of goniatites (Mimimitoceras s.l., Sporadoceras, one tornoceratid genus) and two cymaclymeniid genera, Postclymenia and Cymaclymenia, are currently known to have survived the initial, anoxic Hangenberg Event (e.g. Kaiser et al. 2016; Klug et al. 2016). For overviews of D/C boundary biozonations, extinctions, sea-level changes, glaciations, isotope excursions, and many other aspects of the global Hangenberg Crisis, the reader is referred to the recent reviews by Becker et al. (2016a), Kaiser et al. (2016), and Lakin et al. (2016).

During the Upper Devonian, the South China plate was on the east side of the Palaeotethys Ocean, which was quite distant from the Euramerica continent (Fig. 1). Equivalents of the Hangenberg Black Shale are widespread in the pelagic facies in South China (e.g. Bai et al. 1994; Su et al. 1988). However, no ammonoid fossils have ever been documented from this interval. Here, we report the first discovery of the ammonoid Postclymenia from the Changshun Shale (equivalent strata of the Hangenberg Black Shale) in the Jiarantang section of Guizhou, South China.
Fig. 1

Location of the Jiarantang section and other important localities mentioned in the text. (a) Global geographic reconstruction around the Devonian–Carboniferous boundary, modified from Scotese (2001), with major locations of cymaclymeniid occurrences during the Hangenberg Event Interval (circled). (b) Index map showing the studied region in China. (c) Lithofacies and palaeogeographical map of South China in the Famennian (modified after Hou 1991), showing localities of various lithofacies mentioned in the text

Global record of Hangenberg Crisis survivor cymaclymeniids

Cymaclymeniids of the transgressive and often anoxic pulse of the Lower Crisis Interval (sensu Kaiser et al. 2016) have first been recorded from the Ardennes (Frech 1897; Delepine 1929; Austin et al. 1970) and then from many localities of the northern Rhenish Massif of Germany, such as Riescheid near Wuppertal-Barmen (Paeckelmann 1922), Wuppertal-Elberfeld (Mirker Hain and Am Haken Brickwork Quarry, Paeckelmann 1922; Schmidt 1924; Schindewolf 1926), Oberrödinghausen (Schindewolf 1937; Paproth and Streel 1970; Luppold et al. 1994; Becker et al. 2016a), the Bilstein Cave near Warstein (Korn 1981), Apricke (Paproth and Streel 1982), Oese (Paproth and Streel 1982; Korn 1991; Luppold et al. 1994; Becker et al. 2016a), Hasselbachtal (Luppold et al. 1994), and Drewer (Becker et al. 2016b). These occurrences were reported under different names, from cf. Pseudoclymenia (in Schmidt 1922) to Postclymenia evoluta Schmidt, 1924, Cymaclymenia camerata Schindewolf, 1923a (in Schindewolf 1923b, 1923c, 1926) to Cyma. euryomphala Schindewolf, 1937 (see also Korn 1981), Striatoclymenia euryomphala (in Paul 1939), and Cyma. evoluta (in Korn 1988, 1991). At present, all these Rhenish occurrences are thought to belong to just one crisis opportunist, Postclymenia evoluta. Unfortunately, the poor preservation prevents a detailed morphometric analysis (Price and Korn 1989). It has also been widely overlooked that Paeckelmann (1922, p. 284) emphasised the presence of two Postclymenia species in the Am Haken Brickwork Quarry and that Schindewolf (1926, p. 97) re-assigned one of these, the more involute form, to Cyma. striata. Therefore, the survival of two cymaclymeniid groups was postulated very early in research history but not really documented.

The extinction of most ammonoid groups at the base of the Hangenberg Black Shale defines the Cymaclymenia (now Postclymenia) evoluta Zone sensu Becker (1988) or Postclymenia Genozone (Upper Devonian = UD VI-E, Becker 1993a; Becker et al. 2016a). However, the type-level of Postclymenia evoluta Schmidt, 1924, lies at its Drewer type-locality below, in the slightly older Drewer Sandstone, not in the Hangenberg Black Shale (Schmidt 1922; Schindewolf 1923b, 1923c; Korn 1981, 1988, 1991; Price and Korn 1989). The Drewer Sandstone falls in the higher part of the pre-event Wocklumeria Genozone (UD VI-D), just below the entry of Epiwocklumeria applanata (Wedekind, 1918), which defines in the Rhenish Massif and Poland an upper or applanata Subzone (Becker and House 2000; UD VI-D2).

Postclymenia occurs also widely (in more than a dozen localities) in the more neritic uppermost Famennian of the northwestern Rhenish Massif, in crinoidal limestone and grey or greenish marls at the top of the Velbert Formation (“Etroeungt”; Schmidt 1924; Bärtling and Paeckelmann 1928; Paul 1938, 1939; Conil and Paproth 1968; Price and Korn 1989; Brauckmann 1990). The correlation of these faunas with the more eastern occurrences is not straight forward. Since “Striatoclymenia euryomphala” has been recorded from several levels in the Ratingen-Velbert region, and partly in association with a very rich and fully oxygenated benthic assemblage (e.g. Paul 1939), it is likely that there are regional Postclymenia-bearing equivalents of both the Drewer Sandstone (upper UD VI-D) and Hangenberg Black Shale (UD VI-E) levels. There is evidence for the presence of forms with different umbilical width at different localities (e.g. Paul 1938: pl. 4, fig. 2 versus Paul 1939: pl. 40, fig. 3). Unfortunately, most of the old outcrops have disappeared and cannot be re-sampled.

The Rhenish Hangenberg Black Shale faunal level (UD VI-E) with survivor cymaclymeniids has subsequently been traced in a range of other countries but not yet in South China. There are records from the uppermost Cleveland Shale (0.6–1.5 m below its top) of Ohio (House et al. 1986: localities 3-5), Thuringia (Bartzsch et al. 1998: Breternitz East), the Montagne Noire (southern France, Kaiser et al. 2009: p. 113), the Maider Basin of southern Morocco (Klug et al. 2016), and recently from the Urals (based on collections kindly shown by Y. Gatovsky in 2016). According to supposedly associated conodonts and miospores (Xu et al. 1990), a corresponding richer fauna occurs in the distant, palaeogeographically isolated Junggar Basin of Xinjiang (Zong et al. 2015: Cymaclymenia-Mimimitoceras” Assemblage from Emuha, Unit 2). This fauna and its precise age require further research.

A younger Postclymenia species, Post. nigra (Korn, 1991) (see discussion below for the inclusion of this species in Postclymenia), occurs at Drewer together with Post. evoluta above the Hangenberg Black Shale and Hangenberg Sandstone equivalent (Korn 1991). Both were collected as three-dimensionally preserved specimens from black nodules in the main Acutimitoceras (Stockumites) Genozone (UD VI-F). They were associated with early protognathodid conodonts (Pr. meischneri and Pr. collinsoni in Bed 97; Pr. kockeli in Beds 99/100; Korn et al. 1994), and, therefore, correlate partly with the Lower Stockum Limestone sensu Becker et al. (2016a, p. 359). Youngest (UD VI-F) cymaclymeniids are also known from other Rhenish units and localities, such as the main oolites of the Seiler Conglomerate near Iserlohn (Gallwitz 1928, p. 498), Upper Stockum Limestone of Müssenberg sensu Becker et al. (2016a, p. 361) (Korn 1989: Cyma. striata (Münster, 1832)), and the greenish-grey Hangenberg Shale of Oese (Becker et al. 2016a: Postclymenia sp.). They correlate partly with occurrences in Lower Stockum Limestone equivalents of southern Morocco (Lalla Mimouna South, kockeli Zone, Post. evoluta in Korn et al. 2004, 2007; subsequently re-named as Post. calceola Korn in Klein and Korn, 2014). Cymaclymeniids were also mentioned (but not described) together with acutimitoceratids from the oncolitic marker unit within the Leatham Member (Pilot Shale) of Utah (Feist and Petersen 1995: Cymaclymenia sp.). Elsewhere in the Great Basin, this unit lies above the “Conchostracan Shale”, a clear Hangenberg Black Shale equivalent with mass occurrences of the bivalve Guerichia (field observations by RTB, see Becker et al. 2016a). Cymaclymeniids from dark-grey, laminated shales of the uppermost Famennian Tercenas Formation of South Portugal (Oliveira et al. 1986) are probably not from the Hangenberg Crisis Interval but older, since a second locality of that unit yielded pre-extinction clymeniid genera, such as Linguaclymenia and Cyrtoclymenia (Korn, 1997).

Our new record from South China widely increases the geographic record of cymaclymeniid ammonoid survivors during the Hangenberg Crisis. It underlines a rapid spread triggered by the short-term, eustatic Hangenberg Transgression (e.g. Becker 1993b; Bless et al. 1993; Kaiser et al. 2016), which was previously evident from North African and North American records, where postclymeniids do not occur in immediate pre-crisis beds. The near-global, low to middle palaeolatitude distribution of Postclymenia in the terminal Devonian makes its subsequent sudden disappearance at the end of the extended Hangenberg Crisis Interval, when the other ammonoid survivor group, the Prionoceratidae (Goniatitida) re-diversified and flourished, enigmatic. The Cymaclymeniidae and Prionoceratidae co-existed since early in the upper Famennian (UD IV-B) and without evidence of general differences in their distribution and abundance, or for direct competition between both groups. This emphasises our current poor understanding of survivor extinctions at the end of first-order global biocrises.

The Jiarantang Devonian–Carboniferous boundary interval

The Jiarantang section lies approx. 100 km southeast of the well-known Muhua area (Fig. 1). It was located in the transition zone between the semi-restricted platform and the intraplatform basin facies. Feng (1977) first reported the section, on the basis of a previous geological survey, and with a description of the first Syringothyris brachiopod fauna discovered in South China.

The local Famennian sequence is about 250 m thick, composed of subordinate thin-, mostly medium- to thick-bedded, compact/dense, argillaceous, or dolomitic limestones, which used to be called the Yaosuo Fm. (deposits of a shallow water semi-restricted platform environment), or, later, the Daihua Fm. (= Wuzhishan Fm., deposits of a deeper water environment). In fact, the Famennian sequence at Jiarantang, especially the upper part, is most similar to deposits of a marginal platform environment, the Rongxian Formation (Fig. 2(a): thick- to massive dolomitic limestone), a term, which was first introduced to Guizhou by Wang (1997). Overlying the Rongxian Formation is the Changshun Shale (Fig. 2(c)), a black shale layer of ca. 1.5 m thickness, which is reported here for the first time from this section. It yielded relatively common cymaclymeniids (Postclymenia cf. evoluta) and subordinate bivalves and brachiopods. The overlying Gedongguan Bed, alternating shales and bioclastic limestones of various thicknesses (Fig. 2(c) including a very thin lens below and a main thicker lens above), is about 0.4 m thick. The “Wangyou” and “Muhua” formations (undifferentiated) are composed of thin- to thick-bedded, bioclastic limestones that are overlain by a suite of cherts and siliceous shale (Fig. 2(a)). A few Syringothyris specimens (Fig. 2(b)) have been found in loose bioclastic limestone slabs from the interval above the Changshun Shale, which probably represent a newly emergent brachiopod fauna after the Hangenberg Crisis (see also Zong and Ma 2012).
Fig. 2

Lithological succession and some characteristic fossils of the Devonian–Carboniferous boundary interval of the Jiarantang (ae) and Shijia (f) sections. a Overview of the lithological sequence; circled person (ca. 1.7 m tall) at lower central right as scale. b Bioclastic limestone of the post-Hangenberg Event interval showing the cardinal area of the brachiopod Syringothyris. c Close view of the Changshun Shale and its overlying sequence; black solid-circled letters D and E indicate corresponding position of conodont samples XSJ15-1 and XSJ-1, respectively. d-1 Oral view of Protognathodus meischneri. d-2. Oral view of Siphonodella praesulcata, strongly transitional towards S. sulcata.e Oral view of Protognathodus kockeli (white arrows on right platform indicate two nodes). f Succession of lithological units after Bai et al. (1994), with the “Gedongguan Bed” divided herein

Nomenclatural note: The Changshun Shale of Wang and Yin (1984), which is a marl and shale layer in the Muhua area, corresponds to the lower part of the Gedongguan Bed of Hou et al. (1985). The upper part of the Gedongguan Bed of Hou et al. (1985) is composed of marl/shale and lenses of limestones. The use of the term Gedongguan Bed is restricted here to the upper part of its original definition.

Two conodont samples were collected. Sample XSJ-1, from a level 0.1 m above the top of the Gedongguan Bed, includes the conodonts Bispathodus aculeatus aculeatus, Protognathodus kockeli, Neopolygnathus communis communis, and others. Protognathodus kockeli is a post-Hangenberg Event (Black Shale) species and has a stratigraphic range from the Pr. kockeli Zone (= Upper Si. praesulcata Zone; Kaiser et al. 2009) up to the lower part of the Lower Si. crenulata Zone (Corradini et al. 2017); the two Pr. kockeli specimens obtained from this sample are both morphologically less advanced than the holotype. One specimen possesses four nodes in a row on one side and two nodes on the other side that are not restricted to one strict row (Fig. 2(e)). In light of the underlying (Devonian) Postclymenia-bearing Changshun Shale, this sample is probably within a range from the Pr. kockeli Zone to the Si. sulcata Zone.

Sample XSJ 15-1, from a level ca. 0.75 m above the top of the Gedongguan Bed, includes an advanced Siphonodella praesulcata with a platform curvature of ca. 13.5° that is strongly transitional towards Si. sulcata (Fig. 2(d-2), see morphometrics in Flajs and Feist 1988), Protognathodus meischneri (Fig. 2(d-1)), Bispathodus aculeatus aculeatus, “Pandorinellina” n. sp. (sensu Hartenfels, 2011), and Neopolygnathus communis communis. This assemblage is not reliably age diagnostic in the Devonian–Carboniferous boundary interval (Si. praesulcata to Si. sulcata zones). The spathognathodids and polygnathid crossed the Devonian–Carboniferous boundary. However, Pr. meischneri occurs in South China mostly in the Pr. kockeli Zone, e.g. in the Gedongguan and Limushan sections (Hou et al. 1985: associated with the first occurrence of Pr. kockeli in the former), in the Lali section (Ji and Ziegler 1993: in the upper part of the 2 m thick Tangkou Mbr right below the first occurrence of Si. sulcata), in the Nanbiancun II, III, and IV sections (Yu 1988: associated with or above the first occurrence of Pr. kockeli, whereas Ji et al. (1989) assigned the same interval to the basal Carboniferous), or in the basal Carboniferous, e.g. in the Huangmao section (Bai et al. 1994, fig. 6-2: 0.2 m above the D-C boundary). The species was only rarely found below the Hangenberg Black Shale equivalent, e.g. in the Muhua II (Hou et al. 1985) and Dapoushang (= Daposhang) sections (Ji et al. 1989). Considering the general occurrences of Pr. meischneri in South China and the morphological nature of Si. praesulcata, this sample may have a similar time range to that of sample XSJ-1.

Overall, the above fossil data support the ammonoid evidence that the Jiarantang succession represents a Devonian–Carboniferous boundary sequence and that the Changshun Shale in this section is an equivalent of the Hangenberg Black Shale of Europe.

Macrofauna of the Changshun Shale in the Jiarantang section

In the Changshun Shale, ammonoid impressions are common (Figs. 3 and 4: all specimens are housed in the Department of Geology, Peking University); brachiopods (Fig. 3(h, i)) and bivalves (Fig. 3(f)) are rare. In addition, some trace fossils are also present (Fig. 3(g)).
Fig. 3

Megafossils from the Changshun Shale of the Jiarantang section. a–ePostclymenia cf. evoluta showing shell outlines, growth ornaments, and sutures (PUM 15034PUM 15037), with non-cymaclymeniid, rather simple sutures in PUM 15036 (image c), possibly due to corrosion before its burial. f Internal mould of a bivalve (left) and Postclymenia cf. evoluta (right, PUM 15033a, see Fig. 4j). g A burrow filling (PUM 15040). h, i Ventral valve cast (PUM 15038), viewed ventro-anteriorly, and dorsal valve cast (PUM 15039), viewed dorsally (associated with a Postclymenia cf. evoluta), of the brachiopod Semicostella? sp. The 10 mm scale bar in the upper middle is for all images except for the enlargement b and the trace fossil g

Fig. 4

Postclymenia cf. evoluta from the Changshun Shale of the Jiarantang section, all lateral views of mould specimens. a PUM 15026. b, c Split halves (PUM 15027a and PUM 15027b). d PUM 15028. (e) PUM 15029. (f) PUM 15030. g, h Showing sutures of PUM 15031. i. PUM 15032. j–l Split halves and growth ornaments enlarged (PUM 15033a and PUM 15033b). m Suture of specimen PUM 15031. The 10 mm scale bar is for all images, except for the two enlargements

Postclymenia Schmidt, 1924 (emend.)

Discussion: Giving credit to H. Schmidt, the genus Postclymenia was first mentioned and briefly explained in a footnote by Paeckelmann (1922, p. 284). However, in the absence of a type-species designation, the name remained a nomen nudum. The genus was then formally erected by Schmidt (1924). He assumed that the species name Clymenia evoluta, which had only appeared without any explanation in a footnote in Frech (1897, p. 179), was valid. This is not the case (Price and Korn 1989) and, therefore, Schmidt became the author of Postclymenia evoluta. The assumed distinction between Postclymenia and Cymaclymenia by Schmidt (1924) was rejected by Schindewolf (1926) based on the analysis of a topotype collection. Therefore, the genus was abandoned for many subsequent decades. Eventually Postclymenia was resurrected by Korn and Klug (2002), who briefly justified this by its supposedly much more asymmetric flank lobe (see also Korn et al. 2004). However, this feature is only distinctive in the Moroccan Post. calceola, while the flank lobe in the Rhenish type-species does not differ from that in many Cymaclymenia species. This is clearly visible in the suture illustrations of Schmidt (1924: pl. 8, fig. 21), Schindewolf (1926: fig. 2b), Korn (1981: fig. 21), Price and Korn (1989: fig. 12), Korn et al. (1994: fig. 16A), and Becker et al. (2016a: fig. 5.2). Therefore, Zong et al. (2015) drew attention to differences in the growth ornament between Postclymenia and Cymaclymenia. The first is here re-defined by concavo-convex growth lines with a lateral sinus that extends in full curvature (without interruption by a low salient or straight/radial interval) right to the umbilical seam. In median-sized to mature Cymaclymenia (= Striatoclymenia and Miroclymenia) there is an incipient to well-developed growth line salient on the lower flanks (see illustration of holotype of the type-species, Cyma. striata, in Korn 1981: fig. 11a, and the ornament in many other forms in Korn 1981, Nikolaeva and Bogoslovskiy 2005, and Klein and Korn 2014). In this revised sense, Postclymenia includes also Cyma. camerata (= Cyma. warsteinensis Korn in Clausen et al. 1979), Cyma. curvicosta Lange, 1929, Cyma. nigra Korn, 1991, and Post. calceola. The genus originated long before the Hangenberg Biocrisis in the upper Famennian (Dasbergian of German nomenclature, UD V; Schindewolf 1923c). It probably gave rise to some Russian and Chinese genera. These share the same course of growth ornament but differ in the presence of an additional median ventral lobe (Laganoclymenia, Kazakhoclymenia), ventral band (Laminoclymenia), or marked ventrolateral furrows (Auritoclymenia). Procymaclymenia differs from Postclymenia in its simpler, not pointed flank lobe and fully biconvex, Cymaclymenia-type ornament. Rodachia is characterised by the reduction of the ventral sinus of growth ornament.

Stratigraphic range: Upper Devonian (UD) V-B to VI-F (zonal key after Becker and House 2000).

Postclymenia cf. evoluta Schmidt, 1924

Description: Three Jiarantang specimens show sutures, but each with a somewhat different morphology. The dorsolateral saddle is short and the ventral one is very broad in PUM 15031 (Fig. 4(g, h, m)), while the dorsolateral saddle has a longer, straight (not curved) inner prong in PUM 15027 (Fig. 4(b, c)), where the ventral saddle is not as wide. This seems to be related to different compaction during flattening and may explain why the sutures look rather different in PUM 15035 (Fig. 3(c)), variably with or with only an incipient dorsolateral saddle, creating sutures resembling Genuclymenia, the middle Famennian ancestor of cymaclymeniids. PUM 15035 was probably partially corroded on the seafloor before it was buried and flattened. Based on PUM 15031 (Fig. 4(h)), the adventitious flank lobe is only moderately asymmetric. Fig. 3(b) shows the coarse wrinkle layer in PUM 15034 as it is known from some Moroccan postclymeniids (see Klug et al. 2016: fig. 4h). PUM 15034 (Fig. 3(a)) and PUM 15033 (Fig. 4(j–l)) display the concavo-convex growth ornament (but without distinctive lirae). The umbilical width/diameter (uw/dm) ratio varies at 1015 mm dm (PUM 15033 and PUM 15031) between 0.34 and 0.37 and decreases to 0.30 (PUM 15029) to 0.33 (PUM 15030) between 20 and 25 mm dm. The estimated whorl expansion rate (WER) fluctuates between 1.9 and 2.0, based on PUM 15029 and PUM 15030.

Discussion: Based on the poorly preserved type population from the Drewer Sandstone, Post. evoluta is characterised by a uw/dm ratio of 0.33 to 0.35 between 20 and 40 mm dm and WER of ca. 1.9. This is confirmed by better preserved material from the overlying prorsum Zone (Korn 1991), which additionally give a whorl width/whorl height (ww/wh) ratio of ca. 0.70 at ca. 20 mm dm. Specimens from the Hangenberg Black Shale of Oese and Oberrödinghausen partly show lower uw/dm ratios of only ca. 0.30 to 0.32 between 10 and 35 mm dm (e.g. Paproth and Streel 1970: pl. 24, fig. 4; Becker et al. 2016a: figs. 5.2 and 5.3; additional unpublished specimens), which may reflect their strong flattening and distortion. But it is best to identify such forms as Post. cf. evoluta. As emphasised by Korn (1991), all Sauerland specimens are characterised by very weak growth ornament.

Postclymenia nigra differs from Post. evoluta in its wider whorls (ww/wh ratio near 0.90 at ca. 20 mm dm), steep umbilical wall, and decreasing uw/dm ratios between 20 and 30 mm dm (from near 0.40 to 0.33; see measurements in Korn 1991). It has also smooth whorls without growth lirae. The lectotype of Post. camerata (here designated as the original of Schindewolf 1923a: pl. 17, fig. 6) is slightly more evolute than Post. evoluta (uw/dm = ca. 0.37 at 26 mm dm) and its whorls are somewhat higher (WER = ca. 2.2). In addition there are dense and regular growth lirae, while its ww/wh ratio (ca. 0.69) is not distinctive. The holotype of Cyma. warsteinensis, which also shows the characteristic lirae, is very similar to the Post. camerata lectotype with respect to uw/dm (ca. 0.35), ww/wh (0.69), and WER values (ca. 2.3). Therefore, the species is regarded as a subjective senior synonym (see also Korn and Klug 2002). Morphometric analyses will have to clarify whether other specimens that have been assigned to Cyma. camerata really belong to that species. This applies to Moroccan representatives (Becker et al. 2002; Post. cf. camerata of Becker et al. 2018a, 2018b) or additional material from Franconia (Price 1982). A cross-section figured by Korn (1981) from Reigern Quarry in the Rhenish Massif is too involute (uw/dm = 0.32 at ca. the same size as the camerata lectotype) and has too wide whorls (ww/wh = 0.87). It may present a related but thicker-whorled species with similarly high whorls (WER = 2.15) as in Post. camerata. Specimens from the pre-Hangenberg limestones of Nanbiancun (Ruan 1988), identified as Cyma. warsteinensis, have somewhat intermediate uw/dm (0.33 to 0.34) and ww/wh values (0.80 at ca. 25 mm dm) and show no evidence of regular growth lirae. This suggests relationships with Post. evoluta but the most complete specimen (Ruan 1988: pl. 65, fig. 4), may have a higher WER resembling Post. camerata. The presence of a possibly additional taxon in the more neritic facies of Guangxi has to be tested based on additional material and cross-sections. In any case, alleged Cyma. camerata from Russia (Nikolaeva and Bogoslovskiy 2005) are too involute for that species (uw/dm = 0.30 to 0.31) and they display a Cymaclymenia-type ornament that is straight on the lower flanks.

Postclymenia curvicosta is characterised by umbilical ribbing, the large-sized Post. calceola by its strongly asymmetric flank lobe. Mature individuals of the latter (> 40 mm dm) show a slight increase of WER (towards 2.1) and decrease of uw/dm ratios towards 0.30 to 0.35 (Klein and Korn 2014).

With respect to the lack of distinctive growth lirae and the shape of the flank lobe, the Jiarantang specimens are closest to the Rhenish Post. evoluta. The uw/dm ratio of only 0.30 to 0.33 at 22–25 mm dm and WER values agree with the flattened, contemporaneous Hangenberg Black Shale specimens of the Sauerland that should be called Post. cf. evoluta. Another match is the unusually short dorsolateral saddle (compare Becker et al. 2016a: fig. 5.2) but this may be related to similar distortion during the flattening.

The probably contemporaneous but poorly preserved cymaclymeniids from the top of the Cleveland Shale of Ohio are also similar. The most complete specimen (House et al. 1986, fig.4.14) displays Postclymenia-type concavo-convex growth ornament without lirae and an uw/dm ratio of ca. 0.31. However, the whorls seem to be slightly higher, with an estimated WER of ca. 2.2.

Specimens from the more neritic facies of the northwestern Rhenish Massif are partly very similar to Post. cf. evoluta (e.g. Paul 1939: pl. 40, fig. 3 and pl. 41, fig. 3). However, Paul (1938: p. 4, fig. 2) illustrated as Cyma. euryomphala a large form (without sutures) that has more than 70 mm dm and a wider umbilicus (uw/dm ca. 0.40) than any other illustrated postclymeniid. Such specimens indicate that our knowledge of the group is still incomplete.

Hangenberg Black Shale equivalents in South China

In South China there are a number of well-documented deeper water (intraplatform basin and “slope” facies) Devonian–Carboniferous (D–C) boundary sections (Figs. 1 and 5), where time and facies equivalents of the German Hangenberg Black Shale (the Changshun Shale) are more or less developed. These are Nanbiancun, Guangxi Province (a very thin, shaly parting, not exceeding 0.5 cm thickness; see Yu 1988), the Muhua area, Guizhou Province, including the Dapoushang and Muhua sections (Hou et al. 1984, 1985; Wang and Yin 1984; Ji et al. 1989; Bai et al. 1994; a 2–4 cm, sometimes up to 30 cm thick, dark grey shale to marl layer, the bentonite/tuff of Liu et al. 2012), Zhaisha, Guangxi (Ji et al. 1987; ca. 0.48 m thick, variably coloured mudstones and shales yielding only spores, which correspond to the whole Hangenberg Crisis (HC) interval of Kaiser et al. 2016), Huangmao, Guangxi (Bai et al. 1994; a 0.340.6 m thick interval of black carbonaceous shales of the HC interval, yielding the bivalve “Posidonia sp.” (now Guerichia) and a number of spore taxa), and Lali, Guangxi (Su et al. 1988; Ji and Ziegler 1993; a 2 m thick interval, Tangkou Mbr., that may be divided into the lower Changshun Shale (black carbonaceous shales) and the upper Gedongguan Bed (black to dark grey shales and mudstones intercalated with light grey limestone lenticles, bearing rare conodonts, such as Protognathodus meischneri and Neopolygnathus communis communis).
Fig. 5

Hangenberg Event related stratigraphic interval in various facies settings of South China. Data are from various sources: Lali - Ji and Ziegler (1993); Xiakou - Wang and Yin (1985) and Wang et al. (1987); Huangmao - Bai et al. (1994); Malanbian - Tan et al. (1987), with the spore from Steemans et al. (1996) and lithologies of the Malanbian Fm. modified from Qie et al. (2015); Muhua II - Hou et al. (1985); Muhua III - Bai et al. (1994) and Hou et al. (1985). Numbers on the right of the lithologic column indicate bed number in the original source reference

The presumed Hangenberg Black Shale equivalent is also present in the cherty basin facies of Guangxi, e.g. in the Shijia (= Bancheng) section (Bai et al. 1994, p. 54; Fig. 1). The D–C boundary is composed of Devonian Liujiang Fm. and Carboniferous Shijia Fm. (Fig. 2(f)). However, the whole Upper Devonian through Lower Carboniferous strata in the Shijia section was assigned to the Shijia Fm. (Yin 1997, p. 113) due to their uniform lithology (bedded cherts). The uppermost Liujiang Fm. consists of medium-bedded cherts. The Changshun Shale is a siliceous black shale unit of 25 cm thickness, yielding the bivalve “Posidonia” (now Guerichia; Bai et al., 1994). The “Gedongguan Bed” is composed of (dark) grey, thin-bedded silty cherts or siliceous siltstones intercalated with medium-bedded siliceous rock (Fig. 2(f)). The basal part of the Shijia Fm. consists of thin- (to medium-) bedded cherts.

Wang and Ji (2013) described a very thick succession of the Changshun Shale (in a wide sense) from the Huohua section in Ziyun County, Guizhou. A thin (20 cm) basal black shale with “Posidonia” (= Guerichia) is overlain by ca. 20 meters of siliceous shales and thin limestone bands. According to an anonymous reviewer, the limestone bands are restricted to the lowermost part of this 20-meter unit; the 20 m “shale” is in fact mainly composed of thin-bedded cherts, intercalating with very thin (12 cm) black shale, which is overlain by ca. 60 m of calcareous siltstones and calcarenites of the earlymiddle Tournaisian. In light of the above data, we can correlate the basal part of the 20 m thick unit with the Gedongguan Bed.

In the shallow water mixed carbonate and siliciclastic facies, such as the Malanbian section, Hunan (Fig. 5), the Hangenberg Crisis Interval may be present in the uppermost Menggong’ao Fm., a coarsening-upwards sequence of ca. 3.2 m, although its precise age cannot be determined due to the lack of index conodonts. Benthic fossils may be used as auxiliary markers; the brachiopod Cyrtospirifer (as well as related forms) most probably became extinct at the base of Si. praesulcataPr. kockeli Interregnum sensu Kaiser et al. (2009), e.g. in the Nanbiancun section (except for a single specimen in the Pr. kockeli = Upper Si. praesulcata Zone, see Yu 1988 and also Ji et al. 1989, which is here interpreted to be a reworked specimen) and the Xiakou section (Wang et al. 1987). The rugose coral Cystophrentis is commonly associated with cyrtospiriferid brachiopods in the uppermost Devonian in South China (e.g. in the Dushan area of Guizhou). Therefore, the disappearance of both Cyrtospirifer and Cystophrentis at the approximate same level is suggestive of the main Hangenberg Extinction level at the top of the praesulcata Zone (sensu Kaiser et al. 2009). The spore data give an inconsistent or contradictory result. Tan et al. (1987) found a number of spores in Unit 36 (Fig. 5), including Verrucosisporites nitidus, the index species of the LN Zone, whereas Steemans et al. (1996) suggested the upper part of the LV Zone (below the (Lower) Si. praesulcata Zone) based on size measurements of Retispora lepidophyta in Unit 36. However, they indicate in the meantime that the D–C boundary lies within the same unit or at the top of Unit 36. In the shallow water carbonate facies, the Hangenberg Crisis Interval clastic deposits (such as shale and siltstones/sandstones) may be missing, for example in the Xiakou section (Wang and Yin 1985; Wang et al. 1987: the “Middle Si. praesulcata Zone limestone” is directly overlain by “Si. sulcata Zone limestone”) and the Sujiaping section (Tan et al. 1987; Bai et al. 1994: the Devonian Cystophrentis- and Quasiendothyra-bearing grey bio-intraclastic calcisiltitic limestone is directly overlain by Carboniferous grey bio-intraclastic calcisiltitic limestone bearing the foraminifer Vicinesphaera angulata-Bisphaera malevkensis Assemblage of Wang 1987).

Apart from South China, Hangenberg Black Shale equivalents are also well developed in Tibet (lower part of Zhangdong Formation, Tulong Section, Liu et al. 2018), which belonged in the Devonian and Carboniferous to a different terrain/microcontinent.

Sea level changes during the Hangenberg Crisis interval

There are different opinions regarding the sea level changes of the Hangenberg Crisis Interval, including a (dramatic) sea level fall (e.g. Bai et al. 1994; Sandberg et al. 2002; Ji 2004) or a dramatic initial sea level rise and subsequent major sea level fall (e.g. Bless et al. 1993; Kaiser et al. 2011, 2016). The latter interpretation is supported by palynofacies data, with a significant rarity or restriction of miospores in the Hangenberg Black Shale and a subsequent rapid increase of terrestrial input (e.g. Higgs and Streel 1994; Marynowski and Filipiak 2007). The transgressive nature of the Hangenberg Black Shale was questioned by Bábek et al. (2016), who, however, did not clearly separate the different siliciclastic intervals within the polyphase Hangenberg Crisis Interval and who interpreted the increasing detrital proxies in a too simple way as a sign of general regression. However, it is long known that in offshore, pelagic carbonate settings, the decrease of bottom turbulence with sea-level rise enables the settling of detrital clay and fine silt, resulting in the deposition of transgressive shales and marls.

The lithological succession in the Jiarantang section is consistent with the pattern of a distinct sea level rise and subsequent fall. According to GBG (1965, p.38), the uppermost Rongxian Fm. in the study area is composed of grey medium- to thick-bedded limestones intercalated by dolomitic and oolitic limestones, which apparently represents deposits of a platform margin setting, probably with episodic shallowing. The Changshun Shale, with its sudden influx of abundant pelagic ammonoids and reduced turbulence that enabled the settling of fine, organic-rich mud, undoubtedly suggests a rapid sea level rise corresponding to the transgressive pulse of the Hangenberg Black Shale (Kaiser et al. 2016). The overlying Gedongguan Bed, mostly bioclastic limestones, probably deposited during a shortly following sea level fall, corresponding to the regressive phase of the Hangenberg Shale and Sandstone (Becker et al. 2016a; Kaiser et al. 2016). The Hangenberg Crisis Interval in the Lali section and in the Muhua area have a nearly identical lithological succession and reflect a similar process of sea level changes.

In the shallow water mixed carbonate and siliciclastic facies, the Hangenberg Crisis Interval is represented by a coarsening-up clastic sequence that ends with medium- to thick-bedded sandstones, e.g. in the Xikuangshan (Coen et al. 1996; our own observation) and Malanbian sections. Evidence for a sea level rise of the initial Hangenberg Crisis Interval is generally not visible or less evident, because of the general lack of index fossils. More importantly, the often thin, transgressive Lower Hangenberg Crisis Interval (represented by shale or marl units) may be missing in shallow water carbonate facies due to subsequent erosion during the subsequent sea level lowstand, for example in the Xiakou section of Wang and Yin (1985) and Wang et al. (1987), and in the Sujiaping (= Lijiaping) section of Tan et al. (1987) and Bai et al. (1994).

Conclusions

The discovery of relatively abundant Postclymenia cf. evoluta in Hangenberg Black Shale equivalents (Changshun Shale) of South China (Guizhou) has significant implications for our understanding of ammonoid palaeobiogeography and evolution, of regional patterns of the Hangenberg Crisis, and for the reconstruction of D–C boundary eustatic developments.

1. Since South China belonged to a completely different continent far away from Euramerica (Laurussia) and NW Gondwana (Morocco), the new record documents a global Postclymenia distribution in low to middle palaeolatitudes of the Hangenberg Crisis Interval.

2. The strong similarity with contemporaneous German Post. cf. evoluta indicates an event-controlled, very fast west-east spread of this opportunistic disaster species within the Palaeotethys, whilst differences between the closer southern Laurussia and northern Gondwana areas were more significant, since these regions harboured related but different Postclymenia species.

3. The intercalation of the Changshun Shale with pelagic ammonoids at Jiarantang between shallow-water, organic poor neritic limestones proves its transgressive nature, in an area without high terrestrial input.

4. The disappearance of globally widespread survivor clymeniids suggests that a so far neglected small-scale global extinction occurred at the end of the extended Hangenberg Crisis Interval (Pr. kockeli Zone). Since the recovery from the main Hangenberg Extinction had only just started, this event could not produce high extinction rates and can only be recognised if studies are done at the finest available time resolution.

Notes

Acknowledgements

This paper benefited from various topical discussions with Hou Hongfei (Institute of Geology, CAGS) and Liao Weihua (Nanjing Institute of Geology and Paleontology). Yin Bao’an (Guangxi Regional Geological Survey) and Tan Zhengxiu (Hunan Regional Geological Survey) were helpful during our fieldwork. Sven Hartenfels (WWU Münster) commented on the conodonts. This manuscript benefited from comments by Dieter Korn (Museum für Naturkunde, Berlin) and two other anonymous reviewers. The support of the National Natural Science Foundation of China (Grant 41290260) is also acknowledged.

Compliance with ethical standards

Conflict of interest:

The authors declare that they have no conflict of interest.

References

  1. Austin, R., Conil, R., Dolby, G., Lys, M., Paproth, E., Thodes, F. H. T., Streel, M., Utting, J., & Weyer, D. (1970). Les couches de passage du Dévonien au Carbonifère de Hook Head Island au Bohlen (D.D.R.). Les Congres et Colloques de l’Université de Liége, 35, 167–178 [in French with English summary].Google Scholar
  2. Bábek, O., Kumpan, T., Kalvoda, J., & Grygar, T. M. (2016). Devonian/Carboniferous boundary glacioeustatic fluctuations in a platform-to-basin direction: a geochemical approach of sequence stratigraphy in pelagic settings. Sedimentary Geology, 337, 81–99.CrossRefGoogle Scholar
  3. Bärtling, R., & Paeckelmann, W. (1928). Blatt Velbert, Nr. 2650. Erläuterungen zur Geologischen Karte von Preußen und benachbarten deutschen Ländern, Lieferung, 274, 1–109 [in German].Google Scholar
  4. Bartzsch, K., Hahne, K., & Weyer, D. (1998). Der Hangenberg-Event (Devon/Karbon-Grenze) im Bohlen-Profil von Saalfeld (Thüringisches Schiefergebirge). Abhandlungen und Berichte für Naturkunde, 20, 37–58 [in German].Google Scholar
  5. Bai, S. L., Bai, Z. Q., Ma, X. P., Wang, D. R., & Sun, Y. L. (1994). Devonian events and biostratigraphy of South China (pp. 1–303). Beijing: Peking. University Press.Google Scholar
  6. Becker, R. T. (1988). Ammonoids from the Devonian–Carboniferous Boundary in the Hasselbach Valley (Northern Rhenish Slate Mountains). Courier Forschungsinstitut Senckenberg, 100, 193–213.Google Scholar
  7. Becker, R. T. (1993a). Anoxia, eustatic changes, and Upper Devonian to lowermost Carboniferous global ammonoid diversity. In M. R. House (Ed.), The Ammonoidea: Environment, Ecology, and Evolutionary Change. Systematics Association Special Volume, 47, 115–163.Google Scholar
  8. Becker, R. T. (1993b). Analysis of ammonoid palaeobiogeography in relation to the global Hangenberg (terminal Devonian) and Lower Alum Shale (Middle Tournaisian) events. Annales de la Société Géologique de Belgique, 115, 459–473.Google Scholar
  9. Becker, R. T. (1996). New faunal records and holostratigraphic correlation of the Hasselbachtal D/C boundary auxiliary stratotype (Germany). Annales de la Société Géologique de Belgique, 117, 19–45.Google Scholar
  10. Becker, R. T., & House, M. R. (2000). Devonian ammonoid zones and their correlation with established series and stage boundaries. Courier Forschungsinstitut Senckenberg, 220, 113–151.Google Scholar
  11. Becker, R. T., House, M. R., Bockwinkel, J., Ebbighausen, V., & Aboussalam, Z. S. (2002). Famennian ammonoid zones of the eastern Anti-Atlas (southern Morocco). Münstersche Forschungen zur Geologie und Paläontologie, 93, 159–205.Google Scholar
  12. Becker, R. T., Kaiser, S. I., & Aretz, M. (2016a). Review of chrono-, litho- and biostratigraphy across the global Hangenberg Crisis and Devonian–Carboniferous Boundary. In R. T. Becker, P. Königshof & C. E. Brett (Eds.), Devonian climate, sea level and evolutionary events. Geological Society of London, Special Publications, 423, 355–386.  https://doi.org/10.1144/SP423.10.
  13. Becker, R. T., Hartenfels, S., Weyer, D., & Kumpan, T. (2016b). The Famennian to Lower Viséan at Drewer (northern Rhenish Massif). Münstersche Forschungen zur Geologie und Paläontologie, 108, 158–178.Google Scholar
  14. Becker, R. T., Aboussalam, Z. S., Hartenfels, S., El Hassani, A., & Baidder, L. (2018a). Bou Tchrafine – central Tafilalt reference section for Devonian stratigraphy and cephalopod succession. Münstersche Forschungen zur Geologie und Paläontologie, 110, 158–187.Google Scholar
  15. Becker, R. T., Aboussalam, Z. S., Helling, S., Afhüppe, L., Baidder, L., & El Hassani, A. (2018b). The world-famous Devonian mudmounds at Hamar Laghdad and overlying cephalopod-rich strata. Münstersche Forschungen zur Geologie und Paläontologie, 110, 188–213.Google Scholar
  16. Bless, M. J. M., Becker, R. T., Higgs, K., Paproth, E., & Streel, M. (1993). Eustatic cycles around the Devonian–Carboniferous boundary and the sedimentary and fossil record in Sauerland (Federal Republic of Germany). Annales de la Société Géologique de Belgique, 115, 689–702.Google Scholar
  17. Brauckmann, C. (1990). Oberdevon und Unterkarbon von Ratingen. In W. K. Weidert (Ed.), Klassische Fundstellen der Paläontologie (Vol. 2, pp. 49–58). Korb: Goldschneck Verlag, Korb [in German].Google Scholar
  18. Caplan, M. L., & Bustin, R. M. (1999). Devonian–Carboniferous Hangenberg mass extinction event, widespread organic-rich mudrock and anoxia: causes and consequences. Palaeogeography, Palaeoclimatology, Palaeoecology, 148, 187–207.CrossRefGoogle Scholar
  19. Clausen, C. D., Korn, D., & Uffenorde, H. (1979). Das Devon/Karbon-Profil am alten Schießstand bei der Bilstein-Höhle (Blatt 4515 Hirschberg, Warsteiner Sattel, Rheinisches Schiefergebirge). Aufschluss, Sonderband, 29, 47–68 [in German].Google Scholar
  20. Coen, M., Hance, L., & Hou, H. F. (1996). Papers on the Devonian–Carboniferous transition beds of central Hunan, South China. Mémoires de L’Institut Géologique de l’Université de Louvain, 36, 7–229.Google Scholar
  21. Conil, R., & Paproth, E. (1968). Mit Foraminiferen gegliederte Profile aus dem nordwest-deutschen Kohlenkalk und Kulm. Decheniana, 119(1/2), 51–94 [in German].Google Scholar
  22. Corradini, C., Spalletta, C., Mossoni, A., Matyja, H., & Over, D. J. (2017). Conodonts across the Devonian/Carboniferous boundary: a review and implication for the redefinition of the boundary and a proposal for an updated conodont zonation. Geological Magazine, 154(4), 888–902.CrossRefGoogle Scholar
  23. Delepine, G. (1929). Sur la présence de Cymaclymenia camerata Schind. dans la zone d’Etroeungt à Sémeries (nord de la France). Annales de Société géologique du Nord, 54, 99–103 [in French].Google Scholar
  24. Feist, R., & Petersen, M. S. (1995). Origin and spread of Pudoproetus, a survivor of the Late Devonian trilobite crisis. Journal of Paleontology, 69(1), 99–109.CrossRefGoogle Scholar
  25. Feng, R. L. (1977). Discovery of Syringothyris from Southern Guizhou and its significance. Acta Palaeontologica Sinica, 16(1), 53–58 [in Chinese with English abstract].Google Scholar
  26. Flajs, G., & Feist, R. (1988). Index conodonts, trilobites and environment of the Devonian–Carboniferous Boundary beds at La Serre (Montagne Noire, France). Courier Forschungsinstitut Senckenberg, 100, 53–107.Google Scholar
  27. Frech, F. (1897). Lethaea geognostica oder Beschreibung und Abbildung der für die Gebirgs-Formationen bezeichnensten Versteinerungen. I. Theil. Lethaea palaeozoica, 2. Band, 1. Lieferung (pp. 1–256, 30 pls., 3 maps). Stuttgart: Schweizerbart [in German].Google Scholar
  28. Gallwitz, H. (1928). Stratigraphische und tektonische Untersuchungen an der Devon–Carbongrenze des Sauerlandes. Jahrbuch der Preussischen Geologischen Landesanstalt, 48, 487–527 pl. 23.Google Scholar
  29. GBG (Geological Bureau of Guizhou) (1965). Report of Regional Geological Survey of People’s Republic of China—1:200,000 Geological Map Sheet (G-48-XXIV) of Dushan [in Chinese].Google Scholar
  30. Hartenfels, S. (2011). Die globalen Annulata-Events und die Dasberg-Krise (Famennium, Oberdevon) in Europa und Nord-Afrika – hochauflösende Conodonten-Stratigraphie, Karbonat-Mikrofazies, Paläoökologie und Paläodiversität. Münstersche Forschungen zur Geologie und Paläontologie, 105, 17–527 [in German with English summary].Google Scholar
  31. Higgs, K. T., & Streel, M. (1994). Palynological age for the lower part of the Hangenberg Shales in Sauerland Germany. Annales de la Société Géologique de Belgique, 116(2), 243–247.Google Scholar
  32. Hou, H. F. (1991). An outline of Famennian stratigraphy of South China. In Z. Y. Yang (Ed.), Stratigraphy and Paleontology of China (Vol. 1, pp. 49–69). Beijing: Geological Publishing House.Google Scholar
  33. Hou, H. F., Ji, Q., Xiong, J. F., & Wu, W. H. (1984). A possible stratotype of Devonian–Carboniferous boundary in Guizhou Province, South China. In E. Paproth & M. Streel (Eds.), The Devonian–Carboniferous Boundary. Courier Forschungsinstitut, Senckenberg, 67, 193–205.Google Scholar
  34. Hou, H. F., Ji, Q., Wu, X. H., Xiong, J. F., Wang, S. T., Gao, L. D., Sheng, H. B., Wei, J. Y., & Turner, S. (1985). Muhua sections of Devonian–Carboniferous boundary beds (pp. 1–272). Beijing: Geological Publishing House [in Chinese with English abstract].Google Scholar
  35. House, M. R. (1993). Earliest Carboniferous goniatite recovery after the Hangenberg Event. Annales de la Société Géologique de Belgique, 115, 559–579.Google Scholar
  36. House, M. R., Gordon, M., & Hlavin, W. J. (1986). Late Devonian ammonoids from Ohio and adjacent states. Journal of Paleontology, 60(1), 126–144.CrossRefGoogle Scholar
  37. Ji, Q. (2004). On the change of conodonts near the Devonian–Carboniferous boundary. Professional Papers of Stratigraphy and Palaeontology, 28, 111–122 [in Chinese with English abstract].Google Scholar
  38. Ji, Q., & Ziegler, W. (1993). The Lali section—An excellent reference section for Upper Devonian in South China. Courier Forschungsinstitut Senckenberg, 157, 1–183.Google Scholar
  39. Ji, Q., Zhang, Z. X., Chen, X. Z., & Wang, G. B. (1987). Study of the Devonian–Carboniferous boundary in the Zhaisha section, Luzhai, Guangxi. Journal of Stratigraphy, 11(3), 213–217 [in Chinese with English abstract].Google Scholar
  40. Ji, Q., Wei, J. Y., Wang, Z. J., Wang, S. T., Sheng, H. B., Wang, H. D., Hou, J. P., Xiang, L. W., Feng, R. L., & Fu, G. M. (1989). The Dapoushang Section: An Excellent Section for the Devonian–Carboniferous Boundary Stratotype in China (pp. 1–265). Beijing: Science Press.Google Scholar
  41. Kaiser, S. I., Becker, R. T., Spalletta, C., & Steuber, T. (2009). High-resolution conodont stratigraphy, biofacies, and extinctions around the Hangenberg Event in pelagic successions from Austria, Italy, and France. Palaeontographica Americana, 63, 99–143.Google Scholar
  42. Kaiser, S. I., Becker, R. T., Steuber, T., & Aboussalam, S. Z. (2011). Climate-controlled mass extinctions, facies, and sea-level changes around the Devonian–Carboniferous boundary in the eastern Anti-Atlas (SE Morocco). Palaeogeography, Palaeoclimatology, Palaeoecology, 310, 340–364.Google Scholar
  43. Kaiser, S. I., Aretz, M., & Becker, R. T. (2016). The global Hangenberg Crisis (Devonian–Carboniferous transition): review of a first-order mass extinction. In R. T. Becker, P. Königshof & C. E. Brett (Eds.), Devonian climate, sea level and evolutionary events. Geological Society of London, Special Publications, 423, 387–437.  https://doi.org/10.1144/SP423.9.CrossRefGoogle Scholar
  44. Klein, C., & Korn, D. (2014). A morphometric approach to conch ontogeny of Cymaclymenia and related genera (Ammonoidea, Late Devonian). Fossil Record, 17, 1–32.CrossRefGoogle Scholar
  45. Klug, C., Frey, L., Korn, D., Jattiot, R., & Rücklin, M. (2016). The oldest Gondwanan cephalopod mandibles (Hangenberg Black Shale, Late Devonian) and the mid-Palaeozoic rise of jaws. Palaeontology, 59(5), 611–629.CrossRefGoogle Scholar
  46. Korn, D. (1981). Cymaclymenia – eine besonders langlebige Clymenien-Gattung (Ammonoidea, Cephalopoda). Neues Jahrbuch für Geologie und Paläontologie Abhandlungen, 161(2), 172–208 [in German with English abstract].Google Scholar
  47. Korn, D. (1988). On the stratigraphical occurrence of Cymaclymenia evoluta (H. Schmidt, 1924) at the type locality. Courier Forschungsinstitut Senckenberg, 100, 215–216.Google Scholar
  48. Korn, D. (1989). Cymaclymenia aus der Acutimitoceras-Fauna (prorsum-Zone) vom Müssenberg (Devon/Karbon-Grenze; Rheinisches Schiefergebirge). Bulletin de la Société belge de Géologie, 98(3/4), 371–372 [in German with English summary].Google Scholar
  49. Korn, D. (1991). Three dimensionally preserved clymeniids from the Hangenberg Black Shale of Drewer (Cephalopoda, Ammonoidea; Devonian–Carboniferous boundary; Rhenish Massif). Neues Jahrbuch für Geologie und Paläntologie, Monatshefte, 1991(9), 553–563.Google Scholar
  50. Korn, D. (1993). The ammonoid faunal change near the Devonian–Carboniferous boundary. Annales de la Société Géologique de Belgique, 115, 581–593.Google Scholar
  51. Korn, D. (1997). The Palaeozoic ammonoids of the South Portuguese Zone. Memórias do Instituto Geológico e Mineiro, 33, 1–131.Google Scholar
  52. Korn, D. (2000). Morphospace occupation of ammonoids over the Devonian–Carboniferous boundary. Paläontologische Zeitschrift, 74, 247–257.CrossRefGoogle Scholar
  53. Korn, D., & Klug, C. (2002). Ammoneaea Devonicae. Fossilium Catalogus Animalia, 138, 1–375.Google Scholar
  54. Korn, D., Clausen, C. D., Belka, Z., Leuteritz, K., Luppold, F. W., Feist, R., & Weyer, D. (1994). Die Devon/Karbon-Grenze bei Drewer (Rheinisches Schiefergebirge). Geologie und Paläontologie in Westfalen, 29, 97–147.Google Scholar
  55. Korn, D., Belka, Z., Fröhlich, S., Rücklin, M., & Wendt, J. (2004). The youngest African clymeniids (Ammonoidea, Late Devonian)—failed survivors of the Hangenberg Event. Lethaia, 37, 307–315.CrossRefGoogle Scholar
  56. Korn, D., Bockwinkel, J., & Ebbighausen, V. (2007). Tournaisian and Viséan ammonoid stratigraphy in North Africa. Neues Jahrbuch für Geologie und Paläontologie, Abhandlungen, 243(2), 127–148.CrossRefGoogle Scholar
  57. Lakin, J. A., Marshall, J. E. A., Troth, I., & Harding, I. C. (2016). Greenhouse to icehouse: a biostratigraphic review of latest Devonian–Mississippian glaciations and their global effects. In R. T. Becker, P. Königshof & C. E. Brett (Eds.), Devonian climate, sea level and evolutionary events. Geological Society of London, Special Publications, 423, 439–464.  https://doi.org/10.1144/SP423.12.CrossRefGoogle Scholar
  58. Lange, W. (1929). Zur Kenntnis des Oberdevons am Enkeberg und bei Balve (Sauerland). Abnhandlungen der Preußischen Geologischen Landesanstalt, Neue Folge, 119, 1–132 3 pls. [in German].Google Scholar
  59. Liu, F., Kerp, H., Peng, H., Zhu, H., & Peng, J. (2018). Palynostratigraphy of the Devonian–Carboniferous transition in the Tulong section in South Tibet: A Hangenberg Event sequence analogue in the Himalayan-Tethys zone. Palaeogeography, Palaeoclimatology, Palaeoecology.  https://doi.org/10.1016/ju.palaeo.2018.03.016 12 pp.
  60. Liu, Y. Q., Ji, Q., Kuang, H. W., Jiang, X. J., Xu, H., & Peng, N. (2012). U–Pb zircon age, sedimentary facies, and sequence stratigraphy of the Devonian–Carboniferous boundary, Daposhang Section, Guizhou, China. Palaeoworld, 21, 100–107.CrossRefGoogle Scholar
  61. Luppold, F. W., Clausen, C. D., Korn, D., & Stoppel, D. (1994). Devon/Karbon-Grenzprofile im Bereich von Remscheid-Altenaer Sattel, Warsteiner Sattel, Briloner Sattel und Attendorn-Elsper Doppelmulde (Rheinisches Schiefergebirge). Geologie und Paläontologie in Westfalen, 29, 7–69 (in German with English summary).Google Scholar
  62. Marynowski, L., & Filipiak, P. (2007). Water column euxinia and wildfire evidence during deposition of the Upper Famennian Hangenberg event horizon from the Holy Cross Mountains (central Poland). Geological Magazine, 144(3), 569–595.CrossRefGoogle Scholar
  63. Münster, G. G. z. (1832). Über die Planuliten und Goniatiten im Uebergangs-Kalk des Fichtelgebirges (pp. 1–38). Bayreuth: Birner [in German].Google Scholar
  64. Nikolaeva, S. V., & Bogoslovskiy, B. I. (2005). Devonskie Ammonoidei. IV. Klimenii (podotriad Clymeniina). Trudy Paleontologicheskogo Instituta, 287, 1–220.Google Scholar
  65. Oliveira, J. T., García-Alcalde, J. L., Linau, E., & Truyols, J. (1986). The Famennian of the Iberian Penninsula. Annales de la Société Géologique de Belgique, 109, 159–174.Google Scholar
  66. Paeckelmann, W. (1922). Über das Oberdevon und Untercarbon des Südflügels der Herzkamper Mulde auf Blatt Elberfeld. Jahrbuch der Preußischen Geologischen Landesanstalt, 42(1), 257–306 pl. 2 [in German].Google Scholar
  67. Paproth, E., & Streel, M. (1970). Corrélations biostratigraphiques près de la limite Dévonien/Carbonifère entre les facies littoraux ardennais et les faciès bathyaux rhènans: Les Congres et Colloques de l’Université de Liége, 35, 365–398, pls. 24–26 [in French with English summary].Google Scholar
  68. Paproth, E., & Streel, M. (1982). Devonian–Carboniferous transitional beds of the northern “Rheinisches Schiefergebirge”. Guidebook, IUGS Commission on Stratigraphy, Working Group ion the Devonian/Carboniferous Boundary (pp. 1–63), Liége.Google Scholar
  69. Paul, H. (1938). Das Unterkarbon der Gegend von Lintorf. Decheniana, 97, 25–42 [in German].Google Scholar
  70. Paul, H. (1939). Die Etroeungt-Schichten des Bergischen Landes. Jahrbuch der Preußischen Geologischen Landesanstalt, 59, 647–726 pls. 39–42 [in German].Google Scholar
  71. Price, J. D. (1982). Some Famennian (Upper Devonian) ammonoids from north-western Europe. Unpublished Ph. D. Thesis, University of Hull, pp. 1–555, 49 pls.Google Scholar
  72. Price, J. D., & House, M. R. (1984). Ammonoids near the Devonian–Carboniferous boundary. Courier Forschungsinstitut Senckenberg, 67, 15–22.Google Scholar
  73. Price, J. D., & Korn, D. (1989). Stratigraphically important clymeniids (Ammonoidea) from the Famennian (Late Devonian) of the Rhenish Massif, West Germany. Courier Forschungsinstitut Senckenberg, 110, 257–294.Google Scholar
  74. Ruan, Y. P. (1988). Ammonoids. In C. M. Yu (Ed.), Devonian–Carboniferous Boundary in Nanbiancun, Guilin, China–Aspects and Records (pp. 251–262, pls. 64–65). Beijing: Science Press.Google Scholar
  75. Qie, W. K., Liu, J. S., Chen, J. T., Wang, X. D., Mii, H. S., Zhang, X. H., Huang, X., Yao, L., Algeo, T. J., & Luo, G. M. (2015). Local overprints on the global carbonate δ13C signal in Devonian–Carboniferous boundary successions of South China. Palaeogeography, Palaeoclimatology, Palaeoecology, 418, 290–303.CrossRefGoogle Scholar
  76. Sandberg, C. A., Morrow, J., & Ziegler, W. (2002). Late Devonian sea-level changes, catastrophic events, and mass extinctions. Special Paper of the Geological Society of America, 356, 473–487.Google Scholar
  77. Schindewolf, O. H. (1923a). Beiträge zur Kenntnis des Palaeozoicums in Oberfranken, Ostthüringen und dem Sächsischen Vogtlande. I. Stratigraphie und Ammoneenfauna des Oberdevon von Hof a. S. Neues Jahrbuch für Mineralogie, Geologie und Paläontologie, Beilage-Band, 49, 250–357 393–509, pls. 14–18 [in German].Google Scholar
  78. Schindewolf, O. H. (1923b). Entwurf einer natürlichen Systematik der Clymenoidea. Centralblatt für Mineralogie, Geologie und Paläontologie, 1923, 59–64 [in German].Google Scholar
  79. Schindewolf, O. H. (1923c). Über Fossley, Étroeungt und verwandte Fragen. Centralblatt für Mineralogie, Geologie und Paläontologie, 1923(214–221), 246–254 [in German].Google Scholar
  80. Schindewolf, O. H. (1926). Zur Kenntnis der Devon–Karbon-Grenze in Deutschland. Zeitschrift der Deutschen Geologischen Gesellschaft, Abhandlungen, 78, 88–133 pl. 4.Google Scholar
  81. Schindewolf, O. H. (1937). Zur Stratigraphie und Paläontologie der Wocklumer Schichten. Abhandlungen der Preußischen Geologischen Landesanstalt, neue Folge, 178, 1–132 [in German].Google Scholar
  82. Schmidt, H. (1922). Das Oberdevon-Culm-Gebiet von Warstein i. W. und Belecke. Jahrbuch der Preussischen Geologisches Landesanstalt, 41, 254–339 pls. 12–13 [in German].Google Scholar
  83. Schmidt, H. (1924). Zwei Cephalopodenfaunen an der Devon Carbongrenze im Sauerland. Jahrbuch der Preussischen Geologischen Landesanstalt, 44(for 1923), 98–171 pls. 6–8 [in German].Google Scholar
  84. Scotese, C. R. (2001). Atlas of Earth History. Paleogeography vol. 1 (PALEOMAP Project, Arlington, TX.). [EB/OL]. (2002–04–20) [2014–04–22]. http:www.scotese.com
  85. Steemans, P., Fang, X. S., & Streel, M. (1996). Retizonomonoletes hunanensis Fang et al. 1993 and the Lepidophyta morphon. Memoires de l’Institut Geologique de l’Universite de Louvain, 36, 73–88.Google Scholar
  86. Su, Y. B., Wei, R. Y., & Kuang, G. D. (1988). Conodonts from Devonian–Carboniferous boundary beds of Duolingshan, Yishan County of Guangxi, and their stratigraphic significance. Acta Micropalaeontologica Sinica, 5(2), 183–194 [in Chinese with English abstract].Google Scholar
  87. Tan, Z. X., Dong, Z. C., Jin, Y. L., Li, S. Q., Yang, Y. C., & Jiang, S. G. (1987). The Late Devonian and Early Carboniferous strata and palaeobiocoenosis of Hunan (pp. 1–200, 31 pls.). Beijing: Geological Publishing House [in Chinese with English abstract].Google Scholar
  88. Walliser, O. H. (1984). Pleading for a natural D/C Boundary. Courier Forschungsinstitut Senckenberg, 67, 241–246.Google Scholar
  89. Wang, C. Y., & Yin, B. A. (1984). Conodont zonations of early Lower Carboniferous and Devonian–Carboniferous boundary in pelagic facies. South China. Acta Palaeontologica Sinica, 23(2), 224–238 3 pls. [in Chinese with English abstract].Google Scholar
  90. Wang, C. Y., & Yin, B. A. (1985). An important Devonian–Carboniferous boundary stratotype in neritic facies of Yishan County, Guangxi. Acta Micropalaeontologica Sinica, 2(1), 28–48 3 pls. [in Chinese with English abstract].Google Scholar
  91. Wang, C. Y., Yin, B. A., Wu, W. S., Liao, W. H., Wang, K. L., Liao, Z. T., Mu, X. N., Qian, W. L., & Yao, Z. G. (1987). Devonian–Carboniferous Boundary Section in Yishan Area, Guangxi in: Carboniferous Boundaries in China. In C. Y. Wang (Ed.), Contribution to the 11 th International Congress of Carboniferous Stratigraphy and Geology (pp. 11–21). Beijing: Science Press.Google Scholar
  92. Wang, K. L. (1987). On the Devonian–Carboniferous boundary based on foraminiferal fauna from South China. Acta Micropalaeontologica Sinica, 4(2), 161–173 [in Chinese with English abstract].Google Scholar
  93. Wang, K. Y. (1997). Devonian. In W. P. Dong (Ed.), Stratigraphy (Lithostratic) of Guizhou Province (pp. 143–161). Wuhan: China University of Geosciences Press [in Chinese].Google Scholar
  94. Wang, X. R., & Ji, Q. (2013). The Huohua section: a new Devonian–Carboniferous boundary section of deep-water facies in Ziyun County, Guizhou Province, China. Geological Bulletin of China, 32(7), 977–987.Google Scholar
  95. Wedekind, R. (1918). Die Genera der Palaeoammonoidea (Goniatiten). Mit Ausschluß der Mimoceratidae, Glyphioceratidae und Prolecanitidae. Palӓontographica, 62. Lieferung, 3–4, 85–184 [in German].Google Scholar
  96. Xu, H. K., Cai, C. Y., Liao, W. H., & Lu, L. C. (1990). Hongguleleng Formation in Western Junggar and the boundary between Devonian and Carboniferous. Journal of Stratigraphy, 14(4), 292–301 [in Chinese with English abstract].Google Scholar
  97. Yin, B. A. (1997). Stratigraphy (Lithostratic) of the Guangxi Zhuang Autonomous Region (pp. 1–310). Wuhan: China University of Geosciences Press [in Chinese].Google Scholar
  98. Yu, C. M. (1988). Devonian–Carboniferous boundary in Nanbiancun, Guilin, China—Aspects and records (pp. 1–379). Beijing: Science Press.Google Scholar
  99. Zong, P., & Ma, X. P. (2012). Spiriferide and spiriferinide brachiopods across the Devonian and Carboniferous boundary in western Junggar, Xinjiang. Acta Palaeontologica Sinica, 51(2), 157–175 [in Chinese with English abstract].Google Scholar
  100. Zong, P., Becker, R. T., & Ma, X. P. (2015). Upper Devonian (Famennian) and Lower Carboniferous (Tournaisian) ammonoids from western Junggar, Xinjiang, northwestern China—stratigraphy, taxonomy and palaeobiogeography. Palaeobiodiverdity and Palaeoenviroment, 95, 159–202.  https://doi.org/10.1007/s12549-014-0171-y.CrossRefGoogle Scholar

Copyright information

© Senckenberg Gesellschaft für Naturforschung and Springer-Verlag GmbH Germany, part of Springer Nature 2018

Authors and Affiliations

  • Meiqiong Zhang
    • 1
  • R. Thomas Becker
    • 2
  • Xueping Ma
    • 1
    Email author
  • Yubo Zhang
    • 1
  • Pu Zong
    • 3
  1. 1.Key Laboratory of Orogenic Belts and Crustal Evolution, School of Earth and Space SciencesPeking UniversityBeijingChina
  2. 2.Institut für Geologie und PaläontologieWestfälische Wilhelms-UniversitätMünsterGermany
  3. 3.Institute of GeologyChinese Academy of Geological SciencesBeijingChina

Personalised recommendations