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The Devonian–Carboniferous Boundary In The Devonian–Carboniferous boundary in the stratotype area (SE Montagne Noire, France) Raimund Feist, Jean-Jacques Cornée, Carlo Corradini, Sven Hartenfels, Markus Aretz, Catherine Girard To cite this version: Raimund Feist, Jean-Jacques Cornée, Carlo Corradini, Sven Hartenfels, Markus Aretz, et al.. The Devonian–Carboniferous boundary in the stratotype area (SE Montagne Noire, France). Palaeobiodi- versity and Palaeoenvironments, Springer Verlag, 2020, 10.1007/s12549-019-00402-6. hal-03005525 HAL Id: hal-03005525 https://hal.archives-ouvertes.fr/hal-03005525 Submitted on 16 Nov 2020 HAL is a multi-disciplinary open access L’archive ouverte pluridisciplinaire HAL, est archive for the deposit and dissemination of sci- destinée au dépôt et à la diffusion de documents entific research documents, whether they are pub- scientifiques de niveau recherche, publiés ou non, lished or not. The documents may come from émanant des établissements d’enseignement et de teaching and research institutions in France or recherche français ou étrangers, des laboratoires abroad, or from public or private research centers. publics ou privés. New Manuscript#1 Click here to access/download;Manuscript;Feist_D- C_MN_R#1.doc Click here to view linked References The Devonian-Carboniferous boundary in the stratotype area (SE 1 2 3 Montagne Noire, France) 4 5 6 1* 2 3 4 7 Raimund Feist • Jean-Jacques Cornée • Carlo Corradini • Sven Hartenfels • Markus 8 Aretz5 • Catherine Girard1 9 10 11 12 1 ISEM, UMR 5554, CNRS, IRD, Université Montpellier, Montpellier, France 13 14 2 Géosciences Montpellier, CNRS-Université de Montpellier-Université des Antilles, 15 16 Pointe à Pitre, (FWI), France 17 3 18 Dipartimento di Scienze Chimiche e Geologiche, Università di Cagliari, Cagliari, Italy 19 4 20 Institut of Geology and Mineralogy, University of Cologne, Cologne, Germany 21 5 Géosciences Environnement Toulouse, UPS, CNRS, IRD, avenue Edouard Belin, 22 23 Toulouse (France) 24 25 26 27 * Corresponding author : [email protected] 28 29 30 31 Abstract 32 33 Sections with continuous sedimentation across the Devonian-Carboniferous (D-C) boundary 34 35 in the Montagne Noire allow to build a virtual transect from shoreline to deep basin. 36 Nearshore facies characterise the D-C boundary stratotype and neighbouring sections at La 37 38 Serre in the Cabrières klippen domain and offshore facies are present at the Col de Tribes and 39 40 Puech de la Suque sections in the Mont Peyroux nappe domain. Both domains exhibit 41 42 equivalents of the Hangenberg Black Shale (HBS). At La Serre, an initial regressive trend is 43 44 indicated by the presence of oculated trilobites in the topmost pre-HBS Wocklumeria 45 Limestones. Above the HBS level, regressive depositional conditions characterise oolitic 46 47 deposits that comprise lithic erosional flows with an admixture of transported shallow-water 48 49 biotas. Maximum regression is recognised with the deposition of coarse breccias and local 50 51 features of emergence prior to the first appearance of Protognathodus kockeli. The oolites are 52 53 superseded by the transgression of outer shelf deposits. In the nappe domain, the HBS is 54 55 intercalated in outer ramp nodular limestones, and it exhibits detrital elements pointing to its 56 regressive nature. The regressive trend culminates than reverses when post-HBS carbonate 57 58 sedimentation resumes. Protognathodus kockeli appears in the post HBS carbonates. 59 60 Associated oculated trilobites indicate shallower bathymetric conditions than those of the pre- 61 62 63 1 64 65 HBS Wocklumeria Limestones. Thereafter, replacement of sighted trilobites by blind ones and 1 2 the protognathodid biofacies by facies dominated by siphonodellids indicate a deepening 3 trend. The near- and off-shore sites of the D-C transition permit correlation of short-term 4 5 bathymetric fluctuations with faunal turnovers and entries of biostratigraphic markers. 6 7 8 9 Keywords Devonian-Carboniferous boundary • Montagne Noire • biostratigraphy • 10 11 sedimentary dynamics • bathymetric trends • near-shore – off-shore correlation 12 13 14 15 16 Introduction 17 18 19 20 Palaeozoic rocks of the Montagne Noire, at the external margin of the southern French 21 Massif Central, underwent a complex poly-phased Variscan deformation that resulted in a 22 23 piling of large-scale, south-facing recumbent folds emplaced during the latest Viséan (e.g. 24 25 Arthaud 1970; Echtler 1990). Synorogenic flysch sedimentation comprises gravitational 26 27 mass-flows with large, up to kilometric-sized olistolitic blocks of various pre-tectonic ages 28 29 (Cabrières klippen, “Ecailles de Cabrières”) (Engel et al. 1978). The rocks were affected by 30 31 syntectonic metamorphism with decreasing intensity in the highest parts of the nappe pile, 32 Hence, the south-eastern inverted portions of the Mont Peyroux nappe, including the 33 34 Cabrières klippen (Fig. 1), are composed of highly fossiliferous sedimentary rocks with only 35 36 locally very low-grade metamorphic overprint (conodont Colour Alteration Index between 2 37 38 and 4, Wiederer et al. 2002). This allows facies analyses and investigations on fine-scaled bio- 39 40 and chemostratigraphy to be conducted in good conditions of preservation. 41 42 During Devonian through early Carboniferous times the nappe successions exhibit an 43 almost continuous carbonate succession that was deposited on a low-angle, flat ramp. After 44 45 deposition in coastal environments related to the initial Devonian transgression on an eroded 46 47 early Palaeozoic hinterland (Feist 1985), the depositional conditions subsequently changed 48 49 with an increase in both depth and distance from the shore. In the Mont Peyroux nappe, the 50 51 Devonian-Carboniferous transition is located in a succession of outer ramp nodular limestones 52 (“supragriottes”, Boyer et al. 1968), which contain a Hangenberg Shale horizon of a few 53 54 decimetres in thickness. Conversely, contemporaneous environmental conditions were 55 56 different in the source area from where the erratic Cabrières klippen originated including the 57 58 La Serre olistolite where the D-C boundary stratotype was defined (Paproth et al. 1991). In 59 60 this area the uppermost Devonian exhibits increasingly strong influence from a near-by 61 62 63 2 64 65 shallow shoal or even emerged land that resulted in dominantly mixed carbonate and 1 2 siliciclastic near-shore sedimentation at the Devonian-Carboniferous transition. Consequently, 3 two domains, near-shore Cabrières klippen and off-shore nappe successions, are represented 4 5 in the south-eastern Montagne Noire (Fig. 1). Description and comparison of these two 6 7 domains using biostratigraphical and sedimentological markers to evaluate the currently 8 9 debated D-C boundary definition is the purpose of this contribution. 10 11 12 13 14 Cabrières klippen 15 16 Sections spanning the Devonian-Carboniferous boundary in different blocks among 17 18 the Cabrières klippen were first compared by Engel et al. (1980-81, fig. 6). While in most 19 20 cases late Tournaisian strata conformably overstepped various levels of the Famennian lower 21 and middle Griotte formations, a complete Devonian through early Carboniferous succession 22 23 is exclusively exposed at La Serre. At this site, local facies of the late Famennian through 24 25 early Tournaisian Griotte Group (Feist 1985; Korn and Feist 2007), including transitional 26 27 beds across the D-C boundary, were subsequently investigated in trenched sections (Feist and 28 29 Flajs 1987a, b; Flajs and Feist 1988; Kaiser 2009; Cifer et al. 2017; updates herein). 30 31 La Serre E’ D-C boundary stratotype section 32 33 The GSSP for the base of the Carboniferous is defined in trench LS-E’ (Fig. 2a) on the 34 35 southern slope of La Serre Hill at about 125 m S of the top 252 and 500 m to the E of La 36 37 Rouquette farmhouse, ca. 2.5 km S of Cabrières (Paproth et al. 1991; Feist et al. 2000). Many 38 39 studies were conducted at the La Serre D-C stratotype section concerning conodonts (Engel et 40 41 al. 1980-81, Feist and Flajs 1987a; Flajs and Feist 1988; Girard 1994; Kaiser 2009), 42 ammonoids (Becker and Weyer 2004; Korn and Feist 2007), ostracods (Casier et al. 2002), 43 44 trilobites (Flajs and Feist 1988; Brauckmann et al. 1993; Feist and Petersen 1995), 45 46 brachiopods (Legrand-Blain & Martinez-Chacon 1988), corals (Semenoff-Tian-Chansky 47 48 1988), fish (Derycke et al. 1995), and foraminifera and algae (Vachard 1988). In addition, 49 50 detailed data on microfacies (Flajs and Feist 1988; Casier et al. 2002), isotope and element 51 52 geochemistry (Brand and Legrand-Blain 1993, 2004; Buggisch & Joachimski 2006; Bábek et 53 al. 2016) are available. 54 55 56 The section displays the upper part of the local facies of the Montagne Noire Griotte 57 58 Group straddling the D-C boundary (Figs. 2a, 3). The exposed base of the section, below Bed 59 64, comprises well bedded, compact, grey-beige platy calcilutites with intercalated 60 61 62 63 3 64 65 calcisiltites. The former are organized into dm-thick beds with horizontal to oblique plane 1 2 bedding, convolutes and ripple-marks at their top. As such they are interpreted as fine- 3 grained, distal turbidites. The facies becomes predominantly nodular towards the top (Beds 4 5 64-67), and terminates with a layer of dissociated micritic limestone nodules in a clayey 6 7 matrix (Bed 68). These contain a few poorly preserved iron-oxide coated Wocklumeria sp., 8 9 giant (up to 5mm long) leperditiid-like ostracods and numerous, often fragmented small 10 11 trilobites. The varied association of the latter is dominated by sighted taxa, phacopids 12 13 (Omegops) and proetids (Pseudowaribole) (Fig. 4), whereas blind forms characterizing the 14 deeper off-shore domain such as Helioproetus are rare, and in particular, Dianops and 15 16 Chaunoproetus are missing.
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