Los ambientes de playa de la Cuenca de Lodeve (Languedoc-Francia).
Playa sequences represent one of the richest suites of sedimentary facies and fossils stacked in the geological record because of the overall periodic change of the depositional system. This dry flat-floored bottom depression found in inner to coastal basins of arid and semiarid regions are periodically ponded by ephemeral shallow lakes (Blackwelder, 1931) and shows multiple facies changes from alluvial fan gravel and wadi poorly-sorted sand to lacustrine laminated mud with possible evaporite deposits, topped by desiccated surfaces and aeolian sand dunes. A variety of flora and fauna, carefully preserved, in the fine grained sediments of the playa-lakes reveal evidence of life bloom during humid periods. Animal tracks and other biogenic structures (bioturbations, burrows, paleosoils) complete the paleoecological diversity on the wet banks of the channels and standing waters.
The Lodeve Permian Basin, in the southern border of the Massif Central, displays a particular well preserved suite of playa sequences and associated paleontological remains, because of both large continuous outcrops and a dense mining network for uranium exploration. In particular, large open mine quarries coupled with more than 40 km of galleries and thousand-km borehole revealed complementary fossiliferous-rich layers which allow to better constrain the structure and the geohistory of the basin.
Plant remains are of particular abundance in the lacustrine blackshales of the lowermost part of the Autunian Group and vanish progressively upwards because of the low potential of preservation in the red playa/floodplain pelites of the Saxonian Group. On the contrary, these red sub-emersive facies present a high potential for vertebrate footprints and ichnotraces preservation, associated locally to invertebrate and plant debris accumulations in flooding rills. Thus, in them, Dr Jean Lapeyrie, surgeon in Lodeve discovered, about twenty years ago, an exceptional rich suite of insects, conchostracans and triopsids in several levels, ranging from the base to the top of the Salagou Fm of the Saxonian Group. More recently this Formation revealed vertebrate remains which are excavate every year by a French-German team (Dijon, Freiberg, Montpellier Universities, MNHN and CNRS of Paris; Schleusingen Museum, Thuringe).
These paleontological studies, coupled with sedimentological and structural data help to constrain the overall conditions of the Permian playa paleoenvironment. This paper is an exhaustive synthesis of the physical, biological and geodynamical evolution of the Lodeve Permian playa system.
2. General location
The Lodeve basin is a half-graben of Permian age, with a 15-20[degrees] southward dipping continental infilling that extends over an area of about 150 [km.sup.2], on the southern border of the Massif Central (Fig. 1). The basin was sealed by a thick horizontal Mesozoic cover which is presently eroded, allowing the exposure of the basement and of the lower Permian series on the northern border. It is surrounded by the Palaeozoic of the Montagne Noire to the west, the Mesozoic Causses Plateau to the north, and the Languedoc Tertiary plain to the south. The Permian deposits overlap both the Graissessac Stephanian deposits which crop out westward in a narrow basin and folded Cambrian carbonates which are exhumed in the North of the basin (Lodeve Ridge, Fig. 2). More precisely, four domains demarcate the basin (Figs. 1, 2):
Northward, the basin is bounded by the plateau of the "Causse du Larzac" (700 m high) formed by a 400 m-thick succession of Mesozoic limestone deposits (Jurassic), by basal sandstone, mudstone and evaporite deposits (Triassic). These latters are subhorizontal and lie unconformably on the Permian and on the hercynian basement, which outcrops directly to the north forming the "Lodeve Ridge"; to the south-west in the Montagne Noire, and to the north-east in the Cevennes.
Westward, the basin is hidden by the north-south stretch basaltic plateau of the Escandorgue (800 m high), which underlines a volcanic main axis of Pliocene to Quaternary age.
[FIGURE 1 OMITTED]
[FIGURE 2 OMITTED]
South-westward, the hills of Cabrieres (350 m high) represent the eastern extremity of the Montagne Noire hercynian folded belt.
Eastward, the basin is limited by the NNE-SSW trending Cevennes Fault along which a slice of Lower Liassic carbonates (Hettangian) is sandwiched between the Permian and the Cenozoic deposits of the Herault valley. There is no information of the continuity of the Lodeve basin eastward of the Cevennes Fault. The Lergue valley at the "cluse de Rabieux" constitutes the main access to the basin, when coming from the south. Beyond the Cevennes fault limit, the Tertiary molasses of the Herault plain represent the most important wine growing of the region.
Southward, the basin is presently limited by the E-W trending les Aires-Mas Blanc fault. This post-Bathonian down-to-South normal fault precludes observations of the southern border of the basin. Volcanic ashes beds (= "cinerites) correlations between the Lodeve and the Gabian basins, located 10 km southward, argue for the connection of both basins during the Lower Permian time. However, the Pre-Anisian tilting of Permian deposits implies that the basin registered a synsedimentary tilting during the Middle/Upper Permian time in relation with the activation of a north-dipping listric fault, south of "les Aires-Mas Blanc fault". The Lower to Middle Jurassic carbonates of the Moureze graben are characterized by both slide blocks of Lower Liassic carbonates related to Liassic extension and folds, related to later Pyrenean shortening. At a general scale, the crustal extension linked to the Cevennes fault is related to the thinning of the crust, associated to the opening of the Ligurian Ocean during the Early Jurassic time (Lemoine et al., 1984).
3. Origin, palaeontology and stratigraphy of the studied basin
3. 1. Basin geohistory
3. 1. 1. Hercynian cycle
Over a Precambrian basement, the series are mainly composed of shelf deposits (carbonate and siliciclastic facies) in the Montagne Noire and a comprehensive series of slope shales in the Cevennes. During the Lower Carboniferous, the paroxysm of the Hercynian shortening conduced to turbidite deposition in front of large southward vergent recumbent folds, in the southern side of the Montagne Noire.
The shortening stage is followed in the Montagne Noire by the uplift of the gneiss dome in the axial zone, and the associated collapse of the northern border with the opening of the extensional basin of Graissessac during the Wesphalian time (Echtler and Malavieille, 1990). In this E-W elongated basin, a high heat flow was responsible for coalification of many lacustrine coal beds sandwiched in coarse grained fluvial to deltaic deposits (Becq-Giraudon, 1973; Saint-Martin, 1993). Eastward, the E-W trending Graissessac basin is overlaid by the Permian deposits of the Lodeve basin (Garric, 1965; 2007). It forms a south dipping half-graben necessary limited to the south by a north dipping listric normal fault related to the late orogenic extension.
3. 1. 2. Mesozoic sedimentation
At the base of the Mesozoic series, the Middle Triassic deposits, unconformably seal a major erosive surface truncating the Permian half-graben and its basement at the western margin of the South-East basin. The silicoclastic continental platform of the Triassic (fluvial to playa-lake dominated systems, Lopez and Mader, 1985; Lopez, 1987; Lopez et al, 2005) was invaded by a shallow carbonate platform (stromatolithic dolomudstone flat) during the Lower to Middle Liassic time. The later was drowned by pelagic marls at the Upper Liassic time. During this period, the sedimentation was controlled by NE-SW trending faults (in particular the Cevennes fault) with an overall eastward deepening toward the SouthEast Basin. This crustal scale extension was associated to the thinning of the crust during the opening of the Liguro-Tethysian ocean (Lopez, 1992). Upper Liassic marls grade upward to an outer shelf marl-carbonate interbedding and high energy shelf deposits during Middle Jurassic. Upper Jurassic deposits are dominated by restricted inner to outer carbonate platform sediments (Causses Gulf) (Lopez et al., 1997).
3. 2. Lithostratigraphy
Permian deposits were subdivided for a long time (Feys and Greber, 1972; Chateauneuf and Farjanel, 1989) into 2 large megasequences: Autunian and Saxonian, both lying unconformably upon the Upper Carboniferous and on the Hercynian basement.
In the Lodeve basin, the Permian deposits (Fig. 3, 4) have been differently divided in accordance to different authors with slight modifications of the terminology proposed by the Cogema (Uranium General Company) which uses numerous key beds such as ash-layers (cinerites) and organic-rich layers ("facies couche"), allowing fine correlations. In this sense, two main facies assemblages have been distinguished which represent, both an overall geodynamical and a paleoenvironmental change in the basin geohistory.
In the Lower part of the basin infill the 730 m-thick Pre-rift series (Autunian according to Feys et al. (1972) or Upper Autunian to Lower Thuringien according to Odin (1986) = Autunian Group sensu Gand et al. (1997). It is composed of fluviatile to deltaic sandstones (Usclas--St Privat Fm = F 1) evolving into anoxic deep lacustrine black shales with a high potential source rock for HC (Tuillieres-Loiras Fm = F 2); the later passing upward to sub-emersive floodplain pelites (Viala Fm = F 3).
[FIGURE 3 OMITTED]
The Syn-rift Series (about 2000 m thick = Saxonian Group sensu Gand et al. (1997) is evidenced by a regional unconformity and by an overall southward thickening of the deposits. This series begins with fluviatile coarse conglomerates evolving to sandstone deposits (Rabejac Fm: F 4) forming a key event into the sedimentary pile. The later evolves rapidly to thick floodplain pelites (= silty red mudstones) and thin playa-lake dolomites (Salagou Fm = F 5). In the western part of the basin, floodplain pelites pass directly to thick debris-flow deposits (La Tour-sur-Orb Member), related to the activity of the bordering faults. The global evolution of the facies is connected to the progressive climatic change from wet-tropical to semi-arid conditions, driven by the gradual northward moving of the continental plate.
[FIGURE 4 OMITTED]
3. 3. Palaeontology: flora, fauna and palichnofauna
Connected with the colour of the Formations, macro and microflora is mostly present in grey levels of the Autunian: Usclas and St-Privat Fm (= F1), Tuilieres-Loiras Fm (= F2). Nevertheless, sometimes in red layers (Rabejac Fm = F4) and especially in green beds of the Salagou Fm, macroflora may be found but is less determinable.
In the Autunian Group, vertebrates were mentionned, for the first time, during the 19th century. They consist of a skeleton of an Araeoscelidian [Aphelosaurus lutevensis (Gervais, 1859) (Thevenin, 1910), redescribed by Falconnet, 2007], some remains of Amphibians ("Branchiosaurus", "Actinodon", Discosauriscus, Eryops), and of Pelycosauria (Heyler, 1969), Fishes with Acanthodes sp. (Acanthodians), Pygopterus sp. (Palaeonisciforms Actinopterygians) (Heyler, 1969) and Usclasichthys macrodens Heyler, 1977. The Saxonian group supplies bone-beds and some amphibians, found in the Rabejac Fm (Heyler 1969) and also a small vertebral column of a Tupilakosaurid (Werneburg et al, 2007) coming from the Salagou Fm. A few years ago, Korner discovered in the top of this last Fm, more precisely in la Lieude Member, well preserved Pelycosaurian bones trapped in a debris-flow deposit (under preparation).
In the opposite, footprints are rather widespread in all the Formations (Fig. 5) with 3 remarkable sites: the Cogema quarry (Mas d'Alary Member), the Rabejac quarry (Rabejac Fm), and the paleontological slab of "la Lieude" located at the top of the Salagou Fm.
The first observations on footprints were made by F. and P. Ellenberger (1959) then new discoveries and studies were supported by Heyler and Lessertisseur (1963) who described "14 new genera and 16 new "species". Ellenberger (1983-1984) distinguished and erected "almost 130 new ichnotypes". Later, Gand (1987) revised and reevaluated the French Permian footprints from prospectings in all the French basins and studies of European fossil collections or sites. Thus, he proposed only 14 ichnogenera and 22 ichnospecies for the Lodeve basin. Lately, the following list, still has been shortered with 16 ichnosp. (Gand and Durand, 2006) (Fig. 5). They are:
A- Traces attributed to Temnospondyls (Branchiosauridea and Micromelerpetontidea) = Anthichnium (Geinitz, 1861) Haubold, 1971 = Batrachichnus (Geinitz, 1861) Haubold, 1996 with undertracks Salichnium decessus or S. pectinatus (Heyler and Lessertisseur, 1963); Eryopidea: Limnopus zeilleri (Delage, 1912) Gand, 1985; Amphisauropus latus Haubold, 1970.
B- Traces ascribable to Amniotes; Captorhinomorpha or gracile reptiles with Hyloidichnus major (Heyler and Lessertisseur, 1963), Haubold, 1971; Varanopus curvidactylus Moodie, 1929 (Sarjeant, 1971), Microsauripus acutipes Moodie, 1929 (Sarjeant, 1971); Varanopus rigidus Gand, 1989; Pelycosauria with Dimetropus leisnerianus (Geinitz, 1863) Haubold, 1971, Dimetropus nicolasi Gand and Haubold, 1971 being its undertrack; Diadectids (Voigt, 2004): cf. Ichniotherium cottae (Pohlig, 1886) Haubold, 1971; "Eosuchia" and Araeoscelids: Dromopus lacertoides (Geinitz, 1863) Haubold, 1971; Dromopus didactylus (Moodie, 1930) Gand and Haubold, 1984; Therapsida or "Therosauria": Lunaepes ollierorum, Merifontichnus thalerius, Planipes brachydactylus Gand et al., 2000; Caseids or Therapsida: Brontopus circagiganteus Gand et al., 2000, B. giganteus Heyler and Lessertisseur, 1963.
Insects, Notostraca, and Conchostraca are also frequent, mostly in the Salagou Formation (see infra). Notostraca trackways are described by Gand et al. (2008).
3. 4. Stratigraphical data (Fig. 4, 6)
Autunian and Saxonian were regarded a long time as continental stages. The first, of gray colour, was characterised by its flora and microflora suite, and the second, with dominant redbeds deposits was only dated by a "saxonian" footprint association rather similar to that observed in Thuringian Forest (Germany) (Haubold, 1974; Gand, 1987).
The exclusive use of marine stages in the international stratigraphic scale involved de facto the abandonment of the terms Autunian and Saxonian and the continental series are nowadays reported to their marine equivalent by radioisotopic data or to references to marine series showing fossiliferous continental intercalations. That is the case for some US American and Russian.
3. 4. 1. Age of the Autunian Group
For the Autunian Group of the Lodeve basin, the K/Ar radioisotopic datings, carried out on potassic feldspars of XXIV, X, XI, V volcanic-ashes provided triassic and jurassic ages. Successively, from the base to the top: 242 [+ or -] 7, 173 [+ or -] 5, 206 [+ or -] 6, 248 [+ or -] 8, 248 [+ or -] 8 Ma, i.e Anisian, Aalenian, Norian, and Olenekian; because of a probable rejuvenation of the K/Ar system during the late tectonosedimentary events.
From these results, one of us (JS) undertook new datings. Thus, the Viala Fm. is dated of 289.3 +/- 6.7 Ma (U-Pb) (Schneider et al., 2006; Roscher and Schneider, 2006). This means an age included in a large interval: Middle Asselian to Middle Artinskian.
From palaeontological data: Zeiller (1898), Florin (1938, 1944), Doubinger (1956, 1963 a, b), Doubinger and Kruseman (1965), Doubinger et al. (1987), Galtier and Broutin (1995) (see details in Gand et al., 2004 a, b) and Broutin et al. (1999), the Autunian Group could be dated from the End Gzhelian to the Lower Sakmarian from the top of the Usclas and St-Privat Fm (F1) to the Upper limit of Tuilieres-Loiras Fm (F2). This age is supported from autunian flora and microflora. The Viala Fm (F3) would be partly of Artinskian according to the occurrence of Supaia.
3. 4. 2. Age of the Saxonian group
The Octon Member (Fig. 4) would be of 284 [+ or -] 4 Ma in age (Schneider et al., 2006; Roscher and Schneider, 2006), therefore included between the Middle Sakmarian to the Middle Artinskian interval. From magnetostratigraphic investigations, the "la Lieude Member" would be "in a position just around the Illawara reversal, that is Lower Capitanian respectively Lower Tatarian age" (Legler et al., 2004).
Other ages are suggested by paleontologic data, depending of the taxa. According to:
- The plant Supaia, the whole Rabejac Fm (F4) + Salagou Fm (F5) is supposed to represent a part of the Artinskian and the totality of the Kungurian (= Upper Cisuralian).
- Conchostracans, F4 and F5 would be deposited between the Upper Sakmarian or Artinskian (Middle Cisuralian) to the Tatarian (Capitanian).
- Footprints, the Rabejac Fm + the Salagou Fm (till the "la Lieude") would be dated between the Late Sakmarian (Middle Cisuralian) to the Lower Guadalupian (= Wordian/Roadien) (Gand and Durand, 2006).
- Blattoids, the Salagou Fm (from the base to the Arieges level) would be comprised between the Kungurian (Late Cisuralian) to the Lower Lopingian (Schneider in Gand et al., 2004a, b).
- Odonatoptera and Archaeorthoptera, the Salagou Fm, between R 300-R 800 the reper levels, could be dated between the Artinskian (Middle Cisuralian) to the Kazanian (Guadalupian) (Nel et al., 1999a-c; Bethoux, 2003).
[FIGURE 5 OMITTED]
[FIGURE 6 OMITTED]
4. The playa systems of the Saxonian Group (syn-rift series)
During the deposition of the Saxonian Group, the intense activity of the southern bordering fault linked with differential subsidence, and coupled with semi-arid climatic conditions, was periodically compensated by large flooding inputs from the western source areas, leading to a large terminal sub-emersive muddy fan. Under these conditions, the basin acted as a flat-floored bottom depression, periodically ponded by ephemeral shallow lakes during a water-table rise or during direct flooding allowing playa development.
4. 1. The Rabejac Fm: an alluvail fan conglomerate system
The Rabejac Fm overlies the Viala Fm with an angular unconformity clearly visible along the road from Salelles to Loiras village (Fig. 7 A, B), where the mud-supported conglomerates and unsorted coarse sandstones of the Rabejac Fm erode the floodplain pelites of the Viala Fm. This regional unconformity, with a preserved thickness of the Viala Fm, from 50 m near Lunas village in the western part of the basin, to 330 m near St-Jean-de-la-Blaquiere in the east, marks the beginning of the activity of the Mas Blanc, les Aires, Cevennes bordering faults with the half graben differentiation of the Lodeve basin.
This increasing tectonic activity at the southern and the eastern borders was accompanied by a sudden uplift of the hercynian ranges in the western limit of the basin (Montagne Noire domain) with an overall progradation of alluvial fan systems and debris-flows at the base of the Rabejac Fm.
The Rabejac Fm (= F4) was subdivided, from the western to the eastern part of the basin by Odin (1986), successively in the St-Xist, Rabejac and Lafont "facies". This Formation starts with fluvial basal conglomerates erosive on the Viala Fm. They extend on the entire basin but are thicker and coarser from East to West. Near la Tour-sur-Orb area, they display a fan conglomerates assemblage (St-Xist facies), revealing the tectonic activity of the Bousquet d'Orb / la Tour-sur-Orb border fault, and the uplift of the hercynian domain that provides a persistent supply of coarse debris spreading out to the east.
The Rabejac Fm consists of coarse alluvial fan deposits in the western border, passing toward the basin to red sandstones and mudstones with abundant sedimentary structures (ripple marks, desiccation cracks, footprints and invertebrates tracks), indicating long subaerial exposure. These alluvial fan deposits may be connected with the Saalian volcano-tectonic events.
In this Formation, little Branchiosauridae / Temnospondyls have been mentionned by Heyler (1969). Footprints are numerous with Batrachichnus salamandroides (undertracks = Salichnium decessus or S. pectinatus, Limnopus zeilleri, Amphisauropus latus, frequent Hyloidichnus major, Varanopus curvidactylus / Microsauripus acutipes, Dimetropus leisnerianus and Dromopus didactylus. Isopodichnus furcatus Gand, 1994, is very abundant. It is an invertebrate resting trace (cf. infra. Gand et al., 2008).
Macroflora is often well kept. It is described by Galtier and Broutin (2008).
4. 2. The Salagou Formation: permanent floodplain and playa-lake system
4. 2. 1. The physical environment in the Merifons area
The hills of Merifons expose the Salagou Fm that characterizes the most important syn-rift infill. In this area, the fine green carbonate-rich layers hardened regularly the surface, causing beautifull arabesques with high contrats of colors (Fig. 8).
Stratigraphical and sedimentological organisation
The Salagou Fm (F5) corresponds to a 2000 m-thick vertical accretion on the hanging wall of the Aires-Mas Blanc fault (Fig. 3). It consists of dominant pelites in submersive floodplain to playa-lake environment. During this period, the activity of the "les Aires-Mas Blanc" fault controlled the incremental infilling of the basin, and led to an overall divergent (fan-shape) geometry of the deposits (Fig. 2).
The following facies sensu Kruseman (1962) have been distinguished:
The "Octon facies" is made of fined grained deposits outcropping widely in the western part of the basin ("Ruffes" landscape). It corresponds to a vertical cyclic alternation of meter- to decameter-thick red massive pelites with cm-thick, yellowish-gray carbonaceous siltstone horizons with desiccation cracks, ripples marks, invertebrate tracks, and rarely, arthropod remains. Some of these latters horizons were mapped, and numbered as R 100 to 1000 reper-marks in figure 4 by Henriot (Cogema, 1988; unpublished document).
Desiccation cracks indicate period of intense evaporation causing water level fall, shrinkage and finely exposure (Fig. 9). During this time, ponds are isolated from terrigenous input, and the carbonates precipitated from the standing water by the related increase of salinity. The gray to green dolomitic intervals are thinly laminated and generally topped by oscillation ripples (wind effect) (Pochat et al., 2005), polygonal cracks and footprints. Pelites correspond to extensive sheet floods mobilizing large amount of fine detritus from the source area, and spreading it throughout the basin. On more proximal of zones debris-flow deposits, isolated channel fills develop at the base of the flooding event (Fig. 10). In such environment, regular cyclicity could indicate monsoon-like regimes.
[FIGURE 7 OMITTED]
Westward to the Octon village, the transition of the Octon facies to the "Merifons facies" is observed. The frequence of the cycles increases drastically. The red mudstones/siltstones part decreased to decimetres, and the carbonaceous desiccation crack-horizons are, apparently, more frequent. The colour of the latter one changes to pale green; often they form large surfaces with beautiful desiccation cracks. The base of the "la Lieude facies", in the top of the "Merifons facies", is marked by the sudden shedding of debris flow conglomerates after hundreds of meters of nearly exclusive pelitic sediments. At this level, Therapsid footprints occur (Gand et al., 2000). Higher, in the profile, the pelitic intercalations disappear between stacked conglomerates and sandstone horizons. The very coarse "la Tour-sur-Orb facies", in the south-west corner of the basin, represents the proximal fan deposits of the "la Lieude facies". The drastical change from the Merifons to the La Lieude facies is still under discussion now: climatic change and/or tectonic activation (Korner et al., 2003; Legler et al, 2004).
La Lieude facies: typology of sandstone sequences
Origin of red pelites
Red pelites are mainly composed of clay minerals (in particular kaolinite), fine silt, [Fe.sup.+++] oxides and additional dolomite coming from the erosion of a thick lateritic crust developed on the emerged hercynian belt, and under tropical dry climatic conditions (ferallitisation, Fig. 10). In this sense, the red colour already existed in the transported sediment. It differs from the green colour that indicates syn- to post-depositional diagenetic processes.
Three main types of green horizons are visible:
- Mottled green/red pelites: mark the imprint of fluctuating paleo-watertables;
- Coarse to very fine sandstone beds forming extensive laterally-migrating fluvial channels. The flux of water in these channels is supposed more continuous, with a permanent low-oxygenated water body, allowing early reduction of iron oxides;
- Thin and continuous carbonate-rich layers. This particular facies indicates the development of isolated ponds, were low-oxygenated standing waters evaporate, resulting in carbonate precipitation. Locally, some joints and fractures in red pelites show a centimetre-thick green fringe related to present day drainage by meteoric waters.
Two main types are sandwiched in the red pelites of la Lieude:
1) The type I visible in front of la Lieude farm, corresponds to isolated decametre-wide and metre-thick red sandstone lenses (Fig. 11A). The base of the channel is entrenched on a dolocrete paleosoil (with numerous rootlet prints and nodules = a). It displays discontinuous pelite- and yellow carbonate-supported (= paleosoil reworking) conglomerates (b) passing to ungraded pelite-rich coarse sandstone (c). The upper part of the channel infill is more organized with trough cross-bedding or plane-parallel bedding (e), indicating sheet-flood processes after the channel abandonment and plugging (d).
This type of isolated channel is supposed to form on the alluvial fan fringe by the development of an ephemeral channel network that deeply incises the emerged and highly weathered red pelites above the regional base level.
2) The type II outcrops north-eastward the footprint surface of la Lieude farm. It corresponds to a meter-thick green-coloured sand layers. From the base to the top, it is composed of medium to coarse, poorly graded clayed sandstones, and locally lag conglomerates that fill desiccation cracks (Fig. 11B), passing to massive or planar-laminated, medium to fine grained sandstone beds (Fig. 12), with possible lateral accretion.
This type of sequence indicates the periodic development of wide shallow channels and sand sheets on the central part of the playa during flooding periods. In this zone, the fluvial network does not entrench, because the base level is at (or just above) the topographic surface. The continuous existence of a shallow to sub-emerging watertable is indicated by the dominance of the green iron-reduced facies.
Ponded fine to very fine green sandstones are associated with the last channel sequence and correspond to cm- to dm-thick non-erosive massive to graded beds, with a lenticular shape. The lateral pinch-out of the sandstone layer displays often desiccation cracks on carbonate-rich silts, indicating the rapid exposure of the margins. Such ponded beds are possibly topped by symmetrical ripples, formed by wind-driven oscillatory processes on very shallow standing waters.
The fossiliferous rills: nature and origin
These sandy bodies were discovered by Jean Lapeyrie who found inside numerous and new well preserved fossils, mainly crustaceans and insects (Gand et al., 1997; Garric, 2001). In the Merifons area, these bodies called "rills / drains" display a typical network organization.
The typical rill vertical section shows three parts (Fig. 13).
- The upper part is widened, U- or V-shaped, and corresponds to the rill sensu stricto. The U-shaped rill, more resistant, is generally found intact, while the V-shaped ones are dislocated into thin slabs.
- The lower part is narrower and sub-rectilinear. In some cases, it resembles a plant root or a vein. The intermediate zone is well marked by a collar and is of a clear green-grey colour and contrasts on the red brown pelite background.
[FIGURE 8 OMITTED]
In transverse section, rills appear as sedimentary bodies of small dimensions. Most of the U-shaped rills are isodiametrical (10 cm or a little more), while the V-shaped rills are larger than high. Sometimes, a rill can exceed one meter in overall directions. On the other hand, the lower part or "root" is disproportionate, reaching 2 to 4 m in height for a width not exceeding 10 cm.
In its horizontal plane, the rill is longer than broader; the visible length may reach 10 meters. Exceptionally, the main rill of "les Vignasses" site extends up to 86 m. The U- and the V-shaped rills correspond to well distinct deposits. The U-shaped ones are constituted of poorly graded siltites. They contain green, clayey chloritic pellets and various intraclasts representing a poorly cross-bedded microbreccia facies. They are often very resistant and do not show stratification. They are rich in recrystallized carbonates. The V-shaped rill is formed by finely graded siltites. When the sediment is grey-green, a clear stratification with alternating light and dark laminae (representing periodic kerabitume deposition) is visible. When the sediment is reddish, bedding is less visible but millimetric laminations are obvious in thin section. The fine alternation results in a fragmentation into slabs recding is clearly concave and connected to the enclosing sediment. By intervals, there are joints corresponding to a deposition of whitish, phyllitic (clays) or reddish (ferric oxides) minerals. Those rill structure and infill are interpreted to be made by rainwater entrenchment on desiccation cracks and/or open fractures. They are scattered in claystones, representing former sediments which were formed in a playa environment under semi-arid tropical conditions.
[FIGURE 9 OMITTED]
[FIGURE 10 OMITTED]
The abundance of fossils in the rills is supposed to be due to washing/streaming power of rainwater on desiccated surfaces, and to the action of the wind which could concentrate their body fragments, scattered on the surface of the playa. It is probably the case for the insect wings. The presence of Triopsids and Conchostracans may be explained by the deposit of their remains after their death.
Evidences for volcanic activity during the deposition of the playa sediments
In the Salagou Fm, some playa sequences contain pyroclastic material, indicating the permanence of a volcanic activity in the Lodeve basin as precised by Nmila et al. (1992) and Nmila (1995). The tuffaceous material mixed with detrital sediments, was observed in marker beds R 100 to R 1000 (cf supra). After Nmila et al. (1992): "In thin section, these levels display the following main characteristics: quartz typically of volcanic origin (isomorphous faces, volcanic glass inclusions), numerous stretched crystals of feldspar showing more or less advanced degrees of alteration, volcanic glass shards and pumice fragments with I, T, Y, X, etc... type perlite, and oval glass stones formed at the same time showing a degree of alteration. Analcime developed from fragments of acidic volcanic glass during diagenesis. These characteristics are typical of ash falls and provide evidence for the volcanic origin of these marker horizons". The trace elements and the zircon typology demonstrate also an alkaline volcanisme typical of the second French Permian sedimentary cycle (= "Saxonian").
Cyclicity and geochemistry: the climate during the Salagou formation deposition
Sedimentological, geochemical, mineralogical, palaeoecological investigations were carried out in the Lodeve basin in order to reconstruct the climatic processes which control the litho- and biofacies patterns during an Icehouse/Greenhouse transition, as well as the correlation of marine and continental climatic signals. Based on Odin (1986), Henriot (1988), and Nmila (1995), 250 m of the Usclas-St-Privat, Tuilieres-Loiras and Viala Fm, as well as 1600 m red beds of Rabejac, and Salagou Fm have been documented. In this last one, about 5.000 cycles have been measured for the cyclostratigraphy (Korner 1999a, b; Korner et al, 2003).
[FIGURE 11 OMITTED]
[FIGURE 12 OMITTED]
The climatic signal could be characterized as follows (Figs. 6, 15, 16). From the Upper Tuilieres-Loiras Fm to the Lower Viala Fm., a transition from warm-humid to semi-arid conditions occured. Gypsum-pseudomorphs, desiccation cracks, xeromorphic calcisols and vertisols as well as mesophile fauna and flora were characteristic of the red, brown flood plain deposits of the Viala and the Rabejac Fm. For the Salagou Fm, during the Octon Member deposit, the aridity increased then decreased while the Upperlaying Merifons Member. At this period, palaeoenvironment and climate of the Lodeve basin were probably the following: periodic or episodic strong rain falls, temporary water filled channels contain mass occurences of xerophile organisms (Conchostracans, Triopsids, Insects). The same results are known from observations in modern playa and sabkha environments, e.g. in Jordan and Tunisia.
[FIGURE 13 OMITTED]
[FIGURE 14 OMITTED]
The sedimentary architecture of the la Lieude facies/ Member indicates a fast change of sediment supply. These coarse clastics appear suddenly above 2000 m of nearly exclusive fine grained sediments! They result from rapid increasing precipitations and consequently from prograding alluvial fans. Linked to that is the appearance of very diverse tetrapod tracks and the re-occurrence of mesophile flora and invertebrate burrows (Scoyenia). This climate change could be possibly the effect of Upper Permian transgressions (Bellerophon Fm, Zechstein-transgression).
4. 2. 2. The life in the playa.
In the Lodeve Basin, flora, invertebrate and vertebrate remains (fishes, amphibians, reptiles) have been principally collected in the Lower part of the Permian series: grey Formations F1-F2, L1, L2 Members. Higher, various traces of biological origin have been found in the red facies which began at F2-L3 Fm (Fig. 4).
Invertebrate, and vertebrate tracks, burrows, common in the Autunian Group, were a long time only mentionned at the base of the Rabejac Fm. and at the top of the Salagou Fm. (Saxonian Group) (Fig. 4). As the deposits between the two Fm. lacked of fossils, it was generally accepted that the "Saxonian" was azoic, probably because of arid conditions. In fact, it was not the case like shown by the important discoveries of Dr Jean Lapeyrie happened in small silstone rill lenses of the Salagou Fm (Gand et al., 1997).
Invertebrates (Fig. 17)
They have been found in many levels from the base of the Usclas and St-Privat Fm up to the lower part of the la Lieude Fm. (Fig. 4, 17. 13-14). Species from Salelles and Arieges seem to be somewhat more developed than the Conchostracans of the Upper Rotliegend I, Tambach Fm (Martens, 1983) and Muritz Fm (Germany) dated of Sakmarian/Artinskian (Schneider in Hoffmann et al., 1989; Schneider et al., 1995). One form from Arieges is possibly derived from Lioestheria andreevi of the Tambach Fm, dated of Wolfcampian from vertebrates (Sumida et al., 1996). Specimens from Salleles area could be compared with Isaura harveyi and Palaeolimnadiopsis brevis of the Wellington Fm, (Leonardian of Kansas). Most interesting Conchostracans are found, short below and above the basal fanglomerates of the La Lieude Fm. The 3 mm to 5, 5 mm large forms show a delicate meshwork between the growing lines, a feature also seen in Mesozoic species. This suggests, eventually, a latest Permian age for these beds.
[FIGURE 15 OMITTED]
Triopsids and their tracks
Body-fossils: Triops cancriformis permiensis and Lepidurus occitaniacus have been described, from a large sample composed of thousands of carapaces, thoraco-abdominal fragments and more rarely from intact specimens. They are similar to modern species (Gand et al., 1997) (Fig. 17).
On the basis of the ecological preferences of modern Triopsids and of the sedimentological characteristics of their environment during the Permian, occurrence of shallow, temporary lakes during the deposition of the Salagou Formation was confirmed. These pools, either neutral or slightly alkaline, were scattered across a playa type environment and lasted with the same characteristics during the deposition of the formation which is 2000m thick in the southern part of the basin. Aridity during this long period of sedimentation had been suggested also from sedimentological data (dessication cracks, rubefaction).
Numerous invertebrate traces (Gand et al., 2004; 2008) have been found (Fig. 17). Some of them are Endichnia: endogenic traces (tubes and burrows) among them delicat Scoyenia gracilis common and beautifull in Rabejac Formation. They are probably due to burrowing Insects.
Others are Epichnia: exogene ichnites:
- Furrowing bilobate fine striked tracks Isopodichnus eutendorfensis Linck, 1942 from the Mas d'Alary Member levels in Fialhomme wood (Debriette and Gand, 1990) and the Salagou Fm. (near Octon).
- Resting coffee bean-shaped traces Isopodichnus minutus Debriette and Gand, 1990, and Isopodichnus furcosus Gand, 1994 from the Rabejac and Salagou Fm.
- Walking/nating tracks: Acripes (Matthew, 1910) Walter 1983 also found in the whole Permian series are particurlarly common in the Salagou Formation. Triopsids are the trackmakers; (See Gand et al., 2008).
Five species of Phyloblatta and one of Opsimylacris species are recognized (Fig. 17), similar to those observed at the Obora locality of the Boskovice Furrow (Czech) and in the Wellington Fm of the Kansas (Schneider, 1980, 1984a, b). Fragments of about 2 cm long fore wings from Arieges show first indications of a V-shaped cross-veneation pattern, which is typical of the genus Aisoblatta. This latter appears, possibly, first in the Uppermost Kungurian and is typical of the German Zechstein and the Upper Permian of China (Schneider, 1983, 1996). Blattoid insects of the Salagou Fm suggest a Kungurian to lower Lopingian age.
[FIGURE 16 OMITTED]
The fossil-bearing strata are distributed between the R 300-R 800 reper levels (Fig. 4). The palaeoentomofauna is known from more than 700 specimens, and appears very diverse. Around 12 orders are represented, 3 Palaeoptera (Palaeodictyoptera, Odonatoptera, Diaphanopterodea), 9 Neoptera (Blattaria, Orthoptera, Glosselytrodea, Neuroptera, "Protorthoptera", Caloneurodea, Miomoptera, Protelytroptera, Hemiptera). Four others are of uncertain affinities.
The following insects were described from the Salagou Fm; Lapeyria magnifica Nel et al., 1999a (Odonatoptera: Panodialata: Lapeyriidae); Epilestes gallica Nel et al., 1999c (Protozygoptera: Permolestidae); Lodevia longialata Nel et al., 1999c (Protozygoptera: Permepallagidae), Saxonagrion minutus Nel et al., 2000b (Odonatoptera: Panodonata: Zygoptera: Saxonagrionidae); Orthoptera: Tettigoniidea; Glosselytrodea ... (Bethoux, 2001-2005).
The Odonatoptera are mainly 'Meganisoptera' with several new species of Meganeuridae: Typinae (See Nel et al, 2008). If Protozygoptera are represented, although less abundant than the Typinae, the Permian suborder Protanisoptera is still unknown in the outcrops.
[FIGURE 17 OMITTED]
[FIGURE 18 OMITTED]
Archaeorthoptera are represented by several families and species, described in numerous papers by Bethoux et al. (2001-2004).
Hemiptera occur in the shape of a 'cercopoid-like' wing and a Cicadomorpha: Prosbolidae, the latter being already known from the Late Permian of Russia and Siberia. The same is true for Protelytroptera which are reported for the first time in France.
The Endopterygota include several species of Mecopterida and Neuroptera. Coleoptera, Raphidioptera, Megaloptera have still not been found in the Lodeve basin sites whereas they exist in the Early and Middle Permian of Siberia and of USA.
Curiously, for this time, only a few samples of Lithographus, a walking insect track, were found, although numerous wings and sometimes body fossils have been gathered in the Saxonian Group (Gand et al., 1987; see Gand et al., 2008).
For this time, the palaeoentomofaunal material is almost limited to wings, broken frequently. The body remains found in rills/channels belong to adults. Current taphonomic hypothesis concerning the Salagou Fm formation suggests that animals were dislocated before fossilisation and exposed for a variable time, on areas, close to the fossiliferous sites. After that, sedimentologic events concentrated insects in rills/channels. Possibly, rain and wind or running waters accumulated organic remains in small depressions, during drying periods.
Absence of larvae, in spite of numerous remains of Odonatoptera, should have several possible origins. They could be developped in different areas or fossiliferous events could have been seasonal, when larvae were absent. But, this seems unlikely because of various different living insect larvae are developing during all the year. May be, also, the delicate larvae bodies were easily destroyed by necrophagous than those of adults.
[FIGURE 19 OMITTED]
Footprints (Figs. 5, 18, 19).
Near "la Lieude", on a slab surface, more than one thousand of footprints are distributed in twenty trackways which mesures to 220 m in length. They have been found on one calcareous siltstone level in the site. This latter is located in the Saxonian summit of the Salagou Formation, Fig. 4, 5).
Gand et al. (2000) have distinguished following ichnotaxa: Lunaepes ollierorum,, Merifontichnus thalerius, Planipes brachydactylus and Brontopus circagiganteus. All are attributed (with possibility or probability) to Therapsida or to "Therosauria", except Brontopus circagiganteus that could be due to Caseids. All these animals of 1 to 5 m long, lived in a playa environment. The biological and sedimentological data infered from "la Lieude" footprint levels compared with those provided by the track orientations, suggest that most of the animals crossed a sandy channel bank with plants and walked toward the South for the majority. They could go to the lake of the playa, close to "la Lieude" footprints area, they have just trampled on.
In the "la Lieude Member", Ellenberger (1983a) mentionned some bone beds, but without giving precise locations. In 2001, Frank Korner discovered elements of a probable Pelycosauria in the Salagou river border. Under a working European convention (Gand et al., 2000), since this discovery, excavations are organized by one of us (GG) to extract other skeletal remains. Thus a Tupilakosaurid amphibian have been recently found and described (Werneburg et al., 2007).
Large, continuous outcrops and dense borehole network for Uranium exploration, allow to constrain the second sedimentary cycle of the Lodeve Permian basin. This latter corresponds to a large playa system bordered to the south by a major synrift normal fault, and onlapping both previous Upper Carboniferous sediments and the Hercynian basement in the Northern and the Eastern part of the basin.
Playa sediments of the central part of the E-W elongated half-graben basin turn westward in stacked, thick debris-flow dominated alluvial fan sequences sealing the hanging-wall of an active normal fault along the Orb valley. Alternating arid and humid cycles, on the thick lateritic profiles developed on the drainage basin of the Montagne Noire Hercynian belt controled the periodic flooding of the playa system. During more humid periods, large amount of debris and red clays are vehicled as high density bedload by an ephemeral stream network, and they are expended as extensive thinning upward sheetflood sequences at the playa base level. This metre to decametre-thick climatic cycles record successive inundation-emersion sequences (moonson-like regime?), with a global increase of aridity during the deposition of the lower part of the Salagou Fm, followed by a reverse tendency on the upper part.
The playa sequences reach about 2000 m of total thickness in the hanging-wall of the southern bordering fault, recording the overall synrift differential subsidence of the basin during about the Upper Cisuralian to Lower Lopingian time.
Traces of life of the Lodeve Permian playa were firstly described, in part, as animal tracks and feeding burrows developed on sub-emersive surfaces, and as roots and poorly preserved plant debris at the top of flooding sequences. More recently, a particularly abundant and well preserved invertebrate fauna (thousands of body-fossils, and hundreds of insect wings) were discovered, trapped in silty fossiliferous rills associated to watertable rise and subtile washing and streamean power cleaning of rainwaters on desiccated surfaces. All the insect orders described elsewhere (USA, Russia) are represented here by several families and species. In particular, a 50 cm wingspread Odonata have been discovered in these traps.
This ephemeral ponded micro-environments favoured the seasonal development of small crustaceans like Conchostraca and Notostraca. The latter gives numerous swimming and furrowing traces on subaerial surfaces, delicately fixed by cyanobacterial mats. These short-live blums argue for the aridity of the climate during this period.
Subaerial surfaces expose numerous vertebrate tracks, and more particularly reptilian footprints, with an enigmatic overall increase of their size from the base to the top of the series. At the base, in the Rabejac Fm, both reptilians (Pelycosauria, Parareptilia, Lepidosauria), and amphibians (Temnospondyls) show a moderate size ranging from decimetric to metric; the latters being less abundant and diversified. On the contrary, the upper part of the Salagou Fm is dominated by mammalian reptiles and in particular, pluri-decimetric footprints of large, weighty herbivorous preserved on river bank deposits. Recent European fieldworks, in the vicinity of the outcrops of vertebrate tracks, yielded Pelycosauria bones dispersed into a muddy, debris-flow deposit, arguing for the periodic colonization of vegetaded areas of the playa by herbivorous herds.
Received: 13/05/07/Accepted: 25/09/07
Becq-Giraudon, J. F. (1973): Etude geologique du bassin houiller de Graissessac. Bulletin du Bureau de la Recherche Geologique et Miniere, 2 (1): 151-163.
Bethoux, O. (2003): Evolution des Archaeorthoptera (Insecta: Neoptera) du Paleozoique superieur au Mesozoique inferieur. Diversite taxonomique, disparite morphologique, paleoecologie. These de Paleontologie presentee au Museum d'Histoire Naturelle de Paris, 2 tomes: 213 p + 300 p.
Bethoux, O., Nel, A., Gand, G., Lapeyrie, J. (2001): Surijoka lutevensis nov. sp.: the first Glosselytrodea (Insecta) from the Upper Permian of France (Lodeve basin). Geobios, 34 (4): 405-413.
Bethoux, O., Nel, A., Gand, G., Lapeyrie, J., Galtier, J. (2002): Discovery of the genus Iasvia Zalessky, 1934 in the Upper Permian of France (Lodeve basin) (Orthoptera: Ensifera: Oedischiidae). Geobios, 35: 293-302.
Bethoux, O., Nel, A., Lapeyrie, J., Gand, G., Galtier, J. (2002): Raphogla rubra n. gen., n. sp.: the oldest representative of the clade of modern Ensifera (Orthoptera: Tettigoniidea and Gryllidea). European Journal of Entomology, 99: 111-116.
Bethoux, O., Nel, A., Lapeyrie, J., Gand, G., Galtier, J. (2003): New Martynoviidae from the Permian of Southern France (Lodeve basin) (Insecta: Palaeoptera: Diaphanopterodea). Geobios, 36: 131-139.
Bethoux O., Nel A., Galtier, J., Lapeyrie, J., Gand, G., (2003): A new Tococladidae (Insecta: Archaeorthoptera) from the Permian of south France. Geobios, 36, 3: 275-283.
Bethoux O., Nel, A., Lapeyrie J., Gand, G., (2003): The Permostridulidae fam. n., a new enigmatic insect family from the Upper Permian of France. European Journal of Entomology, 100 (4): 581-585.
Bethoux, O., Nel, A., Lapeyrie, J. (2004): The extinct order Caloneurodea (Insecta): Pterygota: Panorthoptera): wing venation, systematics and phylogenetic relationships. Annales Zoologici, 54 (2): 289-318.
Bethoux O., Nel, A., Lapeyrie, J., Gand, G. (2005): New data on Paleozoic Grylloblattid insects (Neoptera). Journal of Paleontology, 79 (1, 3): 125-138, 629-630.
Bethoux, O., Nel, A., Schneider, J., Gand, G. (2007): Lodetielle magnifica nov.gen. and nov.sp. (Insecta: Palaeodictyoptera; Permian), an extrem situation in wing morphology of palaeopterous insects. Geobios, 40: 181-189.
Blackwelder, E. (1931): Desert Plains. Journal of Geology, 39: 133-40.
Broutin J., Chateauneuf J., Galtier, J., Ronchi, A. (1999): L'Autunien d'Autun rest-t-il une reference pour les depots continentaux du Permien inferieur d'Europe? Apport des donnees paleobotaniques. Geologie de la France, 2: 17-31.
Chateauneuf, J.J, Farjanel, G. (1989): Synthese geologique des bassins permiens francais, Memoire du Bureau de la Recherche Geologogique et Miniere, Orleans la Source, 128: 28 p.
Debriette P., Gand, G. (1990): Consequences stratigraphiques et paleoenvironnementales de nouvelles observations paleontologiques dans le Permien de la partie occidentale du bassin de Lodeve (Sud du Massif Central). Geologie de la France, 1: 19-32.
Delage, A. (1912): Empreintes de grands pieds de quadrupedes de l'Herault. Memoire de l'Academie des Sciences et Lettres de Montpellier, 49 p. Doubinger, J. (1956): Contribution a l'etude des flores Autuno-Stephaniennes. Memoires Societe Geologique de France, 35 (75): 180 p.
Doubinger, J. (1963a): Notes palynologiques sur le Permien de Lodeve (Herault). Compte Rendu sommaire de la Societe Geologique de France, 6: 201-203.
Doubinger, J. (1963b): Nouvelles observations sur la flore fossile de l'Autunien de Lodeve. Compte Rendu sommaire de la Societe Geologique de France, 3: 74-75.
Doubinger, J, Heyler, D. (1959): Note paleontologique sur le Permien de Lodeve et de Bourbon-L'Archambault. Bulletin de la Societe Geologique de France, 7 (1): 304-311.
Doubinger, J, Heyler, D. (1975): Nouveaux fossiles dans le Permien francais. Bulletin de la Societe Geologique de France, 17: 1176-1180.
Doubinger, J., Kruseman, G. P. (1965): Sur la flore du Permien de la region de Lodeve <<zone de transition>> et Saxonien inferieur. Bulletin de la Societe Geologique de France, 7 (7): 541-548.
Doubinger, J., Odin, B., Conrad, G. (1987): Les associations sporopolliniques du Permien continental du bassin de Lodeve Herault, France: caracterisation de l'Autunien superieur, du <<Saxonien>> et du Thuringien. Annales de la Societe Geologique du Nord, 56: 103-109.
Echtler, H., Malavieille, J. (1990): Extensional tectonics, basement uplift and Stephano-Permian collapse basin in a late Variscan metamorphic core complex (Montagne Noire, southern Massif Central), Tectonophysics, 177: 125-138.
Ellenberger, F., Ellenberger P. (1959): Quelques pistes de vertebres du Permien inferieur de Lodeve. Comptes Rendus de l' Academie des Sciences, Paris, Paris, 248: 437.
Ellenberger, P. (1983a): Sur la zonation ichnologique du Permien moyen (Saxonien du bassin de Lodeve, Herault). Comptes Rendus de l' Academie des Sciences, Paris, 297, serie II: 553-558.
Ellenberger, P. (1983b): Sur la zonation ichnologique du Permien inferieur (Autunien du bassin de Lodeve, Herault). ComptesRendus de l'Academie des Sciences, Paris, 297 (II) vena transversa (sub-): 631-636.
Ellenberger, P. (1984): Donnees complementaires sur la zonation ichnologique du Permien du Midi de la France (bassins de Lodeve, St Affrique et Rodez). ComptesRendus de l'Academie des Sciences, Paris, 299, II, 9: 581-586.
Falconnet, J. (2006): Redescription d'Aphelosaurus lutevensis Gervais 1859 (Diapsida, Araeoscelidia) du Permien de Lodeve. Implications phylogenetiques et morpho-fonctionnelles. Memoire de Master 2, UMR 5143 CNRS, Departement Histoire de la Terre, Museum national d'Histoire naturelle, inedit, 43 p.
Feys, R., Greber, C. (1972): L'Autunien et le Saxonien en France. In: H. Falke (ed.), Rotliegend. Essays on european Lower Permian. E. J. Brill, Publisher, Leiden: 114-136.
Florin, R. (1938-1945): Die Koniferen des Oberkarbons und des unteren Perms. Palaeontographica, B, 85, 1-8, 1 - 729.
Galtier, J., Broutin, J. (1995): La flore de la Zone de Transition de l'Autunien Superieur de Lodeve. Sciences Geologiques, 48 (1-3): 83-93.
Galtier, J., Broutin, J. (2008): Floras from red beds of the Permian Basin of Lodeve (Southern France). Journal of Iberian Geology, 34(1): 57-72.
Gand, G. (1985): Significations paleobiologique et stratigraphique de Limnopus zeilleri dans la partie nord du bassin de Saint-Affrique. Geobios, 18 (2): 215-227.
Gand, G. (1986): Interpretations paleontologique et paleoecologique de quatre niveaux a traces de vertebres observes dans l'Autunien du Lodevois Herault. Geologie de la France, 2: 155-176.
Gand, G. (1987): Les traces de Vertebres tetrapodes du Permien francais Paleontologie, Stratigraphie, Paleoenvironnements. These de Doctorat d'Etat, Universite de Bourgogne. Edit. Centre des Sciences de la Terre, 341 p.
Gand, G. (1990): Essai de reconstitution paleoenvironnementale et paleoecologique d'une partie du Nord du bassin de Lodeve (Herault, France) au Permien Inferieur. Geologie de la France, 4: 17-30.
Gand, G. (1994): Ichnocoenoses a Isopodichnus furcosus nov. ichnosp.dans le Permien du bassin de Lodeve, Massif Central, France. Geobios, 27 (1): 74-86.
Gand, G., Durand, M. (2006): Tetrapod footprint ichno-associations from French Permian basins. Comparisons with the Euramerican ichnofaunas. In: S. G. Lucas, G. Cassinis, J. W. Schneider (eds.), Non-Marine Permian Biostratigraphy and Biochronology. Geological Society, London, Special Publications, 265: 157-177.
Gand, G., Galtier, J., Garric, J., Schneider, J., Korner, F., Bethoux, O. (2004a): Les bassins carbonifere de Graissessac et permien de Lodeve. Livret-guide de l'excursion no 3, Congres de Sienne sur l'evolution structurale et stratigraphique des successions marines et continentales entre le Carbonifere tardif et le Trias, mai 2001. Bulletin de la Societe d'Histoire Naturelle d'Autun, 185: 7-40.
Gand, G., Galtier, J., Garric, J., Schneider, J., Korner, F., Bethoux, O. (2004b): Les bassins carbonifere de Graissessac et permien de Lodeve. Livret-guide de l'excursion no 3, Congres de Sienne sur l'evolution structurale et stratigraphique des successions marines et continentales entre le Carbonifere tardif et le Trias, mai 2001. Bulletin de la Societe d'Histoire Naturelle d'Autun, 186: 9-40.
Gand, G., Garric, J., Demathieu, G., Ellenberger, P. (2000): La palichnofaune de vertebres tetrapodes du Permien Superieur du bassin de Lodeve (Languedoc, France). Palaeovertebrata, 29: 1: 1-82.
Gand, G., Garric, J., Lapeyrie, J., (1997): Biocenoses a Triopsides (Crustacea, Branchiopoda) du Permien du bassin de Lodeve (France), Geobios, 30 (5): 673-700.
Gand, G., Garric, J., Lapeyrie, J. (2000): Convention d'etude du Permien des bassins de Lodeve et de Saint-Affrique. Bulletin de la Societe d'Histoire Naturelle d'Autun, 171: 7-16.
Gand, G., Haubold, H. (1984): Traces de Vertebres du Permien du bassin de Saint-Affrique Description, datation, comparaison avec celles du bassin de Lodeve. Geologie mediterraneenne, Marseille, 11 (4): 321 348.
Gand, G., Lapeyrie, J., Garric, J., Nel, A., Schneider, J., Walter, H. (1997): Decouverte d'Arthropodes et de Bivalves inedits dans le Permien continental (Lodevois, France).Comptes Rendus de l'Academie des Sciences,Paris, 325, 891-898.
Gand, G., Garric, J., Schneider, J., Walter, H. Lapeyrie, J., Thiery, A., Martin, C. (2008): Notostraca trackways in Permian playa environments of the Lodeve basin (France). Journal of Iberian Geology, 34(1): 73-108.
Garric, J. (1965): L'uranium dans le carbonifere et le Permien de Lodeve. Les minerais uraniferes francais. Institut national des Sciences et Techniques nucleaires, Presses Universitaires de France, Paris: 149-265.
Garric, J. (2001): Les rigoles fossiliferes du Saxonien du bassin de Lodeve. Bulletin de la Societe d'Histoire Naturelle d'Autun, 173: 7-48
Garric, J. (2007): Le passage du Stephanien a l'Autunien au nord-ouest de La Tour-Sur-Orb, a la limite du bassin de Graissessac et du bassin Permien de Lodeve (Herault- France). Bulletin de la Societe d'Histoire Naturelle d'Autun, 194: 29-51.
Geinitz H.B. 1861. Dyas oder die Zechsteinformation und das Rothliegende, Volume 1, Die Animalischen Ueberreste der Dyas. Wilhelm Engelmann, Leipzig, 130 p.
Haubold, H. (1970): Versuch einer Revision der Amphibien Fahrten des Karbon und Perm. Freiberger Forschungshefte, Leipzig, C 260: 83-109.
Haubold, H. (1971): Ichnia Amphibiorum et Reptiliorum fossilium. In: G. Fischer (ed.), Handbuch der Palaoherpetologie. Encyclopedia of Paleoherpetology. Stuttgart, 18: 123 p.
Haubold, H. (1984): Die Fossilen Saurierfahrten. Wittenberg Lutherstadt, Neue Brehm Bucherei, 230 p.
Haubold, H. (1996): Ichnotaxonomie und Klassifikation von Tetrapodenfahrten aus den Perm. Hallesches Jahrbuch fur Geowissenschaften, Halle, B 18: 23-88.
Henriot, O. (1988): Permis de Merifons. Etude geologique du Saxonien, Rapport final Cogema, inedit: 39 p.
Heyler, D. (1969): Vertebres de l'Autunien de France. Cahiers de Paleontologie du Centre National de la Recherche Scientifique, Paris: 255 p.
Heyler, D. (1997): Les vertebres permiens du bassin de Lodeve (Herault): bilan. Bulletin de la Societe d'Histoire Naturelle d'Autun, 157, 23-24, 5-28.
Heyler, D., Lessertisseur, J. (1963): Pistes de tetrapodes permiens dans la region de Lodeve Herault. Memoire du Museum d'Histoire Naturelle de Paris, C, 11, 2: 100 p.
Hoffmann, N., Kamps, H. J., Schneider, J. (1989): Neuerkenntnisse zur Biostratigraphie und Palaodynamik des Perms in der Norddeutschen Senke ein Diskussionsbeitrag. Zeitschrift fur Angewandre Geologie, 35 (7): 198-207.
Kruseman, G. P. (1962): Etude paleomagnetique et sedimentologique du bassin de Lodeve Herault. These de l'Universite d'Utrecht: 65 p.
Korner, F. (1999a): Dokumentation von Zyklen und Faziesmustern in der Viala-, Rabejac-und Salagou Formation des Lodeve-Beckens, S-Frankreich. Diploma-Geologe (inedit), Technische Universitat, Berakademie of Freiberg, Saxe: 87 p.
Korner, F. (1999b): Sedimentologie und Geochemie der PermKlastite des Lodeve Beckens (S-Frankreich): Fazies, Klima, Genese. Diplomarbeit, 87, TU-Bergakademie Freiberg.
Korner, F. Schneider, J. W., Hoernes, S., Gand, G., Kleebert, R. (2003): Climate and continental sedimentation in the Permian of the Lodeve Basin (Southern France). Bolletino della Societa Geologica Italaina,, Volume speciale, 2: 185-191.
Laversanne, J. (1976): Sedimentation et mineralisation du Permien de Lodeve Herault. These de troisieme cycle, Universite de Paris sud, inedit: 300 p.
Legler, B., Schneider, J., Gand, G., Korner, F. (2004): Playa and sabkha from northern Germany and Southern France. Workshop, IGCP 469 Central European Meeting "Freiberg 2004", Freiberg University, 64-82.
Linck, O. (1942): Die Spur Isopodichnus. Senkenbergiana, 25: 233-255.
Lopez, M. (1992): Dynamique du passage d'un appareil terrigene a une plate-forme carbonatee en domaine semi-aride: Le Trias de Lodeve, Sud de la France. These de Doctorat, Universite de Montpellier 2, 403 p.
Lopez, M., Gand, G., Garric, J., Galtier, J. (2005): Playa environments in the Lodeve Permian Basin and the Triassic cover (Languedoc- France). Excursion, 10-12 may 2005, Association des Sedimentologistes francais: 54 p.
Lopez, M., Mader, D. (1985): Gravelly and sandy braidplain, evolving into floodplain and playa-lake deposition and vice versa, in the Bundsanstein facies sediments and marine incursions, in the Triassic of the Lodeve region (southern France). In: D. Mader (ed.), Lecture Note in Earth Sciences, Berlin, Heidelberg, 4: 509-518.
Lopez, M., Marza, P., Merzeraud, G., Moussine, A. Seguret, M. (1997): Passage terrigene-carbonate et cyclostratigraphies en plate-forme interne: la transition Trias/Lias sur la bordure des Causses et ennoiement de la plate-forme liasique. Congres de l' Association des Sedimentologistes Francais, Montpellier, livret-guide: 49 p.
Lopez, M., Petit, J-P. (2003): Outcrop analogues for Carboniferous and Rotliegende Dutch Oilfiels in the Lodeve Permian Basin, South of France. Fieldtrip guidebook, inedit, Laboratoire Dynamique de la Lithosphere, Montpellier II, 84 p.
Martens, T. (1983): Zur Taxonomie und Biostratigraphie der Conchostraca (Phyllopoda, Crustacea) des Jungpalaozoikums der DDR, Teil 1. Freiberger Forschungshefte, C 382: 7-105.
Matthew, G.F. (1910): Remarkable forms ofthe little River Group. Royal Society of Canada Transactions, 3 (3-4): 115-125.
Moodie, R.L. (1929): Vertebrate footprints from the Red Beds of Texas I. American Journal of Sciences, New-Haven, 5, 17, 352-368.
Nel, A., Gand, G., Garric, J. (1999a): A new family of Odonatoptera from the continental upper Permian: the Lapeyriidae (Lodeve basin, France). Geobios, 32, 1: 63-72.
Nel, A., Gand, G., Fleck, G., Bethoux, O., Lapeyrie, J., Garric, J. (1999b): Saxonagrion minutus nov. gen. nov. sp., the oldest damselfly from the Upper Permian of France (Odonatoptera, Panodonata, Saxonagrionidae fam. nov.). Geobios, 32, 6: 883-888.
Nel, A., Gand, G., Garric, J., Lapeyrie, J. (1999c): The first recorded Protozygopteran insects from the Upper Permian of France. Palaeontolgy, 42 (1): 83-97.
Nel, A.N., Fleck, G., Garrouste, R., Gand, G. (2008): The Odonatoptera of the Late Permian Lodeve Basin (Insecta). Journal of Iberian Geology, 34(1): 115-122.
Nesbitt, H. W., Young, G. M. (1982): Early Proterozoic climates and plate motions inferred from major element chemistry of lutites. Nature, 299: 715-717.
Nmila A., Cabanis, B., Leroy, S., Henriot, O., Mathis, V (1992): Decouverte de nouveaux horizons tuffiques dans le Permien rouge superieur du bassin de Lodeve Herault, France. Essai de caracterisation du volcanisme. Comptes Rendus de l'Academie des Sciences, Paris, 315 (II): 689-696.
Nmila, A. (1995): L'empreinte du volcanisme dans le remplissage permien du bassin de Lodeve. Etude petrographique et geochimique. Implication metallogenique. These de Doctorat en Sciences, Universite Pierre et Marie Curie, Paris VI (inedit): 202 p.
Odin, B. (1986): Les formations permiennes Autunien superieur a Thuringien du <<bassin>> de Lodeve (Herault, France). These de Doctorat de l'Universite de Marseille III, specialite Geologie, 392 p.
Pochat, S., Van Den Driessche, J., Mouton, V., Guillocheau, F. (2005): Identification of Permian palaeowind direction from wave-dominated lacustrine sediments (Lodeve Basin, France). Sedimentology, 52: 809-825
Pohlig, H. (1886): Saurierfahrten im unteren Rotliegenden von Friedrichroda. Verhandlungen naturhistorische. Vereins der Preussischen Rheinlande und Westfalens, Bonn, 43: 277-279.
Roscher, M., Schneider, J. (2006): Permo-Carboniferous climate: Early Pennsylvanian to Late Permian climate development of central Europe in a regional and global context. In: S. G. Lucas, G. Cassinis, J. W. Schneider (eds.), Non-Marine Permian Biostratigraphy and Biochronology. Geological Society, London, Special Publication, 265: 95-136.
Saint-Martin, M. (1993): Evolution du bassin stephanien de Graissessac en relation avec les tectoniques hercyniennes et tardi-hercyniennes de la Montagne Noire (Sud du Massif Central francais). These de l'Universite de Montpellier (inedit), 234 p.
Sarjeant, W.A.S. (1971): Vertebrate Tracks from the Permian of Castle Peak, Texas. The Texas Journal of Science, 22, 4, 344-366.
Schneider, J. (1980): Zur Entomofauna des Jungpalaozoikums der Boskovicer Furche (CSSR), Teil 1: Mylacridae (Insecta, Blattodea). Freiberger Forschungshefte, Leipzig, H., C 357: 43-55.
Schneider, J. (1983): Die Blattodea (Insecta) des Palaozoikums, Teil 1: Systematik, Okologie und Biostratigraphie. Freiberger Forschungshefte, Leipzig, H C 382: 106-145.
Schneider, J. (1984a): Die Blattodea (Insecta) des Palaozoikums, Teil 2: Morphogenese der Flugelstrukturen und Phylogenie. Freiberger Forschungshefte, Leipzig, C 391: 5-34.
Schneider, J. (1984b): Zur Entomofauna des Jungpalaozoikums der Boskovicer Furche (CSSR), Teil 2: Phyloblattinidae (Insecta, Blattodea). Freiberger Forschungshefte, Leipzig, C 395: 19-37.
Schneider, J. (1996): Biostratigraphie des kontinentalen Oberkarbon und Perm im Thuringer Wald, SW-Saale-Senke Stand und Probleme. Beitrage zur Geologie von Thuringen, N.F., 3: 121-151.
Schneider, J., Gebhardt, U., Gaitzsch, B. (1995): Fossilfuhrung und Biostratigraphie. In: E. Pleine (ed.), Stratigraphie von Deutschland I. Norddeutsches Rotliegendbecken. Rotliegend-Monographie Teil II. Cour. Forsch.-Inst. Senckenberg, 183: 25-39.
Schneider, J., Korner, F, Hoernes, S. T., Gand, G., Schaeben, H., Kleeberg, R. (1999): Projekt Schu 408/7-1: Referenzprofil Kontinentales Oberkarbon bis Untertrias fur die Synthese Klima-relevanter geochemister, sedimentologischer und palaontologischer Daten. Teil 1. Perm-red beds des Lodeve-Beckens. Geochimie, Bio-/lithofazies, Zyklostrati graphie, Klima. Freiberg University, Allemagne (Unpublished): 48 p.
Schneider, J., Korner, F., Roscher, M., Kroner, U. (2006): Permian climate development in the northern peri-Tethys area: the Lodeve Basin, French Massif Central, compared in a European and global context. Palaeogeography, Palaeoclimatology, Palaeoecology, 240: 161-183.
Sumida, S., Berman, D. S., Martens, Th. (1996): Biostratigraphic correlations between the Lower Permian of North America and Central Europe using the first record of an assemblage of terrestrial tetrapods from Germany. PaleoBios, 17 (2-4): 1-12.
Vetter, P. (1963): Le bassin de Decazeville. Voyage d'etude no 4, livret-guide du Veme congres du Carbonifere (Inedit): 63-80.
Voigt, S. (2004): Die Tetrapodenichnofauna des kontinentalen Oberkarbon und Perm im Thuringer Wald-Ichnotaxonomie, Palaookologie und Biostratigraphie. Cuvillier Verlag Gottingen, 300 p.
Walter, H. (1983): Zur Taxonomie, Okologie und Biostratigraphie der Ichnia limnisch-terrestrischer Arthropoden des Mitteleuropaischen Jungpalaozoikums. Freiberger Forschung sheft, C 382: 146-193.
Werneburg, R., Steyer, J-S., Sommer, G. Gand, G., Schneider, W., Vianey-Liaud, M. (2007): The Earliest Tupilakosaurid amphibian with diplospondylous vertebrae from the Late Permian of Southern France. Journal of Vertebrate Paleontology, 27 (1): 26-30.
Zeiller, R. (1898): Contribution a l'etude de la flore pteridologique des schistes permiens de Lodeve. Bulletin du Museum de Marseille, 1: 68 p.
M. Lopez (1), G. Gand (2), J. Garric (3), F. Korner (4), J. Schneider (4).
(1) Laboratoire Dynamique de la Lithosphere, UMR 5573, Universite de Montpellier II, Case 060, 34095 Montpellier Cedex 05 (France), e-mail: Michel.firstname.lastname@example.org
(2) Laboratoire Biogeosciences, Universite de Bourgogne, CNRS; 6, Bd Gabriel, 21000 Dijon (France)
(3) Jacques Garric, 16 rue des Azalees, la Chamberte, 34070 Montpellier(France)
(4) Freiberg University, Department of Palaeontology, Institute of Geology, Bernhard-von-Cotta street 2; D-09596 Freiberg (Germany).
|Printer friendly Cite/link Email Feedback|
|Author:||Lopez, M.; Gand, G.; Garric, J.; Korner, F.; Schneider, J.|
|Publication:||Journal of Iberian Geology|
|Date:||Jan 1, 2008|
|Previous Article:||Playas del Permico y del Cuaternario: una discusion basada en los marcos climatico, tectonico y paleogeografico.|
|Next Article:||Floras en las capas rojas de la cuenca permica de Lodeve (Sur de Francia).|