Playas del Permico y del Cuaternario: una discusion basada en los marcos climatico, tectonico y paleogeografico.
A major effort is under way to reconstruct past climatic changes to help predict physical and biologic responses to climate. The planet Earth is already experiencing the impacts of these changes on biodiversity, freshwater resources and local livelihoods. Glacier melting, sea-level rise and desertification in the tropical regions (Fig. 1) are the major problems to be solved. For the study of global climate, the interest of the Late Carboniferous to Permian time-span (Ludwig, 1988; Fluteau et al2001; Chumakov and Zharkov, 2003) and this from the latest Permian to Early Triassic as well (Kiehl and Shields, 2005; Woods, 2005) has been emphasised. The tectonic influence on climate has been evidenced either during Carboniferous to Triassic times (Oyarzun et al., 1999) or simply for the Late Carboniferous to Early Permian interval (Glover and Powell, 1996). Fluteau (2003) provided with an extended synthesis for the Phanerozoic. More recently, Roscher and Schneider (2006) synthetized the climate setting of the Late Carboniferous and Permian, considering some major geodynamic aspects such as the closure of the Rheic ocean. Moreover, they proposed for the Variscan orogen a lower elevation (about 2000 m) than previously assumed (Becq-Giraudon and Van den Driessche, 1994).
The Late Carboniferous-Permian-Early Triassic times record the transition from a cold interval, approximately ending during the Early Permian (Table 1), characterised by repeated periods of extensive glaciation and deglaciation affecting the southern Gondwana, to a warm-climate interval, prolonged during the whole Mesozoic and a major part of the Cenozoic until the Quaternary cold events. The most extensive Phanerozoic glaciation lasted about 90 My and its termination occurred during the Sakmarian on the southern border of the Gondwana supercontinent (Visser, 1993).
[FIGURE 1 OMITTED]
Consequently, Late Carboniferous to Early Permian has been considered as the best available analogue to the Recent (DiMichele et al., 2001). During that period, Laurasia and Gondwana became welded together to constitute the supercontinent Pangaea rimmed by a broad and unique watermass, the Panthalassic ocean or Panthalassa (Fig. 2). Recent advances in palaeogeographic reconstructions ask for reconsidering the global tectonic evolution (Scotese, 2001; Stampfli and Borel, 2002; Torsvik and Cocks, 2004). A major worldwide geodynamic event, the Variscan orogeny sensu lato, culminated during the Permian. From the Visean onward, mantle-derived activity indicated lithosphere thinning and post-orogenic crustal extension (Lorenz and Nicholls, 1984; Matte, 1986; Bonin, 1998; Stampfli et al., 2002). The European segment, the so-called Variscan belt sensu stricto or Hercynian belt, was formed by the collision of Gondwana and Laurasia. This sketch is complicated by the subduction of the north-western Palaeotethys along an active margin. The major collisional effects ceased during the Late Carboniferous. During the Permian, the Scythian belt was formed (Natal'in and Sengor, 2005), Laurasia-Kazakhstan collision produced the Uralian belt (Matte, 2002), whereas Kazakhstan and Eastern Siberia led to the Central Asian belt (Nikishin et al., 2002; Van der Voo et al, 2006), also named Altaids or Mongolian belt. These events culminated during the Middle Permian. Some tectonic movements occurred also during the Late Permian, particularly in eastern Eurasia. In the Alleghanian orogeny (Hatcher, 2002), the major tectonic activity occurred first in the Early Carboniferous (Mississipian) with the closure of the eastern Rheic ocean due to the collision of Gondwana and part of North America and, second, between the Late Carboniferous (Pennsylvanian) and the Early Permian, more precisely the Late Sakmarian, with the collision of South America and southern North America, forming the Ouachitas. The Gondwanan segment or 'Mauritanides' is less known and time-constrained. One other problem is the place of North Gondwana (current Africa) and the transition from the Alleghanides to the Eurasian Variscides. Indeed, in northern Africa the chronology of the Late Palaeozoic tectonics is not well established such as in the Moroccan Meseta and also in the Anti-Atlas where there is a lack of Late Carboniferous and Permian deposits (Burkhard et al., 2006).
[FIGURE 2 OMITTED]
Therefore, during the Middle Permian, there is probably a worldwide culmination of the orogenic deformations for the Phanerozoic (Khain and Seslavinsky, 1992; see also Table 1). Granitization appears as a major geodynamic marker for the Middle and Late Permian, particularly in America and Asia. The opening of the Neotethys initiated also during the Early Permian (Fig. 2), characterised by the drift of the Cimmerian blocks (Cimmerian continent?) from the Gondwana toward the northern margin of the Palaeotethys (Ziegler and Stampfli, 2001; Stampfli and Borel, 2002).
The global aridity of the Permian and Triassic Pangaea, including some high latitude areas, could be explained by the particular distribution of land- and watermasses. Geochemical variations of unusual amplitudes occurred during the Permian (Scheffler et al., 2003) and particularly at the Permian-Triassic boundary interval (PTBI) (Baud, 2005). Geochemical elements, such as oxygen or sulphur, show extreme negative or positive excursions, revealing major changes on the continent and in the ocean where the general circulation should be affected (Winguth and Maier-Reimer, 2005). This unique Phanerozoic setting ended with the major biological crisis close to the PTBI.
The present paper focuses on playas. This typical landform could be easily defined in the present-day arid and semi-arid landscapes. Ancient playa environments are more difficult to decipher, although they have been documented in a number of places of different stratigraphic ages. One of the oldest playa is probably that identified by Simpson et al. (2004) in the Palaeoproterozoic of South Africa. Playa facies have been proposed for Uppermost Neoproterozoic (Vendian) deposits of Svalbard (Fairchild and Hambrey, 1995). Generally, a few examples of saline pan deposits has been described in the Precambrian. On the contrary, playa mudflats, perennial lakes and ephemeral stream environments are very common in the 'Old Red Sandstones' (Devonian) (e.g., Clarke and Parnell, 1999). After the Carboniferous, a stratigraphic system poor in playas, the Permian and Triassic are conversely the richest in that kind of environment. However, playas still remain relatively rare in the Early Permian, for example in the Salagou Fm of the Lodeve basin, Nahe Subgroup of the Saar basin or the Hornburg Fm of the Saale basin (Schneider and Gebhardt, 1993; Schneider et al., 2006), and in the Orobic Alps (Cassinis et al., 1986; Cadel et al., 1996). Permian playas develop in the middle Early Permian (Schneider and Gebhardt, 1993; Roscher and Schneider, 2006) and become more and more common in the Middle and Late Permian (Gand et al., 1997; Freytet et al., 1999) and in the Triassic (e.g. Paul and Peryt, 2000). More generally, during the Permian the widening of closed drainage areas on land reduced the transport of organic and mineral nutrients to seas (Chumakhov and Zharkov, 2003). Playa environments are also very common from the Jurassic (Spalletti and Pinol, 2005) to the Present, a period characterised by global temperate climate conditions. Since the amalgamation of almost all continental terranes into the Pangaea supercontinent, plate tectonics radically altered the distribution of landmasses. Regional climates developed, and current arid conditions prevail in tropical areas but also close to the equatorial regions, such as in Peru, NE Brazil, Somalia, Kenya etc. (Fig. 1).
[FIGURE 3 OMITTED]
As a result of their low density and high solubility, evaporites play key roles in some geological processes and particularly in the crustal deformation. Sometimes, thick Permian evaporitic sequences could be recognised, such as in the Zechstein sea (Langbein, 1987; Hryniv and Peryt, 2003), but their marine origin is clear and only some paralic facies could be considered as actual playas such as in the Late Permian of NE England (Turner and Smith, 1997). Using the example of Chott el Djerid, Tunisia, Bryant et al. (1994) have shown that as an ephemeral lake shrank, brine produced could be similar to modern sea water. Thus, evaporites alone can not be considered as the evidence of playa, as illustrated by the evaporites of the Messinian crisis, which are linked with evaporation in a deep basin-shallow water model (Rouchy and Caruso, 2006) and do not indicate playa environments.
2. The playa environment
2.1 The current playas and their setting
The Spanish name playa, which literally means 'beach', was initially used in Mexico and U.S. Southwest (e.g. Hamilton, 1951). This morphology, also named 'alkali flat' or 'salt pan', describes a flat-bottom depression periodically covered by water (Fig. 3). This water could either slowly filtrate into the ground water system or evaporate into the atmosphere, both causing the deposition of evaporites, sand, and mud as well. Briere (2000) stipulates that a playa, as a discharging intracontinental basin, remains dry at least 75% of the year. Typical sites of playa environments are known at Black Rock Desert in Nevada and the Bonneville Salt Flats in Utah. Nevertheless, alkali flats are very common, particularly in the driest regions of Asia such as the Qaidam Pendi or Qaidam desert in Western China (Fig. 4B), in Southern America and particularly in the Atacama desert (Flint, 1985; Hartley and Chong, 2002; Hartley, 2003), in the arid regions of Australia -- the Lake Eyre Basin, including much of the landmass of arid inland Australia drains into it, is the largest modern endorheic system in the world (Magee et al., 2004) -- in the Middle East and in northern Africa. They also exist in temperate zone, for example at Laguna de Playa in the central Ebro basin, NE Spain.
[FIGURE 4 OMITTED]
Therefore, playas or alkali flats constitute large zones of aggradation in semiarid or arid regions. The flat-floored desert depression, usually centred on the playa and surrounded by mountains, is named bolson, from the Spanish bolson, which means 'large purse' (Fig. 3). Basically, it is necessary to consider the playa as a whole, including the bolson (Fig. 4A). This type of basin characterises Basin-and-Range structures. If developed under certain conditions of aridity, the centre of the playa could be occupied by a shallow intermittent endorheic lake, the so-called sabkha lake, sometimes but inadequately named playa lake. Some authors consider that sabkha -- or sebkha -- would be marine influenced, whereas playa would be only continental (e.g., Bates and Jackson, 1987; Briere, 2000). For us, this definition is inappropriate because some typical current sabkhas, such as the 'Sebkha Mekerrhane', Algeria, are far away from the sea (see also Fig. 6). According to seminal works (e.g., Coque, 1962) we consider here the sabkha as the centre of the endorheic system. Some evaporite-free coastal playas, the so-called khabras, are linked with variations of the sea level, in Eastern Oman for example. Others are related to the dissolution of continental salts, such as the Zone of Chotts in Tunisia (chott meaning 'shore' in arabic).
In the salt pan, evaporites are deposited due to the concentration by evaporation of natural solutions of salts (Warren, 1999). Such areas consist of fine-grained sediments including colloids and clays infused with alkali salts. The least soluble salts (calcium and magnesium carbonates) precipitate first, on the outside of the pan, followed by sodium and potassium sulphates. Finally, in the centre of the playa, sodium chlorides, potassium chlorides, and magnesium sulphates are deposited. Associated to sodium chlorides, sodium and potassium carbonates could be concentrated in alkali sabkha lake, such as the current Lake Magadi in the Eastern Rift Valley, Kenya. The most common minerals are halite, gypsum (or its water-depleted form, the so-called bassanite), anhydrite, primary dolomite, and sodium sulphates. While the alkali flat itself will be devoid of vegetation, flats are commonly ringed by salt-tolerant plants, forming a halophytic steppe, the famous 'chott' stricto sensu. Therefore, the vegetation-free character indicated by Bates and Jackson (1987) is not relevant for defining a playa.
Some of the present-day playas obviously suffer a tectonic influence. For example, the Zone of Chotts, region of the Presaharian Tunisia, is situated in a series of tectonically controlled depressions that lie between the Atlas Mountains and the Saharan Platform, along a structural line, the so-called Sillon Tunisien or Tunisian trough, linking the Tripolitania trough, Libya, to the East, to the Chott Merouane-Chott Melrhir, Algeria, to the West (Burollet, 1991). In such areas, subsidence phenomena are superimposed to the evaporation and deflation processes. Nevertheless, evaporite deposits are not necessarily linked with tectonics (Rouchy et al., 2001). For example, elevation and strong evaporation could explain the presence of the famous Salar of Uyuni in the Bolivian Altiplano. Salar means salt pan in Spanish and, therefore, is equivalent to sabkha. In addition, hypersaline systems are known in current polar regions.
Finally, it should be emphasised the interest of the playa as a palaeoenvironmental marker. This landform characterises the aridity of the area under investigation, any extrapolation in terms of palaeolatitudes being more difficult.
2.2. The Permian playas
2.2.1. Evidences and location of the Permian playas
Permian times represent not only a key period for understanding the Late Variscan tectonic evolution (e.g. Khain and Seslavinsky, 1992; Nikishin et al, 2002; Deroin and Bonin, 2003), but also for studying palaeoclimates (e.g. Fluteau et al., 2001; Roscher and Schneider, 2006). During the Permian and the Triassic as well, a worldwide development of deserts could be emphasised in a number of Pangaean places. But, whereas arid facies should be inferred, real playa environment are sometimes difficult to evidence. If evaporites are used as markers for the Permian playas, the following regions should be cited: Southern America, South-West north America, Central Asia, etc. (Fig. 2).
Some authors have depicted the North American equatorial region as predominantly everwet. Nevertheless, as early as 1964, Briden and Irving recognised eolian sandstones and evaporites in the western equatorial Pangaea. Equatorial aridity during Early Permian has been specifically dealt with by Kessler et al. (2001) and shifts in Late Palaeozoic atmospheric circulation in that region have been documented by Tabor and Montanez (2002). A synthesis of the Permian facies of the USA has been done by Mazzullo (1995). In Texas, coastal sabkha and salt pan deposits have been inferred by Handford (1981). More recently, Dickson et al. (2001) working in West Texas examined Late Permian continental calcite and saddle dolomite cement. This cement has 87Sr/86Sr values lower than those known for contemporaneous marine carbonates. This is interpreted by the authors as the evidence of the presence of hypersaline brine during diagenesis. Anderson and Dean (1995) and Kirkland et al. (2000) detailed some aspects of the evaporitic series in the Late Permian of the Delaware Basin. Benison and Goldstein (2000) studied the sedimentology of ancient Permian saline pans in North Dakota. Acid saline lake deposits have even been proposed as analog of the Martian strata (Benison, 2006). In Arctic North America, Beauchamp (1995) has also emphasised the importance of evaporitic deposits.
In Southern America, part of Gondwana, Permian evaporites are frequent, particularly at the top of the Late Paleozoic, for example in the Upper section of the Paganzo Group, Argentina (Limarino et al., 2006). The Permian-Triassic sedimentary facies have been correlated with both tectonics (Zerfass et al., 2004) and palaeoenvironment (Zhang et al., 1998).
In Europe, there is a considerable amount of references concerning Permian geology (e.g., Cassinis et al., 1995; Cassinis, 2001; Virgili et al., 2006). These numerous references include the seminal works using the French (Autunian, Saxonian, Thuringian) and German terminology (Rotliegende, Zechstein). Facies such as the so-called 'Saxonian' and 'Zechstein' characterise the continental and marine shallow-water facies, respectively. In the same areas, Late Triassic is the realm of large-scale evaporites (Keuper). It exists an old and general consensus about the existence of wet conditions during the very Early Permian continuing palaeoenvironments developed during the uppermost Carboniferous. With the north oriented drift of Laurasia, Europe suffered tropical conditions as early as the Guadalupian and until the PTBI. Driest facies appeared in the Middle (Guadalupian) and Late Permian (Lopingian). For example, the Uppermost Dethlingen and Hannover Formations (Capitanian-Wuchiapingian according to Schneider et al, 2006) represent an evaporitic playa mud flat environment with associated perennial playa lake and salt flats. The facies distribution is the result of a complex interplay of climate and tectonism. The recent synthesis by Schneider et al. (2006) also precises that several short phases of increased humidity could temporarily interrupt the general trend, especially during the Wuchiapingian (lower part of the Lopingian) as well (Table I). These phases could correspond to the last pulses of the major Permo-Carboniferous glaciation.
[TABLE 1 OMITTED]
The Early and Middle Permian are uniquely represented by continental deposits. In France for instance, most of the Permian basins show evidence of arid environments (Chateauneuf and Farjanel, 1989, Deroin et al., 2001). Nevertheless, in Europe evaporites are rare. It is possible to mention the Eisenach Formation (KungurianRoadian) of the Thuringian Forest Basin, Germany, or the Chotevice Formation (Kungurian) of the Krkonosepiedmont Basin, Czech Republic (Schneider et al, 2006). The same trend could be described in Spain (Arche and Lopez-Gomez, 2005), British Islands, Germany (Roscher and Schneider, 2006), Italy (Cassinis, 2001) and particularly Sardinia (Pittau and Del Rio, 2004), North Sea (Martin et al., 2002), the Czech Republic, Poland, Bulgaria (Yanev, 2000), Russia, Ukraine, etc., where "New Red Sandstones" characterised Late Palaeozoic intracratonic basins.
Playa facies are generally devoid of any biostratigraphical indicative fossils, but tetrapod footprints, and also insects, concostracans, plant remains, etc. appear in places very common. Such a sedimentology and palaeontology as well are consistent with dry conditions during the Middle Permian (Guadalupian). Playa environment dominates and is associated with aeolianites and rare evaporites. Thus, no large-scale evaporitic deposits are known in the Cisuralian and in the Roadian as well. On the contrary, Wordian and Capitanian (Upper Rotliegend II) and Zechstein present a great amount of marine evaporites especially in the Southern Permian Basin, which extended from England to North Germany and Poland, and in the Zechstein Sea. Legler et al. (2005) have shown that the mega-playa system of the central Southern Permian Basin has been temporary flooded by marine ingressions. Evaporites are also frequent in central Eurasia (Chuvashov, 1995) and largely developed in the eastern regions such as the Kungurian deposits of the Precaspian basin, Kazakhstan (Barde et al., 2002).
In the higher latitudes of Eurasia, the same sketch as been reported from the Norwegian-Greenland sea area (Stemmerik, 1995) and in the Barents shelf area as well (Stemmerik and Worsley, 1995). Therefore, from the Middle Permian onward, arid conditions prevail. These conditions characterised also the Triassic times as illustrated in the Early Triassic of the Thuringian sub-basin of the Germanic basin, where carbonate sedimentation took place in a playa lake environment with variable salinities (Paul and Peryt, 2000).
Rotliegend sequence stratigraphy in the Southern Permian Basin suggests climatically forced fluctuations in the level of an expanding playa lake system (Gast, 1991, Kiersnowski et al, 1995). The associated facies changes define essentially isochronous sequence boundaries. Spectral analyses of gamma ray logs have indicated that individual sequences display internal cyclicity consistent with orbital (Milankovitch) forcing. Confirmatory results have been reported from the spectral analysis of field logs from the continental Permian Brodick Beds of the Isle of Arran, England (Bailey, 2001).
In Northern Africa, the situation is very similar to that encountered in Spain or France (Medina, 1996; Hofman et al., 2000). Elsewhere in the North African craton, the same type of environment prevailed (Sidor et al., 2005). No Permian evaporites are known in southern Africa. Nevertheless, the Karoo supergroup perfectly illustrates the changes between a cold and semi-arid climate during the Late Carboniferous-earliest Permian interval to warmer and eventually hot with fluctuating precipitation during the most of Permian times (Stollhofen et al., 2000; Burgoyne et al., 2005).
3. Geochemical particularities of the Permian times
A number of studies evidence extreme geochemical conditions during Permian times and particularly at the Permian-Triassic boundary interval (PTBI). These geochemical variations could be related to major global changes leading from icehouse to hothouse conditions, probably mainly caused by a drop in atmospheric C[O.sub.2] to about five times present levels (Berner, 2006a), even if some authors argue that low atmospheric levels prevailed (Beerling, 2002). This Late Permian drop was brought about mainly by a decrease in the burial of terrestrial derived organic matter, but also with a possible contribution from the weathering of older organic matter on land (Berner, 2006b). The Early Triassic time is characterised by a quite different biological activity, and particularly the absence of large metazoan reefs. More generally, carbon isotopes provide interesting information for the continent landmass and for the marine environment as well (Krull et al., 2004).
Although a major attention has been placed on the PTBI where rapid environmental changes may occur, a longer period spanning at least 4 My also experienced a series of evolutionary events as evidenced by numerous extinctions and recoveries of terrestrial animals or plants (McAllister Rees, 2002; McAllister Rees et al., 2002; Burgoyne et al, 2005). In the meantime, multiple extinctions of marine organisms occurred and a sustained oceanic anoxia prevailed. In the aftermath of the major extinction, the fossils are characterised by an incredibly small size (Twitchett, 2006). It is noteworthy to consider the development of halotolerant bacteria at about 250 Ma (Satterfield et al, 2005).
The dramatic negative excursion of the rate in [delta][sup.34]S in the Late Permian is probably related to the extent of evaporites. High [O.sub.2] environment could have altered canopy transpiration rates and thefore water-use efficiency during the Permo-Carboniferous (Beerling and Berner, 2000). More generally, decreased [delta][sup.18]O revealed as early as the Early Permian is generally interpreted as a decrease in rainfalls. Nevertheless, increased C[O.sub.2] seemed to be the main parameter and evidenced the rapid episode of plant die-off (Smith, 1995). To explain such an increase in Permian atmospheric C[O.sub.2] different hypotheses have been proposed. The role of the volcanic activity (flood basalts), particularly that of the Siberian (Tunguska) and Emeishan traps, has been emphasised (Fig. 2) (Bin He et al., 2007). If this hypothesis is correct, it should be noticed that the C[O.sub.2] increase appeared as early as the Early Permian. In fact, there is few Early Permian datings for this volcanic activity and if developed from the Cisuralian onward, the traps were probably limited. A more general influence of the extensional tectonics as outgassing and C[O.sub.2]-releasing source should be taken into account.
[FIGURE 5 OMITTED]
4. Comparison between the Appalachian-Variscan-Uralian-Mongolian belt and the Alpine-Himalayan belt
A consensus exists regarding the presence of a mainly Palaeozoic ocean North of the Cimmerian continent, the Palaeotethys (Fig. 5), a younger late Palaeozoic-Mesozoic ocean located South of this continent, the Neotethys, and finally a middle Jurassic ocean, the Alpine Tethys, an extension of the central Atlantic ocean in the western Tethyan regions. Additional Late Palaeozoic to Mesozoic oceans complicate somewhat this relatively simple picture. Therefore, there are still some confusions about what Tethys existed at what time. The classical Pangaea A is consistent with field data and also with the supposed plate arrangement of the Jurassic prior to the onset of the Atlantic ocean (Scotese, 2001; Stampfli and Borel, 2002). Palaeomagnetic measures have led to the Pangaea B hypothesis, Gondwana landmass being in an about 3000 km more eastward position with respect to Laurasia (Irving, 1977). As a contribution to solve that problem, Muttoni et al. (1996, 2003) proposed an evolution from an Early Permian Pangaea B to a Late Permian Pangaea A. From the geodynamic point of view, a large westward displacement of Gondwana could be explained by the dextral strike-slip regime during the Late Palaeozoic (Arthaud and Matte, 1975, 1977; Shelley and Bossiere, 2002). As an illustration for France, this large-scale dextral shearing brought together, from the one hand the Ligerian (French Massif Central) and Aquitaine terranes and, from the other hand the Armorican (Brittany) terrane (Stampfli et al., 2002). The dextral strike-slip is indicated by arrows in Figure 5. During post-Early Permian to Triassic this movement is more difficult to advocate. In the Variscan belt of Western Europe, for example, the dominant strikeslip regime along west-east faults is mainly sinistral and the strike-slip is probably slower than during the previous period. This movement appears later, during the Triassic, in the Russian platform (Ruban and Yoshioka, 2005). However, the problem of relating the movement along the Palaeotethyan major shear zone (active margin) and the deformations along the other shear zones has already been addressed (Lawver et al., 2002). It remains difficult to consider a 3000 km-displacement during the Late Carboniferous-Permian? having no other field marker than palaeomagnetism.
First studies in the 1970's have quoted resemblance between the Variscan and the Himalayan belts, particularly concerning the type of thrusting (Mattauer and Etchecopar, 1977). Whereas early stages of an orogen's exhumation history are generally obscured in the belt itself by later tectonics and erosion, late events are theoretically simpler to illustrate. In that way, the comparison between the geometry of the Variscan belt of Western Europe and the Himalayas (Burg, 1983) or the Basin and Range Province (Malavieille, 1993) has been envisaged. Thus, some similarities between the pattern of strike-slip faults and thrusts in the Ibero-Armorican and West-Himalayan virgations have been emphasised (Matte, 1986). Some attempts have been made to compare the orographic set ting of the Tibet Plateau and the French Massif Central (Becq-Giraudon and Van den Driessche, 1994). It seems interesting to extent the comparison between the orogenies using the location of the playas, actually observed for the current ones, simply suggested by the geological records for the Permian ones.
At the current Earth surface, it exists a more or less continuous belt line from the Atlantic ocean to the Far East (Fig. 6). Around the Mediterranean sea, the Alps, Apennin, Dinarides, Hellenides, Taurides and Pontides are linked to the Tethyan Cenozoic tectonics. To the East, the major event is the continent-continent collision between India, one part of the former Gondwana, and the south-eastern margin of Eurasia. This collision is in progress since about 55 My and produced the major current orogen, the Himalayas. Nevertheless, other belts have been laterally produced by the collision, for example the Hindu Kush and Pamir. One particular aspect of the India-Eurasia collision is the presence of a large plateau, the so-called Tibet Plateau, the mean elevation of which is about 4500 m. The Tibet Plateau suffered a polyphased evolution. It is bordered on its north-western edge by a large sinistral strike-slip fault, the Altyn Tagh fault, which is still very active (Fig. 7B).
'Tectonic escape', 'extrusion tectonics' or 'lateral extrusion' have been proposed for the last tectonic developments either in Tibet (Tapponnier et al., 1986) or in the Alps (Ratschbacher et al., 1991). The identification of such a tectonics in the Variscan belt is still debated and represents a challenge for a better understanding of the orogen. Nevertheless, escape tectonics has been proposed by Vauchez et al. (1987) to explain the dextral strike-slip in the southeastern Appalachian and the sinistral strikeslip in the western Senegal-Mauritania (Mauritanides) provinces. In the European Variscan belt (Fig. 7A) some major faults could be related to escape tectonics such as the Bray Fault, the Cevennes Fault, a number of faults in southern Iberia, etc. The role of the Tornquist Suture, possibly reactivated during the Late Palaeozoic movements, is not clear. In Figure 7A, dextral late strike-slip movements are clearly put into light by the displacement of the Armorica terrane bordered to the north by the Avalonia terrane and, to the south, by the Galicia-South Brittany suture.
Currently, typical playas could be observed in the Qinhai Province of western China between the Kuku Nor (Lake Kuku) and the northern border of the Altyn Tagh sinistral strike-slip fault. These correspond to the Qaidam Pendi (Fig. 4B) with other occurrences in the Taklamakan (Fig. 7B). This latter is China's largest and driest desert. In Qaidam Pendi and Taklamakan as well, basins lack drainage and salt has accumulated over large areas. The Qaidam basin has been undergoing continuous shortening since the beginning of the Cenozoic and show good synchroneity with uplifting history of the Qinhai-Tibet Plateau (Wenchen et al, 2001). It has a rhombic shape, largely due to the strike-slip tectonics, and an area of about 120 000 [km.sup.2] with a mean elevation of 3000 to 3500 m a.s.l. It suffered a relatively weaker Cenozoic deformation than that of the deformed surrounding area in the northeastern edge of the Qinhai-Tibet Plateau (Zhou et al., 2006). Due to their setting, Taklamakan and Qaidam Pendi are cut off from the effects of the Asian monsoon. In such areas, playas rich in evaporites are common. In addition, between the Qaidam Pendi and the Kunlun piedmont, a complex system of playas, endorheic basins, and braided rivers surprisingly recalls what should have occurred during the erosion of the Variscan belt associated to coarse sediments such as sandstones and conglomerates (Fig 4C).
[FIGURE 6 OMITTED]
[FIGURE 7 OMITTED]
Playas are relatively rare at the current Earth surface. They are concentrated in isolated areas where arid conditions prevail, principally in Qinhai-Tibet, Central Asia, the Middle East and northern Africa (Fig. 6). From the tectonic point of view, it is necessary to take into account the bolson, which is a better marker than the playa itself. The bolson delineates large and elongated zones of aggradation such as the current Qaidam Pendi. Such areas could be linked with escape tectonics. Moreover, evaporites could characterise the central part of the morphological system, the so-called sabkha, but they are not necessarily present in the current systems and preserved in the old ones. Such morphologies were developed in the Valley and Ridge Province of the Appalachians and in the Ouachitas as well. Due to the Alpine deformation, the view is not so clear in the Asian segments of the Variscan orogeny where evaporites are common.
The current dispersion of the landmass results in a great number of local climatic barriers and, therefore, to different playa types: elevated in the Andes, close to the sea -- and possibly below the sea level such as in Algeria - in the Zone of Chotts, linked with endorheic basin in Lake Eyre, etc. Playas from the US Southwest and those from China are closely linked to present-day belts. They are probably closer analogues to the Permian playas than others.
In southern stable Europe (Fig. 7A), i.e. southern France, the Provence, Lodeve, Saint-Affrique, Rodez and Brive Permian basins contain the most developed playas with a special emphasis on the Lodeve basin. All these basins are separated from the Variscan Front by the Massif Central. It is interesting to note that in the current Tibet Plateau the younger unit, Plio-Quaternary in age, the so-called Qaidam Pendi rich in playa environments, is in the same structural position with respect to the Main Central Thrust of the Himalayas (note that the vergence of the Variscan and Himalayan main thrusting is opposite). There is a centrifugal zonation of the Tibetan units lasted since about 55 My (Fig. 7B). This time period could more or less represent the latest stages of the orogeny, i.e. Late Carboniferous-Early Permian for the Variscan one. For the Tibetan Plateau this sketch is complicated by large-scale strike-slip faults and the link with other further tectonic features (Baikal rift, Altai, etc.). Moreover, the Tibet plateau is still uplifting, whereas the Variscan orogen's uplift probably stopped during the Late Carboniferous. Therefore, the situation during the Late Variscan time with the amalgamation of all the landmasses into the Pangaea was clearly different. Nevertheless, it is possible to suggest that the basins of southern France were parts of an isolated area forming a structural unit at the southwestern edge of the Massif Central and bordered by large-scale strike-slip faults. The largest Permian playa system, the Southern Permian Basin, was in a quite different tectonic setting characterized by thermal subsidence.
A question arises: was the Late Variscan belt more or less continuous? The large Appalachian-Variscan-Uralian-Mongolian belt comprised some dependencies: Ouachitas, Mauritanides, Moroccan Meseta, Scythian belt, Altaids (Fig. 5). The entire belt was comparable to the present 'Alpine' belt starting from the north African Atlas, and joining the Alps, Dinarides, Taurides, Causasus, Penjab, Himalayas, etc. (Fig. 6). Clearly, these are the results of diachronous and different types of collision: continent/ continent (Himalayas), progressive shortening collapse of narrow oceans (Alps, Dinarides), etc. Between the different segments, it exists large corridors of lowlands or sea. The timing of each orogeny could be very variable and short as recently illustrated by Dewey (2006), particularly if arc/continent collisions are concerned -- this is probably the case for the Scythian belt and also for the Permian far eastern orogenies affecting the southeastern margin of Eurasia and exotic blocks (Tarim, North China, etc.).
The study of the Permian and Triassic times, particularly the tectonic setting of a number of intramountainous basins, indicates a transition from plate tectonics to continental tectonics (Molnar, 1988). There are only rare occurrences of Permian oceanic deposits such as in Oman Mountains. Therefore, the palinspastic reconstructions should be elaborated only with isolated pieces. Some of the pieces of this gigantic jigsaw considerably derived, such as the Cache Creek terrane of the Canadian Cordillera recently interpreted as accreted seamounts that originated close to the eastern Tethys ocean (Johnston and Borel, 2007). The major problem is to consider the transition from the crustal thickening as a syn-collisional effect, and the gravitary collapse clearly post-collision and possibly related to basin and range extensional structures. It should be noticed that the valleys and ridges of the Appalachians present some affinities with the basin and range structures.
The problem of gravitationary collapse has been discussed for the Tibet Plateau and the Variscan orogeny as well (Becq-Giraudon and Van den Driessche, 1994). But as already mentioned, the European Variscides are probably formed as early as the Late Carboniferous and are not representative of the entire Late Palaeozoic belt, the maximum development of which is situated in the late Early Permian and, most probably, in the Guadalupian (Khain and Seslavinsky, 2002).
The Late Carboniferous and earliest Permian is represented by worldwide coal basins -- even at high latitudes. Progressively, arid conditions appeared and dominated in the Middle Permian (Guadalupian), with a large development of playas even close to the equator. From a palaeoenvironmental viewpoint, during the Late Permian (Lopingian) and the Early Triassic as well the most important feature is a major carbon lack, with no more reefs in the ocean and no more coal deposits in the continental basins. The entire planet Earth has been dramatically altered: atmospheric composition, general water circulation, chemistry of the oceans, etc. This is mainly due to the geodynamic setting, the existence of the large Appalachian-Variscan-Uralian-Mongolian belt modifying a lot of parameters. Low [sup.87]Sr/[sup.86]Sr values observed until the PTBI illustrate the fact that erosion is a continuing phenomenon during the entire Permian and the Triassic as well. Moreover, the widening of closed drainage areas on land reduced the transportation of organic and mineral nutrients to seas. A dramatic negative excursion of the rate in 834S during the Late Permian could be related to the extent of evaporites, particularly in the Southern Permian Basin. This resulted in a great climate change and finally by the major biological crisis of the Phanerozoic, which is not necessary concentrated at the PTBI boundary but begins a few My before.
The understanding of the evaporites and, more generally, of the Permian and Triassic playa environments with respect to the geodynamic evolution would require a better knowledge of the palaeogeography from the one hand, and of the geometry of the orogens, particularly their elevation, from the other hand.
Received: 27/02/07/Accepted: 20/03/07
The author thanks Dr Georges Gand (Dijon, France) for the organization of the Symposium on the Permian and Triassic playas held in Montpellier and his initiative for publishing the papers in the Journal of Iberian Geology. He is also grateful to the two reviewers, Prof. Giuseppe Cassinis (Pavia, Italy) and Prof. Jorg W. Schneider (Freiberg, Germany) for their constructive comments.
Anderson R.Y., Dean, W.E. (1995): Filling the Delaware Basin: Hydrologic and climatic controls on the Upper Permian Castile Formation varved evaporite. In: P. A. Scholle, T. M. Peryt, D. S. Ulmer-Scholle (eds.), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 61-78.
Arche, A., Lopez-Gomez, J. (2005): Sudden changes in fluvial style across the Permian-Triassic boundary in the eastern Iberian Ranges, Spain: Analysis of possible causes. Palaeogeography, Palaeoclimatology, Palaeoecology, 229:104-126.
Arthaud, F., Matte, P. (1975): Les decrochements tardi-hercyniens du Sud-Ouest de l'Europe. Geometrie et essai de reconstitution des conditions de la deformation. Tectonophysics, 25:139-171.
Arthaud, F., Matte, P. (1977): Late Paleozoic strike-slip faulting in southern Europe and northern Africa: Result of a right-lateral shear zone between the Appalachians and the Urals. Geological Society of America Bulletin, 88:1305-1320.
Bailey, R.J. (2001): Sequence stratigraphy and orbital forcing in Permian (Rotliegend) desert deposits: a discussion. Journal of the geological Society, 158:785-791.
Barde, J.P., Gralla, P., Harwijanto, J., Marsky, J. (2002): Exploration at the eastern edge of the Precaspian basin: Impact of data integration on Upper Permian and Triassic prospectivity. AAPG Bulletin, 86: 399-415.
Bates, R.L. and Jackson, J.A. (1987): Glossary of Geology. American Geological Institute, 3rd edit., 788 pp.
Baud, A. (2005): Geochemical changes at the Permian-Triassic transition in Southern Alps and adjacent area: a review. Annali dell'Universita degli Studi di Ferrara, volume speciale, 5-11.
Beauchamp, B. (1995): Permian history of Arctic North America. In: P.A. Scholle, T.M. Peryt, D.S. Ulmer-Scholle (eds.), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 3-22.
Becq-Giraudon, J.F., Van den Driessche, J. (1994): Depots periglaciaires dans le Stephano-Autunien du Massif Central: temoin de l'effondrement gravitaire d'un haut plateau hercynien. Comptes Rendus de l'Academie des Sciences, Paris, 318: 675-682.
Beerling, D.J. (2002): Low atmospheric C[O.sub.2] levels during the Permo-Carboniferous glaciation inferred from fossil lycopsids. Proceedings of the National Academy of Sciences of the United States of America (PNAS), 99: 12567-12571.
Beerling, D.J., Berner, R.A. (2000): Impact of a Permo-Carboniferous high [O.sub.2] event on the terrestrial carbon cycle. Proceedings of the National Academy of Sciences of the United States of America (PNAS), 97: 12428-12432.
Benison, K.C. (2006): A Martian analog in Kansas: Comparing Martian strata with Permian acid saline lake deposits. Geology, 34: 385-388.
Benison, K.C., Goldstein, R.H. (2000): Sedimentology of ancient saline pans: an example from the Permian Opeche Shale Williston Basin, North Dakota, U.S.A.. Journal of Sedimentary Research, 70: 159-169.
Berner, R.A. (2006a): GEOCARBSULF: A combined model for Phanerozoic atmospheric [O.sub.2] and C[O.sub.2]. Geochimica et Cosmochimica Acta, 70: 5653-5664.
Berner, R.A. (2006b): Carbon, sulfur and [O.sub.2] across the Permian-Triassic boundary. Journal of Geochemical Exploration, 88:416-418.
Bin He, Yi-Gang Xu, Xiao-Long Huang, Zhen-Yu Luo, Yu-Ruo Shi, Qi-Jun Yang, Song-Yue Yu (2007): Age and duration of the Emeishan flood volcanism, SW China: Geochemistry and SHRIMP zircon U-Pb dating of silicic ignimbrites, postvolcanic Xuanwei Formation and clay tuff at the Chaotian section. Earth Planetary Science Letters, 255: 306-323.
Bonin B. (1998): Orogenic to non-orogenic magmatic events: overview of the Late Variscan magmatic evolution of the Alpine Belt. Turkish Journal of Earth Sciences, 7: 133-143.
Briden, J.C., Irving, E. (1964): Paleolatitude spectra of sedimentary paleoclimatic indicators. In: Nairn, A.E.M. (ed.) Problems in Paleoclimatology, London, Wiley Ed., 199-224.
Briere, P.R. (2000): Playa, playa lake, sabkha: proposed definitions for old terms. Journal of Arid Environments, 45: 1-7.
Bryant, R.G., Sellwood, B., Millington, A.C., Drake, N.A. (1994): Marine-like potash evaporite formation on a continental playa: case study from Chott el Djerid, southern Tunisia. Sedimentary Geology, 90: 269-291.
Burg, J.P. (1983): Tectogenese comparee de deux segments de chaine de collision: le sud du Tibet (suture du Tsangpo) et la chaine hercynienne en Europe (sutures du Massif Central). These Doctorat d'Etat, Univ. Montpellier, 368 pp.
Burgoyne, P.M., van Wyk, A.E., Anderson, J.M., Schrire, B.D. (2005): Phanerozoic evolution of plants on the African plate. Journal of African Earth Sciences, 43: 13-52.
Burkhard, M., Caritg, S., Helg, U., Robert-Charrue, C., Soulaimani, A. (2006): Tectonics of the Anti-Atlas of Morocco. Comptes Rendus Geoscience, 338: 11-24.
Burollet, P.F. (1991): Structures and tectonics of Tunisia. Tectonophysics, 195: 359-369.
Cadel, G., Cosi, M., Pennacchioni, G., Spalla, M.I. (1996): A new map of the Permo-Carboniferous cover and Variscan metamorphic basement in the central Orobic Alps -- Italy: structural and stratigraphical data. Memorie di Scienze Geologiche, Padova, 48: 1-53.
Cassinis, G., Dal Piaz, G.V., Eusebio, A., Gosso, G., Martinotti, G., Massari, F., Milano, P.F., Pennacchioni, G., Perello, M., Pessina, C.M., Roman, E., Spalla, M.I., Tosetto, S., Zerbato, M. (1986): Report on a structural and a sedimentological analysis in the Uranium province of the Orobic Alps, Italy. Uranium, Amsterdam, 2: 241-260.
Cassinis, G. (editor) (2001): Permian continental deposits of Europe and other areas. Regional reports and correlations. Monografie di << Natura Bresciana >>, Ann. Museo Civico di Scienze naturali di Brescia, 25, 375 pp.
Cassinis, G., Toutin-Morin, N., Virgili, C. (1995): A General Outline of the Permian Continental Basins in Southwestern Europe. In: The Permian of Northern Pangea, 2, Sedimentary Basins and Economic Resources, P.A. Scholle, T.M. Peryt and D.S. Ulmer-Scholle (eds), Springer-Verlag, 137-157.
Chateauneuf, J.J., Farjanel, G. (1989): Synthese geologique des bassins permiens francais. Memoire du Bureau de recherches geologiques et minieres, 128, 288 pp.
Chumakov, N.M., Zharkov, M.A. (2003): Climate during the Permian-Triassic biosphere reorganization. Article 2. Climate of the Late Permian and Early Triassic: General inferences. Stratigraphical and Geological Correlation, 11: 361-375.
Chuvashov, B.I. (1995): Permian deposits of the Urals and Preduralye. In: P. A. Scholle, T. M. Peryt, D. S. Ulmer-Scholle (eds), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 158-183.
Clarke, P., Parnell, J. (1999): Facies analysis of a back-tilted lacustrine basin in a strike-slip zone, Lower Devonian, Scotland. Palaeogeography, Palaeoclimatology, Palaeoecology, 151: 167-190.
Coque, R. (1962): La Tunisie presaharienne. Armand Colin, Edit., Paris.
Demangeot, J., Besnus, E. (2001): Les milieux desertiques. Armand Colin/HER Edit., Paris, 295 pp.
Deroin, J.P., Bonin, B. (2003): Late Variscan tectonomagmatic activity in Europe and surrounding areas: the Mid-Permian Episode. Bollettino della Societa Geologica Italiana, volume speciale, 2: 169-184.
Deroin, J.-P., Bonin, B., Broutin, J., Cabanis, B., Chateauneuf, J.J., Damotte, R., Durand, M., Gand, G. (2001): The Permian of Southern France: an overview. In: G. Cassinis (ed.), Permian continental deposits of Europe and other areas. Regional reports and correlations. Monografie di <<Natura Bresciana>>, Ann. Museo Civico di Scienze naturali di Brescia, 25: 189-202.
Dewey, J.F. (2006): Orogeny can be very short. Proceedings of the Academy of Sciences of the United States of America (PNAS), 102: 15286-15293.
Dickson, J.A.D., Montanez, I.P., Saller, A.H. (2001): Hypersaline burial diagenesis delineated by component isotopic analysis, late Paleozoic limestones, West Texas. Journal of Sedimentary Research, 71: 372-379.
DiMichele, W., Pfefferkorn, H.W., Gastaldo, R.A. (2001): Response of Late Carboniferous and Early Permian plant communities to climate change. Annu. Rev. Earth Planet. Sci., 29: 461-487.
Fairchild, I.J., Hambrey, M.J. (1995): Vendian basin evolution in East Greenland and NE Svalbard. Precambrian Research, 73: 217-233.
Flint, S. (1985): Alluvial fan and playa sedimentation in an Andean arid closed basin: the Pacencia Group, Antofagasta Province, Chile. Journal of the Geological Society, London, 142: 533-546.
Fluteau, F. (2003): Earth dynamics and climate changes. ComptesRendus Geoscience, 335:157-174.
Fluteau, F., Besse, J., Broutin, J., Ramstein, G. (2001): The Late Permian climate. What can be inferred from climate modelling concerning Pangea scenarios and Hercynian range altitude? Palaeogeography, Palaeoclimatology, Palaeoecology, 167: 39-71.
Freytet, P., Toutin-Morin, N., Broutin, J., Debriette, P., Durand, M., El Wartiti, M., Gand, G., Kerp, H., Orszag, F., Paquette, Y., Ronchi, A., Sarfati, J. (1999): Palaeoecology of non marine algae and stromatolites: Permian of France and adjacent countries. Annales de Paleontologie, 85: 99-153.
Gand, G., Garric, J., Lapeyrie, J. (1997): Biocenoses a triopsides (Crustacea, Branchiopoda) du Permien du Bassin de Lodeve (France). Geobios, 30: 673-700.
Gast, R. (1991): The perennial Rotliegend saline lake in NW Germany. Geologisches Jahrbuch, A 119: 117-139.
Glover, B.W., Powell, J.H. (1996): Interaction of climate and tectonics upon alluvial architecture: Late Carboniferous-Early Permian sequences at the southern margin of the Pennine Basin, UK. Palaeogeography, Palaeoclimatology, Palaeoecology, 121: 13-34.
Hamilton, W.H. (1951): Playa sediments of Rosamond Dry lake, California. Journal of Sedimentary Petrology, 21: 147-150.
Handford, C.R. (1981): Coastal sabkha and salt pan deposition of the Lower Clear Fork Formation (Permian), Texas. Journal of Sedimentary Petrology, 51: 761-778.
Hartley, A.J. (2003): Andean uplift and climate change. Journal of the Geological Society, London, 160: 7-10.
Hartley, A.J., Chong, G. (2002): Late Pliocene age for the Atacama Desert: Implications for the deserticfication of western South America. Geology, 30: 43-46.
Hatcher, R.D. (2002): Alleghanian (Appalachian) orogeny, a product of zipper tectonics: Rotational transpressive continent-continent collision and closing of ancient oceans along irregular margins. Geological Society of America, Special Paper, 364: 199-208.
Hofman, A., Tourani, A., Gaupp, R. (2000): Cyclicity of Triassic to Lower Jurassic continental red beds of the Argana Valley, Morocco: implications for palaeoclimate and basin evolution. Palaeogeography, Palaeoclimatology, Palaeoecology, 161: 229-266.
Hryniv, S.P., Peryt, T.M. (2003): Sulfate cavity filling in the Lower Werra Anhydrite (Zechstein, Permian), Zdrada area, Northern Poland: Evidence for early diagenetic evaporite paleokarst formed under sedimentary cover. Journal of Sedimentary Research, 73: 451-461.
Irving, E. (1977): Drift of the major continental block since the Devonian. Nature, 270: 304-309.
Johnston, S.T., Borel, G.D. (2007): The odyssey of the Cache Creek terrane, Canadian Cordillera: Implications for accretionary orogens, tectonic setting of Panthalassa, the Pacific superwell, and break-up of Pangea. Earth and Planetary Science Letters, 253: 415-428.
Kessler, J.L.P., Soreghan, G.N., Wacker, H.J. (2001): Equatorial aridity in Western Pangea: Lower Permian loessite and dolomitic paleosols in Northeastern New Mexico, U.S.A. Journal of Sedimentary Research, 71: 817-832.
Khain, V.E., Seslavinsky, K.B. (1992): Global rhythms in the Phanerozoic endogenic activity of the Earth. 29th International Geological Congress, Kyoto, Japan, abstract volumes.
Kiehl, J.T., Shields, C.A. (2005): Climate simulation of the latest Permian: Implication for mass extinction. Geology, 33: 757-760.
Kiersnowski, H., Paul, J., Peryt, T.M., Smith, D.B. (1995): Facies, paleogeography, and sedimentary history of the Southern Permian basin in Europe. In: P. A. Scholle, T. M. Peryt, D. S. Ulmer-Scholle (eds), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 119-136.
Kirkland, D.W., Denison, R.E., Dean, W.E. (2000). Parent brine of the Castile Evaporites (Upper Permian), Texas and New Mexico. Journal of Sedimentary Research, 70: 749-761.
Krull, E.S., Lehrmann, D.J., Druke, D., Kessel, B., Yu, Y., Li R. (2004): Stable carbon isotope stratigraphy across the Permian-Triassic boundary in shallow marine carbonate platforms, Nanpanjiang Basin, south China. Palaeogeography, Palaeoclimatology, Palaeoecology, 204: 297-315.
Langbein, R. (1987): The Zechstein sulphates: the state of the art. In: Tadeusz M. Peryt (ed), The Zechstein Facies in Europe, Lecture Notes in Earth Sciences, Volume 10, Springer-Verlag, Berlin and Heidelberg, 143-188.
Lawver, L.A., Grantz, A., Gahagan, L.M. (2002): Plate kinematic evolution of the present Arctic region since the Ordovician. In: Miller E.L., Grantz A. and Klemperer S.L. (eds.), Tectonic evolution of the Bering Shelf-Chukchi sea-Arctic margin and adjacent landmasses, Geological Society of America Special Papers, 360: 333-358.
Legler, B., Gebhardt, U., Schneider, J. (2005): Late Permian non-marine-marine transitional profiles in the central Southern Permian Basin, northern Germany. International Journal of Earth Sciences, 94: 851-862.
Limarino, C., Tripaldi, A., Marenssi, S., Fauque, L. (2006): Tectonic, sea-level, and climatic controls on Late Paleozoic sedimentation in the western basins of Argentina. Journal of South American Earth Sciences, 22: 205-226.
Lorenz, V., Nicholls, I.A. (1984): Plate and intraplate processes of Hercynian Europe during the Late Paleozoic. Tectonophysics, 107: 25-56.
Ludwig, A.O. (1988): Climate, tectonics, sedimentation during the transitional period from the Early to the Late Permian. Zeitschriftfur Geologische Wissenschaften, 16: 1073-1080.
Magee, J.W., Gifford, H.M., Spooner, N.A., Questiaux, D. (2004): Continuous 150 k.y. monsoon record from lake Eyre Australia: Insolation-forcing implications and unexpected Holocene failure. Geology, 32: 885-888.
Malavieille, J. (1993): Late orogenic extension in mountain belts: insights from the Basin and Range and the late Paleozoic Variscan belt. Tectonics, 12: 1115-1130.
Martin, C.A.L., Stewart, S.A., Doubleday, P.A. (2002): Upper Carboniferous and Lower Permian tectonostratigraphy on the southern margin of the Central North Sea. Journal of the Geological Society, London, 159: 731-749.
Mattauer, M., Etchecopar, A. (1977): Argument en faveur de chevauchements de type himalayen dans la chaine hercynienne du Massif Central francais. Colloque Int. CNRS, 268, Ecologie et Geologie de l'Himalaya, 261-267.
Matte, P. (1986): Tectonics and plate tectonics model for the Variscan belt of Europe. Tectonophysics, 126: 329-374.
Matte, P. (2002): Variscides between the Appalachians and the Urals: Similarities and differences between Paleozoic subduction and collision belts. Geological Society of America, Special Paper, 364:239-251.
Mazzullo, S.J. (1995): Permian stratigraphy and facies, Permian basin (Texas-New Mexico) and adjoining areas in the Midcontinent United States. In: P. A. Scholle, T.M. Peryt, D.S. Ulmer-Scholle (eds), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 41-60.
McAllister Rees, P. (2002): Land-plant diversity and the end-Permian mass extinction. Geology, 30: 827:830.
McAllister Rees, P., Ziegler, A.M., Gibbs, M.T., Kutzbach, J.E., Behling, P.J., Rowley, D.B. (2002): Permian phytogeographic patterns and climate. Data/model comparisons. The Journal of Geology, Chicago, 110: 1-31.
Medina, F. (ed.) (1996): Le Permien et le Trias du Maroc: etat des connaissances. PUMAG (edit.), Marrakech, 305 pp.
Molnar, P. (1988): Continental tectonics in the aftermath of plate tectonics. Nature, 335: 131-137.
Muttoni, G., Kent, D.V., Channel, J.E.T. (1996): The evolution of Pangaea: paleomagnetic constraints from the Southern Alps, Italy. Earth and Planetary Science Letters, 140: 97-112.
Muttoni, G., Kent, D.V., Garzanti, E., Bnrack, P., Abrahamsen, N., Gaetani, M. (2003): Early Permian Pangaea 'B' to late Permian Pangaea 'A'. Earth and Planetary Science Letters, 215: 379-394.
Natal'in, B.A., s.engor, A.M.C. (2005): Late Palaeozoic to Triassic evolution of the Turan and Scythian platforms: The prehistory of the Palaeo-Tethyan closure. Tectonophysics, 404: 175-202.
Nikishin, A.M., Ziegler, P.A., Abbott, D., Brunet, M.F., Cloethingh, S. (2002): Permo-Triassic intraplate magmatism and rifting in Eurasia: implications for mantle plumes and mantle dynamics. Tectonophysics, 351: 3-39.
Oyarzun, R., Doblas, M., Lopez-Ruiz, J., Cebria, J.M., Youbi, N. (1999): Tectonically-induced icehouse-greenhouse climate oscillations during the transition from the Variscan to the Alpine cycle (Carboniferous to Triassic). Bulletin de la Societe Geologique de France, 170: 3-11.
Paul, J., Peryt, T.M. (2000): Kalkowsky's stromatolites revisited (Lower Triassic Buntsandstein, Harz Mountains, Germany). Palaeogeography, Palaeoclimatology, Palaeoecology, 161: 435-458.
Pittau, P., Del Rio, M. (2004): Upper Carboniferous to Triassic terrestrial palynofloras of Sardinia; biostratigraphic, paleoclimatologic and paleophytogeographic implications. Abstracts with Programs -- Geological Society of America, 36:83.
Ratschbacher, L., Frisch, W., Linzer, H.G., Merle, O. (1991): Lateral extrusion in the Eastern Alps. Tectonics, 10:257-271.
Roscher, M., Schneider, J.W. (2006): Permo-Carboniferous climate: early Pennsylvanian to Late Permian climate development of central Europe in a regional and global context. In: Non-marine Permian biostratigraphy and biochronology, S.G. Lucas, G. Cassinis and J.W. Schneider (eds.), Geological Society, London, Special Publications, 265: 95-136.
Rouchy, J.M., Caruso, A. (2006): The Messinian salinity crisis in the mediterranean basin: A reassessment of the data and an integrated scenario. Sedimentary Geology, 188-189: 35-67.
Rouchy, J.M., Orszag-Sperber, F., Pierre, C., Guilhaumou, N., Lagny, P. (2001): Les evaporites. Geochronique, Societe Geologique de France, Paris, BRGM, Orleans, 80: 10-36.
Ruban, D.A., Yoshioka, S. (2005): Late Paleozoic -- Early Mesozoic tectonic activity within the Donbass (Russian Platform). Trabajos de Geologia, Oviedo, 25: 101-104.
Satterfield, C.L., Lowenstein, T.K., Vreeland, R.H., Rosenzweig, W.D., Powers, D.W. (2005): New evidence for 250 Ma age of halotolerant bacterium from a Permian salt crystal. Geology, 33: 265-268.
Scheffler, K., Hoernes, S., Schwark, L. (2003): Global changes during Carboniferous-Permian glaciation of Gondwana: Linking polar and equatorial climate evolution by geochemical proxies. Geology, 31: 605-608.
Schneider, J., Gebhardt, U. (1993): Litho- und Biofaziesmuster in intra- und extramontanen Senken des Rotliegend (Perm, Nord- und Ostdeutschland). Geol. Jb, A 131:57-98.
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.
Scotese, C.R. (2001): Atlas of Earth history PALEOMAP Project. Arlington, Texas, 52 pp.
Shelley, D., Bossiere, G. (2002): Megadisplacements and the Hercynian orogen of Gondwanan France and Iberia. Geological Society of America, Special Paper, 364: 209-222.
Sidor, C.A., O'Keefe, F.R., Damiani, R., Steyer, J.S., Smith, R.M.H., Larsson, H.C.E., Sereno, P.C., Ide, O., Maga, A. (2005): Permian tetrapods from the Sahara show climate-controlled endemism in Pangaea. Nature, 434: 886-889.
Simpson, E.L., Eriksson, K.A., Kuklis, C.A., Eriksson, P.G., Bumby, A.J., van Jaarsveld, C.F. (2004): Saline pan deposits from the ~ 1.8 Ga Makgabeng Formation, Waterberg Group, South Africa. Sedimentary Geology, 163: 279-292.
Smith, R.M.H. (1995): Changing fluvial environments across the Permian-Triassic boundary in the Karoo Basin, South Africa and possible causes of tetrapod extinctions. Palaeogeography, Palaeoclimatology, Palaeoecology, 117: 81-104.
Spalletti, L.A., Pinol, F.C. (2005): From alluvial fan to playa: An Upper Jurassic ephemeral fluvial system, Neuquen Basin, Argentina. Gondwana Research, 8: 363-383.
Stampfli, G.M., Borel, G.D. (2002): A plate tectonic model for the Paleozoic and Mesozoic constrained by dynamic plate boundaries and restored synthetic oceanic isochrons. Earth and Planetary Science Letters, 196: 17-33.
Stampfli, G.M., von Raumer, J.F., Borel, G.D. (2002): Paleozoic evolution of pre-Variscan terranes: From Gondwana to the Variscan collision. Geological Society of America, Special Paper, 364: 263-280.
Stemmerik, L. (1995): Permian history of the Norwegian-Greenland sea area. In: P. A. Scholle, T. M. Peryt, D. S. Ulmer-Scholle (eds.), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 98-118.
Stemmerik, L., Worsley, D. (1995): Permian history of the Barents shelf area. In: P. A. Scholle, T. M. Peryt, D. S. Ulmer Scholle (eds.), The Permian of Northern Pangea, 2, Sedimentary basins and economic resources, Springer-Verlag, Berlin-Heidelberg, 81-97.
Stollhofen, H., Stanistreet, I.G., Bangert, B., Grill, H. (2000): Tuffs, tectonism and glacially related sea-level changes, Carboniferous-Permian, Southern Namibia.- Palaeogeography, Palaeoclimatology, Palaeoecology, 161: 127-150.
Tabor, N.J., Montanez, I.P. (2002): Shifts in late Paleozoic atmospheric circulation over western equatorial Pangea: Insights from pedogenic mineral [delta][sup.18]O compositions. Geology, 30, 12: 1127-1130.
Tapponnier, P., Meyer, B., Roger, F. (2002): Le haut plateau tibetain: des ensembles de bassins prisonniers, une montee en trois temps. In: J. P. Avouac, P. De Wever (eds.), Himalaya-Tibet. Le choc des continents. CNRS Editions et Museum national d'Histoire naturelle, Paris, France: 106-111.
Tapponnier, P., Peltzer, G., Armijo, R. (1986): On the mechanics of the collision between India and Asia. In: Coward M.P. and Ries A.C. (eds), Collision Tectonics, Geological Society Special Publication, 19: 115-157.
Torsvik, T.H., Cocks, R.M. (2004): Earth geography from 400 to 250 Ma: a palaeomagnetic, faunal and facies review. Journal of the Geological Society, London, 161: 555-572.
Turner, B.R., Smith, D.B. (1997): A playa deposit of pre-Yellow Sands age (upper Rotliegend/Weissliegend) in the Permian of northeast England. Sedimentary Geology, 114: 305-319.
Twitchett, R.J. (2006): The palaeoclimatology, palaeoecology and palaeoenvironmental analysis of mass extinction events. Palaeogeography, Palaeoclimatology, Palaeoecology, 232: 190-213.
Van der Voo, R., Levashova, N.M., Skrinnik, L.I., Kara, T.V., Bazhekov, M.L. (2006): Late orogenic large-scale rotations in the Tien Shan and adjacent mobile belts in Kyrgyzstan and Kazakhstan. Tectonophysics, 426: 335-360.
Vauchez, A., Kessler, S.F., Lecorche, J.P., Villeneuve, M. (1987): Southward extrusion tectonics during the Carboniferous Africa-North America collision. Tectonophysics, 142: 317-322.
Virgili, C., Cassinis, G., Broutin, J. (2006): Permian to Triassic sequences from selected continental areas of southwestern Europe. In: Lucas, S.G., Cassinis, G., Schneider, JW. (eds), Non-Marine Permian biostratigraphy and biochronology. Geological Society, London, Special Publications, 265: 231-259.
Visser, J.N.J. (1993). A reconstruction of the late Palaeozoic ice sheet on southwestern Gondwana. In: Veevers (eds.), International Gondwana Symposium, Findlay, Unrug, Banks, 8: 449-458.
Warren, J. (1999): Evaporites. Their evolution and economics. Blackwell Science, 438 p.
Wenchen, X., Ning, Z., Xiaoping, Y., Lianshun, F. (2001): Cenozoic Qaidam basin, China: A stronger tectonic inversed, extensional rifted basin. AAPG Bulletin, 85, 4: 715-736.
Winguth, A.M.E., Maier-Reimer, E. (2005): Causes of the marine productivity and oxygen changes associated with the Permian-Triassic boundary: A reevaluation with ocean general circulation models. Marine Geology, 217:283-304.
Woods, A.D. (2005): Paleoceanographic and paleoclimatic context of Early Triassic time. Comptes Rendus Palevol, 4: 463-472.
Yanev, S. (2000): Palaeozoic terranes of the Balkan Peninsula in the framework of Pangea assembly. Palaeogeography; Palaeoclimatology, Palaeoecology, 161: 151-177.
Zerfass, H., Chemale Jr, F., Leandro Schultz, C., Lavina, E. (2004): Tectonics and sedimentation in Southern South America during Triassic. Sedimentary Geology, 166: 265-292.
Zhang, G., Buatois, L.A., Mangano, M.G., Acenolaza, F.G. (1998): Sedimentary facies and environmental ichnology of a ?Permian playa-lake complex in western Argentina. Palaeogeography, Palaeoclimatology, Palaeoecology, 138: 221-243.
Zhou, J., Xu, F., Wang, T., Cao, A., Yin, C. (2006): Cenozoic deformation history of the Qaidam Basin, NW China: Results from cross-section restoration and implications for Qinghai-Tibet Plateau tectonics. Earth and Planetary Science Letters, 243: 195-210.
Ziegler, P.A., Stampfli, G.M. (2001): Late Palaeozoic-Early Mesozoic plate boundary reorganization: collapse of the Variscan orogen and opening of Neotethys. In: Cassinis, G. (ed.), Permian continental deposits of Europe and other areas. Regional reports and correlations. Monografie di "Natura Bresciana", Ann. Museo Civico di Scienze Naturali di Brescia, 25: 17-34.
Universite Paris-Est-Marne-la-Vallee, EA 4119, IFSA (Institut Francilien des Sciences Appliquees), 5 boulevard Descartes, Cite Descartes, Champs sur Marne, 77454 Marne-la-Vallee cedex 2, France. firstname.lastname@example.org
|Printer friendly Cite/link Email Feedback|
|Publication:||Journal of Iberian Geology|
|Date:||Jan 1, 2008|
|Previous Article:||Algunas precisiones sobre el uso del termino playa en la bibliografia geologica.|
|Next Article:||Los ambientes de playa de la Cuenca de Lodeve (Languedoc-Francia).|