An Annotated Correlation Chart for Continental Late Pennsylvanian and Permian Basins and the Marine Scale

Home , Atrasado Formation, Diplocaulus, Gehren, Gray Mesa Formation, Kupferschiefer, Luisenthal

Lucas, S.G. and Zeigler, K.E., eds., 2005, The Nonmarine Permian, New Mexico Museum of Natural History and Science Bulletin No. 30. 282 AN ANNOTATED CORRELATION CHART FOR CONTINENTAL LATE PENNSYLVANIAN AND PERMIAN BASINS AND THE MARINE SCALE

MARCO ROSCHER AND JÖRG W. SCHNEIDER

TU Bergakademie Freiberg, Cottastraße 2, D-09596 Freiberg, Germany; [email protected]

Abstract—Late Pennsylvanian and Permian continental deposits of 20 basins in a west-east traverse from North America via France, Germany, Czech Republic, Italy, Morocco and the Ukraina are correlated by a compilation of biostratigraphic data and isotopic ages. Included is the correlation to the Karoo Basin in southern Africa. The biostratigraphy is based mostly on insect and amphibian biozones, which give the most reliable data up to now. Additionally, information from macro- and microfloristic investigations have been used for some basins. Reliable biostratigraphic data, derived from bio(chrono)species, are well accessible in most of the basins, particularly in the Pennsylvanian and lower half of the Cisuralian. For this part a time resolution down to 0.5 Ma is obtained from morphogenetic lineages of blattid insects and evolutionary lineages of aquatic amphibians. Late Cisuralian, Guadalupian and Lopingian sediments are mostly discontinuously developed in the overwhelming number of basins. Terrestrially-adapted amphibians and reptiles became more important for this time span. Correlations to the global marine standard scale are based on isotopic ages from volcanites of the continental basins. But, they are not unambiguous, because tectonic reactivations in the European Variscides and multiple Mesozoic thermal events have upset the geochronologic systems. Only cross correlation in conjunction with biostratigraphic data enable the best fitting of isotopic ages for the time being. To overcome these problems, future investigations should focus on the Permian mixed marine/continental deposits of the North Ameri- can Midcontinent Basin and of the Volga-Kama region of Tatarstan in Eastern Europe.

INTRODUCTION river systems, whereas semi-aquatic amphibians could migrate between different drainage systems as “pond-hoppers.” Very wide rivers and The stratigraphic correlation of Late Pennsylvanian and Permian high mountain ranges could form barriers for terrestrially-adapted am- continental basins is confronted with a series of methodical problems phibians and reptiles. In contrast, actively flying insects and the minute (Schneider, 1998, 2001). The often limited extent of most basins, and eggs of conchostracans could be widely distributed by air currents, pro- the influence of tectonic and volcanic processes as well as climatic viding the base for inter-regional, high-resolution biostratigraphy. Tet- fluctuations results in irregular lithofacies patterns and prevented the rapod tracks are most common in red beds. Since tetrapod footprints deposition of regionally extensive key beds. Although lithostratigraphic reflect evolutionary changes in taxonomic levels above genera and fami- correlation of local sections provides a useful tool for intra-basinal cor- lies only, the time resolution of footprint associations is generally low relations, simple lithostratigraphic comparisons generally fail to corre- (Lucas, 1998; Voigt, 2005). late the sections between basins. To cope with these changing environ- The most intricate problems are correlations between pure con- ments, different biostratigraphic tools are used for diverse environments tinental profiles or basins with the marine standard scale (e.g., Schneider and different litho- and biofacies patterns as well. The classical macro- et al., 1995b). Up to now, such correlations are based nearly exclu- and microfloristic methods are basically ecostratigraphy, because the sively on isotopic ages (Schneider et al., 1995a; Menning 1995; Menning distribution of plants in space and time is primarily governed by cli- et al., 2000, 2003; Lützner et al., 2003). Attempts for direct nonma- mate and the resulting environments of different extent – interregional rine-marine biostratigraphic correlations have been made in the last to local. Plant biostratigraphy works well inside climatic belts or biomes several years (Schneider et al., 1991, 1995b), but real progress has that display large-scale, balanced biotopes. This is the case during the been at the horizon only recently, when nearshore marine profiles have late Palaeozoic Mississippian and partly the Pennsylvanian up to the delivered conodonts and insect remains together (Schneider et al., 2004). end of the Moscovian. From the Moscovian onward into the Permian, In the following, the actual state of the art for continental-continental interference between the vanishing late Palaeozoic glacial ages, the and continental-marine correlations will be demonstrated for the most decreasing marine transgressions, the general warming and possibly important and best investigated European basins in relation to two mixed the phases of enhanced volcanism (Schneider et al. 1995a, 2006, in marine/continental basins (Lucero Basin, New Mexico; Donetsk Ba- press) generate strong differentiation of the vegetation on regional to sin, Ukraine) and to the Karoo Basin in southern Africa. local scales, which restrict the application of plant biostratigraphy (Broutin et al., 1990; DiMichele et al., 1996; Kerp, 1996). Because of EXPLANATIONS OF THE CORRELATION CHART these problems, additional biostratigraphic methods have been devel- The correlations in Figures 1 and 2 are based mainly on tetrapod oped: zonations based on amphibians (e.g. Boy, 1987; Werneburg, 1996, 1999; Werneburg and Schneider, 2006, in press), conchostracans (Mar- and insect bio-zones or lineage-zones (e.g. Werneburg, 1996; Werneburg and Schneider, 2006, in press; Schneider, 1982; Schneider et al., 2003), tens, 1983 ff.), blattid insects (cockroaches) (Schneider, 1982; Schneider et al., 2003), freshwater shark teeth (e.g., Schneider et al., 2000) and because of the above discussed constraints and limitations in the appli- cations of nonmarine biostratigraphic methods. The relatively closely on tetrapod footprint associations (e.g. Haubold, 1973; Boy and Fichter, 1982; Gand, 1985; Lucas, 1998). The application of these tools, how- spaced sequence of amphian and insect bearing horizons in the Thuringian Forest Basin has been used for the development of these ever, is constrained by biological and physiogeographical factors, too (Schneider, 1989; Boy and Schindler, 2000), because different groups methods as well as for cross checking these methods against each other and additionally against isotopic ages (Lützner et al. 2003; Lützner et of organisms have distinct migration potentials. For instance, the dis- persal of exclusively aquatic animals, such as fishes, is restricted to al. 2005, in press.). Because of the comparatively large amount of biostratigraphic data and isotopic ages, the profile of the Thuringian For- 283

FIGURE 1. Correlation chart of late Late Pennsylvanian and Permian continental basins - New Mexico, France, Germany. est Basin acts together with the profiles of the Saale Basin, the Saar Desmoinesian, fusulinids (Wengerd, 1959b, 1959a) Nahe Basin, the North German Basin and (newly) the Lodève Basin as reference sections for the continental European late Pennsylvanian and · Gray Mesa Formation (upper part): late Desmoinesian, Permian. In contrast to most of the European basins, the macro- and fusulinids (Wengerd, 1959b, 1959a) microflora is consequently investigated and revised only in the Czech basins during the last decades. Therefore, paleobotanical data nearly · Atrasado Formation: Missourian, fusulinids (Wengerd, exclusively from there were partially considered for correlations. For 1959b, 1959a; Martin, 1971) numerical ages of the global scale we use the data published by Menning and the German Stratigraphic Commission (2002); for the Carbonifer- · Bursum Formation: Virgilian to Wolfcampian (Krainer ous/Permian boundary the 299 Ma age given by Ramezani et al. (2003) et al., 2001; Lucas and Krainer, 2004); Virgilian, conodonts is adopted. (Orchard et al., 2004); Stephanian C to Lower Rotliegend, The French terms Autunian, Saxonian and Thuringian, often used blattid insects (Schneider et al., 2004), as well as based in Europe to designate so called West European chronostratigraphic on spiloblattinid fragments latest Gzhelian/Early Asselian stages, are in reality lithostratigraphic units only (e.g. Schneider, 2001; (Schneider, herein); ?latest Pennsylvanian to Early Per- comp. Broutin et al., 1999). They are equivalents of German mian, tetrapod skeleton remains, Eryops sp., lithostratigraphic units as follow (table 1 and 2, left columns): Autunian Trimerorachis sp., Edaphosaurus sp., Sphenacodon sp., is equivalent to the German Lower Rotliegend, Saxonian (type area Dimetrodon cf. milleri, caseids (Harris et al., 2004) Sachsen(=Saxony)-Anhalt in Germany) is equivalent to the Upper Rotliegend, Thuringian (type area Thuringia in Germany) is equivalent to the Zechstein. French Massif Central The following compilation is based on the direct knowledge of Lodève Basin the basins by the senior author, J.W.S. as well as the cooperation of the “Freiberg team” of biostratigraphers, especially R. Werneburg, and data · Graissesac Formation: 295.5 ± 5.1 Ma (U/Pb) from the cited literature as well. (Bruguier et al., 2003); Stephanian C macroflora (Galtier United States in Lopez et al., 2005)

New Mexico-Lucero Uplift · Usclas-St. Privat Formation: Melanerpeton pusillum - Melanerpeton gracile or Discosauriscus austriacus-zone · Sandia Formation: upper Atokan, fusulinids (Martin, (Werneburg, 1996; Werneburg and Schneider, 2006, in 1971) press)

· Gray Mesa Formation (lower part): early · Viala Formation: 289.3 ± 6.7 Ma (U/Pb) (Schneider et 284

FIGURE 2. Correlation chart of late Late Pennsylvanian and Permian continental basins - Czech Republic, Italy, Morocco, Ukraine, Southern Africa.

al., 2006, in press.) (Schneider et al., 2006, in press); Melanerpeton pusillum – M. gracile-zone (Werneburg and Schneider, 2006, in · Salagou Formation (Octon Member): 284 ± 4 Ma (U/ press) Pb) (Schneider et al., 2006, in press); insects,

conchostracans Kungurian/Roadian (Gand et al., 1997; Bourbon l’Archambault Basin Bethoux et al., 2002) · Buxières Formation: Bohemiacanthus type Buxières; · La Lieude Formation: base close to IR (Bachtadse pers. 289 ± 4 Ma (Pb/Pb) (Schneider et al., 2006, in press); comm. 2004); this is supported by a drastically short Melanerpeton pusillum – M. gracile-zone (Werneburg, termed change from playa deposits to alluvial plain de- 2003); Sysciophlebia alligans-zone, uppermost Lower posits at the base of the La Lieude Formation, linked to a Rotliegend or Autunian respectively (Schneider, herein) fast climatic change – possibly caused by the onset of the Upper Permian (Lopingian) Zechstein and Bellerophon Blanzy-Montceau Basin transgressions (Schneider et al., 2006, in press.; Legler et al. 2005, in press) · Montceau Formation: Syscioblatta lawrenceana-zone Autun Basin / Sysciophlebia grata- to S. rubida-zone, Stephanian B/C transition (Schneider, herein) · Muse Formation: Melanerpeton sembachense - Apateon dracyiensis or Apateon flagrifer flagrifer - Branchierpeton reinholdi-zone (Werneburg, 1996; Werneburg and Germany Schneider, 2006, in press); Syscioblatta dohrni to Sysciophlebia balteata-zone, lowermost Rotliegend or Saar-Nahe Basin lowermost Autunian respectively (Schneider, herein) · Saarbrücken Subgroup, Luisenthal Formation: Archimylacris lubnensis-zone, lower Westphalian D · Millery Formation: Bohemiacanthus type Buxières (Schneider et al., 2005, in press) 285 · Göttelborn to Heusweiler Formation, Ottweiler Sub- ± 2 Ma (295 ± 3 to 291 ± 2) (Ar/Ar) (Goll and Lippolt, group: Pseudestheria limbata/Ps. rimosa - Lioestheria 2001) form Köllerbach - Assemblage-Zone, Stephanian A/B (Schneider et al., 2005, in press) · Ilmenau Formation: Apateon dracyiensis - Melanerpeton sembachense-zone (Werneburg, 1996; · Dilsburg Formation, lower Ottweiler Subgroup: 302.7 Werneburg and Schneider, 2006, in press) ± 0.6 Ma, Ar/Ar (Burger et al., 1997) · Manebach Formation: Apateon dracyiensis - · Göttelborn Formation, lower Ottweiler Subgroup: Melanerpeton sembachense-zone (Werneburg, 1996; Syscioblatta intermedia-Sysciophlebia sp. A-zone, Werneburg and Schneider, 2006, in press); Stephanian A (Schneider et al., 2005, in press) Bohemiacanthus Um/Om-zone (Schneider, 1985, 1996) = upper Bohemiacanthus lauterensis to palatinus-zone · lowermost Heusweiler Formation, middle Ottweiler (Hampe, 1989; Schneider, 1996); Sysciophlebia ilfeldensis Subgroup: Spiloblattina pygmae-zone, Stephanian B to S. balteata-zone (Schneider, 1982; Schneider and (Schneider, 1982; Schneider and Werneburg, 1993) Werneburg, 1993)

· Breitenbach Formation: Bohemiacanthus Ug - zone · Goldlauter Formation: 288 ± 7 Ma (Lützner et al., 2003; (Schneider and Zajic, 1994); Sysciophlebia euglyptica - Lützner et al., 2006, in press); Spiloblattina homigtalensis Syscioblatta dohrni-zone (Schneider and Werneburg, - S. sperbersbachensis to Sysciophlebia balteata-zone 1993); 300 ± 2.4 Ma (Ar/Ar) (Burger et al., 1997) (Schneider, 1982; Schneider and Werneburg, 1993); Bohemiacanthus Ugo/Ogo-zone (Schneider, 1985) = · ?Göttelborn to Breitenbach Formation: SN a- Bohemiacanthus palatinus-zone (Hampe, 1989; Schneider, xenacanthid-zone (Hampe in (Schneider et al., 2000) 1996); Apateon flagrifer flagrifer-Branchierpeton reinholdi - to Melanerpeton eisfeldi-zone (Werneburg, · Remigiusberg to Wahnwegen Formation: SN ß- 1996; Werneburg and Schneider, 2006, in press) xenacanthid-zone (Hampe in (Schneider, et al., 2000) · Oberhof Formation: 287 ± 2 Ma (282 ± 2) (Ar/Ar) (Goll Apateon flagrifer oberhofensis - · Quirnbach to higher Meisenheim Formation: SN ?- and Lippolt, 2001); Melanerpeton arnhardti - to Melanerpeton pusillum – M. xenacanthid-zone (Hampe in Schneider et al., 2000) gracile-zone (Werneburg, 1996; Werneburg and Schneider, 2006, in press) · Meisenheim Formation: 297 ± 3.2 Ma (U/Pb-SHRIMP) (Königer, 2000) · Rotterode Formation: Moravamylacris kukalovae-zone (Schneider, herein) · Upper Meisenheim Formation: SN d-xenacanthid-zone (Hampe in (Schneider et al., 2000) · Tambach Formation: Elgersburg rhyolithe 275 ± 4 Ma (U/Pb) (Lützner, et al., 2003; Lützner et al., 2006, in press); · Top Meisenheim Formation: SN e-xenacanthid-zone Moravamylacris kukalovae-zone (Schneider, herein); Melanerpeton pusillum (Hampe in (Schneider et al., 2000); Lioestheria monticula-zone (Martens, 1987) = L. andreevi – M. gracile-zone (Werneburg and Schneider, 2006, in -zone (Holub and Kozur, 1981); Seymouria sanjuanensis, press) earliest Wolfcampian (Berman and Martens, 1993); Dimetrodon teutonis, early Kungurian (Werneburg and · Dissibodenberg Formation to lower Nahe Subgroup: Schneider, 2006, in press) SN ?-xenacanthid-zone (Hampe in Schneider et al., 2000) · Eisenach Formation: Pseudestheria wilhelmsthalensis- · Dissibodenberg Formation: Spiloblattina zone (Martens, 1987) odernheimensis - Sysciophlebia n. sp. B-zone (Schneider and Werneburg, 1993) · Förtha Formation: Lueckisporites virkkiae, Corisaccites, Capitanian to Abadehian (Kozur, 1988) · Donnersberg Formation: 290.7 ± 0.9 Ma (Rb/Sr) (Hess and Lippolt, 1989); inconsistent age after Lützner et al. · Zechstein Group: Merrillina divergens in the 1. cycle

(2003) and Lützner et al. (2006, in press) (Werra) carbonates - lower Wuchiapingian (Bender and Stoppel, 1965; Kozur, 1994); 257.3 ± 1.6 Ma Re/Os iso- · Wadern Formation, Sobernheim horizon: topic age of the Kupferschiefer at the base of the Zechstein Moravamylacris kukalovae-zone (Schneider, herein) (Brauns et al., 2003); see North German Basin, below.

Thuringian Forest Basin Saale Basin · Gehren Subgroup: Apateon intermedius - · Siebigerode Formation, Wettin Subformation: Apateon Branchierpeton saalensis-zone (Werneburg, 1996; intermedius -Branchierpeton saalensis-zone (Werneburg, Werneburg and Schneider, 2006, in press); 1996; Werneburg and Schneider, 2006, in press); Bohemiacanthus Ug-zone (Schneider and Zajic, 1994); Bohemiacanthus Ug - zone (Schneider and Zajic, 1994); Sysciophlebia euglyptica - Syscioblatta dohrni-zone Sysciophlebia euglyptica - Syscioblatta dohrni-zone (Schneider, 1982; Schneider and Werneburg, 1993); 293 (Schneider and Werneburg, 1993); 293 ± 2 Ma (295 ± 3 286 to 291 ± 2) (Ar/Ar) (Goll and Lippolt, 2001) 1995a, 1995b)

· Halle Formation: 297-301± 3 Ma (U/Pb-SHRIMP) · Müritz Subgroup: Lioestheria andreevi - Pseudestheria (Breitkreuz and Kennedy, 1999); Apateon intermedius - graciliformis - Palaeolimnadiopsis wilhelmsthalensis-as- Branchierpeton saalensis-zone (Werneburg, 1996; semblage-zone, Upper Rotliegend I (Hoffmann et al., 1989; Werneburg and Schneider, 2006, in press) Schneider et al., 2005, in press)

· Upper Hornburg Formation: conchostracans, · Parchim Formation: Illawara Reversal in the basal part Lioestheria andreevi - Pseudestheria graciliformis - (Menning, 1995) Palaeolimnadiopsis wilhelmsthalensis - assemblage-zone (Hoffmann et al., 1989; Schneider et al., 2005, in press) · Zechstein Group: see Thuringian Forest Basin; Mesogondolella britannica in the Kupferschiefer, · Eisleben Formation: equivalent to the Hannover For- Wuchiapingian (Legler et al., 2005, in press) mation of the North German Basin Döhlen Basin · Zechstein Group: see Thuringian Forest Basin · Döhlen Formation: Stephanian/Lower Rotliegend tran- sitional flora (Barthel, 1976); after macroflora the Döhlen Ilfeld Basin Formation is younger as the Wettin-Subformation, · Netzkater Formation: Apateon intermedius - Stephanian C of the Saale Basin and of similar age as the Branchierpeton saalensis-zone (Werneburg, 1990, 1996; Netzkater Formation of the Ilfeld Basin (Barthel, 1976; Werneburg and Schneider, 2006, in press); Sysciophlebia Schneider and Barthel, 1997) ilfeldensis-zone (Schneider, 1982) · Niederhäslich Formation: Melanerpeton pusillum – M. · Sülzhayn Formation: 290 Ma (Ar/Ar) (Lippolt and gracile-zone (Werneburg, 1996; Werneburg and Schneider, Hess, 1996) 2006, in press)

· Walkenried Formation: equivalent to the Hannover Formation of the North German Basin Czech Republic Central and Western Bohemian Basins · Zechstein Group: see Thuringian Forest Basin · Kladno Formation, Radnice Member: macroflora, Bolsovian (Pešek, 2004); Archimylacris lubnensis-zone, Erzgebirge Basin Bolsovian to lower Westphalian D (Schneider et al., 2005, · Zwickau Formation: Archimylacris form Zwickau-zone in press) (Schneider et al., 2005, in press) · Kladno Formation, Nýrany Member: Branchiosaurus · Härtensdorf Formation: macroflora - Lower Rotliegend salamandroides - Limnogyrinus elegans-zone (Werneburg, (Barthel, 1976); lower Härtensdorf Formation - 1996; Werneburg and Schneider, 2006, in press); sporomorph zone VII, level Q8 (upper Kartamysh Forma- Westphalian D to Cantabrian, macro-/microflora (Pešek, tion) of the Donetsk Basin and higher; upper Härtensdorf 2004) Formation - sporomorph zone XIII, level S2 (lower Slavansk Formation) of the Donetsk basin.; Asselian · Týnec Formation: Barruelian, macroflora (Pešek, 2004) (Döring et al., 1999) · Slaný Formation, Hredle Member: Sysciophlebia · Leukersdorf Formation: Melanerpeton pusillum – M. grata-zone, Stephanian B (Schneider, 1982) gracile- to Discosauriscus austriacus -zone (Werneburg, 1996; Werneburg and Schneider, 2006, in press); lower- · Line Formation: Apateon intermedius - Branchierpeton most Leukersdorf Formation - sporomorph zone XVI, level saalensis-zone (Werneburg, 1996; Werneburg and S4 (upper Slavjansk Formation) of the Donetsk basin, Schneider, 2006, in press); macroflora, Stephanian C upper Asselian (DÖRING et al., 1999) (Pešek, 2004)

· Zechstein Group: see Thuringian Forest Basin Krkonoše-Piedmont Basin · Syrenov Formation: macroflora, early Stephanian B North German Depression (Šimunek in Pešek, 2004) · Lower Ignimbrite: 302 ± 3 Ma (U/Pb, SHRIMP) (Breitkreuz and Kennedy, 1999) · Semily Formation, Plouznice Horizon: macroflora, Stephanian C (Pešek, 2004); Spiloblattina lawrenceana · Sediment intercalations within the volcanics: and Sysciophlebia rubida-zone = late Stephanian B Bohemiacanthus Om-Ugo-zone (Gaitzsch, 1995a, 1995b), (Schneider, 1982) Pseudestheria paupera and Pseudestheria palaeoniscorum, middle Lower Rotliegend (Gaitzsch, · Vrchlabí Formation: macroflora, Autunian (Pešek, 287 2004) (Werneburg, 1999; Werneburg and Schneider, 2006, in press; Ronchi et al., 2006, this volume) · Prosec· né Formation: macroflora, late Autunian (Šimunek in Pešek, 2004) Morocco Intra-Sudetic Basin Sous Basin and Argana Basin · •aclér Formation: macroflora, Late Namurian to · Oued Issene Formation: Spiloblattina pygmaea- and Bolsovian (Pešek, 2004) Sysciophlebia grata- zones, Stephanian B (Hmich et al. 2003, Hmich et al., 2006, this volume) · Odolov Formation: Sooblatta stephanensis, Stephanian B (Schneider, 1983; Pešek, 2004) · Ikakern Formation (T2 or Tourbihine Member): diplocaulid nectridean (Diplocaulus minimus), the · Chvalec· Formation: macroflora, Stephanian to captorhinid Acrodonta and a moradisaurine, Kazanian age Autunian (Pešek, 2004) (Middle Permian, Guadalupian) after Dutuit (1976, 1988) and Jalil and Dutuit (1996); transition Ait Driss / · Broumov Formation: macroflora, late Autunian Tourbihine Member (T1/T2) based on tetrapod tracks (Šimunek in Pešek, 2004); Melanerpeton pusillum - (Synaptichnium, Rhynchosauroides) latest Permian (S. Melanerpeton gracile-zone (Werneburg, 1996; Werneburg Voigt, personal comm., 2005) and Schneider, 2006, in press)

Ukraina Boskovice Graben Donetsk Basin · Rosice-Oslavany Formation: macroflora, Stephanian C (Pešek, 2004) · for marine correlations see Davydov and Leven (2003)

· Padochov Formation, Ríc· any Horizon: · Mironovsk Formtion (Araukararitovaja svita) P5 Coal Spiloblattina weissigensis-zone, middle Lower Rotliegend seam: possibly Pseudestheria limbata/Ps. rimosa - or Autunian respectively (Schneider and Werneburg, 1993) Lioestheria form Köllerbach - assemblage-zone, Stephanian A/B (Schneider et al. 2005, in press) · Letovice Formation, Zbonek-Svitavka Horizon: Sysciophlebia alligans-zone, upper Lower Rotliegend or Autunian respectively (Schneider and Werneburg, 1993) S-Africa Karoo Basin · Letovice Formation, Bac· ov Horizon: Discosauriscus austriacus -zone (Werneburg, 1996; · Deglaciation cycle II (Ganigobis Shale Member): 299.2 Werneburg and Schneider, 2006, in press); Obora Hori- ± 3.2 / 302.0 ± 3 Ma (SHRIMP) (Bangert et al., 1999); zon: Moravamylacris kukalovae-zone (Schneider, 1980) for interpretations of glaciation/deglaciation cycles see Scheffler et al. (2003)

Italy · Pietermaritzburg Formation: 288.0 ± 3.0 Ma (SHRIMP) (Bangert et al., 1999) Southern Alps · Bozen Volcanite Complex: Brack and Schaltegger · Collingham Formation: 270 ± 1.0 Ma (SHRIMP) (1999) report an 276.3 ± 2.2 Ma age fort he upper part of (Turner, 1999) the BVC, but up to now no agreement exist on the age of the whole BVC; Cassinis and Ronchi (2001) estimate an · Middleton Formation: 265 ± 2.5 Ma (SHRIMP) (Wanke late Carboniferous to early Permian age using different et al., 2000) data (for references see there) · lowermost Abrahamskraal Formation: Eodicynodon · Gröden Formation / Val Gardena Sandstone and A.Z. (Rubidge, 1995) Bellerophon Formation: tetrapod footprints Rhynchosauroides, Pachypes dolomiticus, Ichniotherium, · mid Abrahamskraal Formation (Koonap Formation): Dicynodontipus, uppermost Permian (Massari et al., Tapinocephalus A.Z. (Smith and Keyser, 1995a) 1999); sporomorphs, upper Tatarian (Massari et al., 1999); marine microfauna (Bellerophon Formation), Dzhulfian- · upper Abrahamskraal Formation (upper Koonap For- Dorashamian (Neri and Massari, 1999) mation) to lower Teeklof Formation (lower Middleton Formation): Pristerognathus A.Z. (Smith and Keyser, Sardinia - Perdasdefogu Basin 1995b)

· Rio su Luda Formation: Melanerpeton eisfeldi-zone, · mid Teeklof Formation (mid Middleton Formation): middle Lower Rotliegend or Autunian respectively Tropidostoma A.Z. (Smith and Keyser, 1995c) 288 · upper Teeklof Formation (upper Middleton Formation) shown by Lützner et al. (2003, 2005, in press), because tectonic reacti- to lower Balfour Formation: Cictecephalus A.Z. (Smith vations in the European Variscides and multiple Mesozoic thermal events and Keyser, 1995d) have upset the geochronologic systems throughout large areas. Only cross correlation in conjunction with biostratigraphic data enable the · mid Balfour Formation: Dicynodon A.Z. (Kitching, best fitting of isotopic ages for the time being. On the other hand, most 1995) of the numerical ages used for the stage boundaries are estimated ages only, not really measured (comp. Menning, 1995; Menning et al., 2000). · upper Balfour Formation to lowermost Burgersdorp These problems need a solution, if we are to understand biotic and Formation: Lystrosaurus A.Z. (Groenewald and Kitching, abiotic processes on the late Palaeozoic earth. 1995) The tables and explanations provided here as well as further correlation charts of Carboniferous and Permian basins are available at CONCLUSIONS www.geo.tu-freiberg.de/~schneidj/ The progressively improved tables should be cited as: Roscher, Reliable biostratigraphic data, derived from bio(chrono)species, M. and Schneider, J.W., (year). Carboniferous/Permian correlation charts are very accessible in most of the basins, particularly in the Pennsylva- - www.geo.tu-freiberg.de/~schneidj/ nian and lower half of the Cisuralian. The density of data depends We will be grateful for constructive criticism as well as the sup- merely on the intensity of investigations - see for example the Thuringian ply of published data or references, which we have overlooked or which Forest basin. Late Cisuralian, Guadalupian and Lopingian sediments are newly published. are mostly discontinuously developed in the overwhelming number of basins; compare Figures 1 and 2. Additionally, drastic changes in the ACKNOWLEDGMENTS environments took place during Permian time. In the Late Pennsylva- nian and the lowermost Early Permian, sedimentary environments in- The authors thank the Deutsche Forschungsgemeinschaft (DFG), clude alluvial plains with palustrine and lacustrine gray facies that who supported this study with the research grants DFG-SCHN 408/7, interfinger with relatively wet, red alluvial deposits (Schneider et al., which was a part of the SPP “Evolution of the System Earth,” as well 2006, in press). In the late Lower Permian and the early Middle Per- as the common project of M. Menning and J.W. Schneider DFG-Me mian, sedimentary environments evolved to increasingly dryer, red al- 1134/5-2 “Devonian-Carboniferous-Permian Correlation Chart.” The luvial plains with lacustrine gray facies restricted to depocenters only. German Academic Exchange Survey (DAAD) has contributed with the Playa red beds predominate during the Middle and Late Permian. Ma- grant A/01/00754 for investigations in Morocco, and the DFG with the rine incursions in the southern and northern foreland of the Variscan grant 436 UKR 18/1/02 for fieldwork in the Donetsk basin, Ukraine. morphogene, such as the Bellerophon transgression in southern Europe The DFG grant SCHN 408/8 enables the revision of Euramerian Car- and the pre-Zechstein incursions and the Zechstein transgression in boniferous and Permian conchostracans by J. Goretzki, well supported northern Europe, generated alternations of playa and sabkha environ- by V. R. Lozovsky, Moscow. The Geological Survey of Saxony, espe- ments (Legler et al., 2005, in press). Similarly, the biotic environments cially W. Alexowsky, H. Walter and H.J. Berger, is thanked for coop- and the fossil record changed. Insects are still common, as in the eration as well as for research and mapping projects in some German Tambach Formation of the Thuringian Forest basin and the Wadern basins. The studies in the North German Basin have been supported by Formation of the Saar Nahe basin; they are really frequent in the playa the Central Geological Institute, namely by N. Hoffmann, and the Erdöl/ red beds of the Salagou Formation of the Lodève basin and in the Erdgas Gommern company of the former GDR, later by the BEB, Mobil Wellington shales of Kansas and Oklahoma. Aquatic amphibians, such Oil and EEG hydrocarbon exploration companies in Germany. Recently, as the temnospondyl branchiosaurs, disappear because of the disap- these studies could be intensified by the DFG grant SCHN 408/10. pearance of stable lake biotopes. On the other hand, terrestrially-adapted J.W.S would like to thank his friends, especially G. Gand, of the Asso- amphibians and reptiles became more important for biostratigraphy ciation des Géologues du Permien et du Trias (AGPT) for common (Lucas, 1998, 2002; Lozovsky 2003). Unfortunately, they are not well excursions and research projects in the French Massif Central and else- enough known from Western Europe, but perspective sites exist, as where, his Czech, Ukrainian and Russian friends for decades of coop- shown by the Tambach locality in the Thuringian Forest (e.g. Martens eration in fieldwork and biostratigraphic studies as well as the team of et al., 1981; Berman and Martens, 1993) and the La Lieude site in the the New Mexico Museum of Natural History for current extensive co- Lodève basin (Schneider et al., 2006, in press). operative work in collections and the field. This inestigations are sup- Real serious problems are the direct biostratigraphic correlations ported by the DFG grant SCHN 408/12. S. Gosh, Geological Survey of to the marine scale. Besides single exceptions (Schneider et al., 1995b; India, and G. Schneider, Geological Survey of Namibia, enable J.W.S. Schneider et al., 2004), terrestrial zone fossils were rarely found in to get an idea of the Gondwana Carboniferous and Permian during field- well dated marine profiles. But again, the potential is much higher. work and excursions. We would like to thank Spencer G. Lucas (Albu- Very perspective plays are the Permian mixed marine/continental de- querque) for his linguistic improvements of the text. This publication posits of the North American Midcontinent basin and in the Volga- is a contribution to the tasks of the working group “Marine – non- Kama region of Tatarstan in Eastern Europe. Up to now, non-marine/ marine correlations” of the Subcommission on Permian Stratigraphy of marine correlations are based nearly exclusive on isotopic ages from the IUGS. volcanites of the continental basins. But, they are not unambiguous, as

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