Abstract Two outstanding Permian petrified forests, those of Chemnitz, in Germany, and northern Tocantins, in Brazil, contribute to the understanding of the composition, peculiarities and dynamics of Early Permian wetland ecosystems. These assemblages represent seasonally influenced, essentially contemporaneous but quite comparable, tree-ferndominated plant communities in the Northern and Southern Hemispheres. The Chemnitz fossils are embedded in coarse-grained pyroclastics of the Zeisigwald Tuff Horizon (Leukersdorf Formation, Erzgebirge Basin), whereas those of Tocantins occur in different lithofacies of a cyclic alluvial succession (Pedra de Fogo/Motuca formations, Parnaíba Basin). The outstanding three-dimensional preservation of particularly large fossil remains, made possible by siliceous permineralization, provides the opportunity to study the gross morphology, anatomy and internal organization of plant tissues, as well as taphonomical and ecological aspects of late Palaeozoic plants in a way not allowed by other preservational states. Recent studies of newly collected material permit a re-evaluation of the popular reconstructions of Early Permian floras. Various plant-plant and plant-animal interactions add to our understanding of two diverse lowland ecosystems that, irrespective of their different palaeogeographic position and taphonomic modes, show striking similarities.

Abstract A revised amphibian zonation for the European Pennsylvanian and Cisuralian (Upper Carboniferous to Lower Permian) with nine amphibian zones is presented. The index fossils belong to species-chronoclines with two or three closely related species. The time resolution of these amphibian zones is about 1.5–3.0 Ma. Biostratigraphical correlations with amphibian zones are applicable to 16 basins in the Czech Republic, Poland, France, Italy and Germany. The biostratigraphical potential of other tetrapods is discussed.

Abstract Late Palaeozoic sediments in central Morocco and the High Atlas Mountains document the development of this area during the formation of the Mauretanide part of the Hercynian orogeny. Continental basins formed during the Stephanian and Permian. Although scattered in time, they provide valuable bioGéographical and climatic information for the Mauretanides as a link between the Variscides in the east, the Appalachians in the west and the Karoo in the south. New blattid insects in the Souss Basin enable correlation to Early Stephanian B. Furthermore, we document the oldest African tetrapod tracks ( Batrachichnus, Dromopus ). Litho- and biofacies indicate seasonally wet and dry phases. Wet red beds of the Khenifra Basin have produced tetrapod bones and the tracks Limnopus, Batrachichnus and Dromopus . Macrofloras give a transitional Autunian/Saxonian age. This fits well into the Artinskian wet phase. Similar facies pattern in the Tiddas Basin are correlated by tetrapod tracks as transitional Artinskian to Kungurian. Advanced tetrapod tracks of Synaptichnium and Rhynchosauroides were discovered in the Ikakern Formation of the Argana Basin, dated by pareiasaur remains as Wuchiapingian. Red beds of similar type are known in Europe, for example, from the Late Permian of the Lodève Basin. They originated during the Wuchiapingian wet phase.

Abstract The Permian (299-251 Ma; Wardlaw et al. 2004 ) succession of Central Europe records the change from a Pangaea configuration and compressive tectonic regime inherited from the Variscan Orogeny, to the development of the broad thermal subsidence-controlled Southern Permian Basin and its inundation by the Zechstein Sea. During latest Carboniferous-Early Permian times, the final phase of Variscan orogenic extension produced a series of small strike-slip and extensional continental basins across central and western Europe. Within these basins Stephanian and Lower Rotliegend continental successions were deposited. Subsequent thermal subsidence led to the gradual coalescence of these isolated basins to form the large Southern Permian Basin which extended across much of central and western Europe (Fig. 10.1 ). Early Permian sedimentation was predominantly fluvial and lacustrine, changing later to aeolian. This change was due either to a significant climate change, or the result of a decline in relief of the surrounding uplands. By the end of the Early Permian extensive dunefields occupied the basin margins with saline lakes (playas) in the basin depocentres ( Verdier 1996 ). A regional, possibly glacio-eustatic, rise in sea level later in Permian (Zechstein) times resulted in the rapid flooding (from the north) of the Southern Permian Basin. The Zechstein succession comprises a series of evaporitic cycles, and associated carbonates and muds, reflecting progressively greater evaporation and the shallowing either of the whole basin or the margins of the basin. There has been a considerable amount of interest in the Permian in recent years, with a number