VOLUME 18 (4)/August 1988

The tectonic link between the Balkanides and the South Carpathians is accomplished through an arc which follows the western margin of the Moesian plate. The arc consists of three partial arcs. They show different rock composition, structure and development. The central strip (Hemus-Danubian partial arc) is a chain of large autochthonous to paraautochthonous anticlines. It originated on the Thraco-Moesian suture – the boundary between the Thracian and Moesian lithospheric plates. Its development may be traced from the Vendian-Cambrian to the last folding during the lllyrian phase. The Severin partial arc is located between the suture and the Moesian plate. It developed from the Tithonian to the end of the Late Cretaceous. The Srednogorie-Getic partial arc was formed after the Austrian phase, behind the Hemus-Danube partial arc. It evolved as a consequence of recurrent rifting, very intensive during the Late Cretaceous, Paleogene and the Neogene. It is thrusted on the Hemus-Danube and Severin partial arcs.
   The Kraištide structural zone is independent from the Balkan-Carpathian arc. It is slightly arcuate. The zone originated along a directrice of 160-170° and only its northern and southern termination were rotated as a result of the wedging-in of the Moesian plate to the west. Thus, it may be understood as an open arc, unconformable and renegant with respect to the Balkan-Carpathian arc. Three longitudinal strips of different rock composition, structure and development are recognized in the Kraištide structural zone. The eastern strip (Trân-Kučai) is a chain of large autochthonous anticlines. The middle (Krepolin-Penkjovci) comprises mainly Lower Paleozoic rocks thrusted over the autochthonous unit. The inner (Morava) strip is made up of the Vendian-Cambrian Tribalian geocomplex, thrust to the east over the middle unit. The evolution of the Kraistides may be traced throughout the Phanerozoic . They are superimposed on the Thracian microcontinent.

E. Kozhoukharoua, M. G. Leontiev. Ductile deformation and metamorphism in Southern Tian-Shan. Early Paleozoic sequences of the Ganza-Chimtargin Massif in Southern Tian-Shan are represented by the complex of the so-called green (chlorite) schist: basic volcanics and tuffs, sandstones, siltstones and quartzites all metamorphosed in green chist facies. Metamorphic phenomena (recrystallization, differentiation and schistosity) had taken place in two stages (Paleozoic and Alpine) and developed irregularly in space and intensity. A relationship between the degree of metamorphism, the initial lithologic features of the rock and the character and intensity of: structural deformations has been observed. Most intensive structural and material transformations are bound to zones of most active ductile deformations. Therefore, the ductile deformation plays the role of a thermodynamic factor of metamorphism.

No abstract is available for this article.

No abstract is available for this article.