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Paleozoic Tectonostratigraphic Development and Paleogeography of Brunovistulian Terrane and Comparison with Other Terranes at the SE Margin of Baltica-Laurussia

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Paleozoic Tectonostratigraphic Development and Paleogeography of Brunovistulian Terrane and Comparison with Other Terranes at the SE Margin of Baltica-Laurussia Journal of the Czech Geological Society 47/34(2002) 81 Late Proterozoic Paleozoic Tectonostratigraphic Development and Paleogeography of Brunovistulian Terrane and Comparison with Other Terranes at the SE Margin of Baltica-Laurussia Svrchnoproterozoický paleozoický tektonostratigrafický vývoj a paleogeografie brunovistulického teránu a srovnání s dalími terány na JV okraji Baltiky-Laurusie (9 figs, 2 tabs) JIØÍ KALVODA1 ROSTISLAV MELICHAR2 ONDØEJ BÁBEK3 JAROMÍR LEICHMANN4 1 Department of Geology and Paleontology, Kotláøská 2, 61137 Brno, [email protected] 2 Department of Geology and Paleontology, Kotláøská 2, 61137 Brno, [email protected] 3 Department of Geology, Tø. Svobody 26, 771 46 Olomouc; [email protected] 4 Department of Geology and Paleontology, Kotláøská 2, 61137 Brno, [email protected] There are close similarities between the Brunovistulian Terrane and the Istanbul Zone both in the Neoproterozoic and Paleozoic. The geological structure, lithology and geochronology of the Cadomian Brunovistulicum show a broad fit with the crystalline basement of the Istanbul Zone. Their Gondwana or Baltica affinity is still poorly constrained and remains a matter of discussion. The Vendian and Cam- brian sequences recognized in the central Malopolska, Brunovistulian and Moesian terranes correlate well with the Scythian Platform. In the Istanbul Zone the presence of pre-Ordovician sedimentary sequences has not been confirmed and may only be anticipated. In Paleozoic the best fit was attained in the DevonianCarboniferous. The sedimentary record in the Zonguldak and Istanbul terranes correlates closely to the Moravian Karst and Ludmírov facies developments of the Brunovistulian Terrane. This correlation is reinforced by the good fit of the main Variscan deformation phases attributed in both the Brunovistulian Terrane and the Istanbul Zone to the late Viseanearly Namurian and Westphalian-Stephanian intervals. This supports, together with the paleobiogeographical data, the interpretation that the Istanbul and Zonguldak terranes can be regarded as counterparts to the Rhenohercynian and Subvariscan Zone in Central Europe. The Istanbul Zone was juxtaposed against the Sakarya Zone viewed as a part of the Armorican Terrane Assemblage. Key words: Brunovistulicum, Istanbul Zone, terranes, paleogeography, late Neoproterozoic, Paleozoic A. Introduction bul Zone in Asia Minor (Pharaoh 1999, Belka et al. 2000, Kalvoda 2001). Kalvoda (2001, 2002) termed these ter- The affinity of the terranes at the SE margin of Laurus- ranes as the Brunovistulian group based both on similar sia to major continents is not clear and has been a mat- geotectonic position and paleobiogeographic similarities. ter of some discussion. A long term late Neoproterozoic A comparison will be made also with the Scythian oro- (Cadomian, Panafrican) consolidation was regarded as a gen (see Fig. 2) that fringes the southern margin of the reliable criterion for distinguishing Perigondwana-derived East European Craton and is regarded as an eastern pro- terranes. Nevertheless, late Neoproterozoic deformations longation of the Variscan orogen in Central Europe. have been recently reported in the Timanides and the Urals or assumed in the Scythian Platform (Zoubek 1992, B. Geological Setting Puchkov 1998, Glasmacher et al. 1998, 1999, Pharaoh 1999, Gee 2001) and in southern Poland (Zelazniewicz In the Brunovistulian Terrane, the Cadomian age of the et al. 1997). The supposed Panafrican provenance of basement cropping out primarily in the Brno Massif has some crustal elements thus requires careful scrutiny be- been well established (van Breemen et al. 1982, Dallm- fore an interpretation of their affinity. eyer et al. 1994, Finger et al. 2000a). The term Bruno- The present paper builds on the work of the authors vistulian is preferred here to other synonyms Upper in Moravia where the best data on the Cadomian base- Silesian or Moravian-Silesian because the Upper Sile- ment and DevonianCarboniferous sediments and pale- sian Massif forms only the northern part of the Brunovis- obiogeography are available and their study has a long tulian unit and the Moravian and Silesian units are narrow tradition. An effort here is made to view these data with- zones formed mostly by metamorphosed Brunovistulicum in the broader pattern of the NeoproterozoicPaleozoic at the contact with Moldanubian and Saxothuringian (Lu- tectonostatigrahic and paleogeographic development of gian) units of the Armorican Terrane Assemblage. The the southern Baltica Laurussia margin. Brunovistulicum (BVT see fig. 1) is separated from the A collage of various crustal blocks was derived either Malopolska Terrane by a tectonic unit known as the Kra- from Baltica or Gondwana and accreted to the Precam- kow-Lubliniec Fault Zone that is a part of the largely brian East European Craton (EEC) along the Transeuro- concealed Hamburg-Krakow Fault Zone (see fig. 1) par- pean Suture Zone (TESZ) to form the southeastern mar- allel to the Transeuropean Suture Zone (TESZ). This fault gin of Laurussia during the Variscan orogeny. These zone continues southeast of Krakow, where Carpathian includes the Lysogory, Malopolska, Brunovistulian and flysch is thrust over the Paleozoic basement (Bula Ja- Moesian terranes in Central and SE Europe and the Istan- chowicz 1997). In the North the Holly Cross Fault sepa- 82 Journal of the Czech Geological Society 47/34(2002) Fig. 1 Structural setting of the Brunovistulian, Malopolska and Lysogory terranes. Modified according to Bula et al. (1977). BVT Brunovistu- lian Terrane, MT Malopolska Terrane, LT Lysogory Terrane, HKFZ Hamburg-Krakow Fault Zone, HCF Holy Cross Fault, TESZ Trans- european Suture Zone, MSFZ Moravo-Silesian Fault Zone, PPFZ Peri-Pieninian Fault Zone, VDF Variscan Deformation Front, CDF Caledonian Deformation Front, AF Alpine Front. Journal of the Czech Geological Society 47/34(2002) 83 rates the Malopolska Terrane from the Lysogory Terrane from the Brunovistulian Terrane along the TESZ during (see Fig. 1). the opening of the proto-Pannonian marginal basin in late In the Malopolska Terrane the Cadomian basement has Triassicearly Jurassic. only been proposed based on the presence of late Neopro- According to Pharaoh (1999), the basement of the terozoic detrital micas (Belka et al 2000). In the Lyso- Moesian Platform (see Fig. 2) resembles that of the Ukrai- gory terrane (Fig. 1), detrital micas in Cambrian silici- nian Shield. However, the affinity of the terrane is poor- clastic rocks show a wide age spectrum with well defined ly constrained at present. Geophysical evidence (Seghe- Archean, Early Archean, Mesoproterozoic and late di, 1998) suggests that the deep crustal boundary of the Neoproterozoic ages (Valverde-Vaquero et al. 2000). EEC (TESZ) corresponds to the surface position of the Some interpretations favour a Gondwana origin for the Peceneaga-Camena Fault, a NE-vergent Cimmerian-age Malopolska and Lysogory terranes (Belka et al. 2000). thrust that juxtaposes Precambrian rocks of the Moesian In other interpretations they are regarded as slivers of Platform with Permian-late Jurassic strata of the North Baltica and it is inferred that the Neoproterozoic crust is Dobrogea orogen (Seghedi 1998, Pharaoh 1999). The of Assyntian affinity, derived either from the Scythian Paleozoic position of the Moesian Terrane is also a mat- Platform or the Uralian margin of Baltica (Pharaoh 1999). ter of discussion. Yanev (1997, 2000) inferred a Perigo- It is hypothesized that both the Brunovistulian Terrane ndwana affinity and middle Devonian accretion to Lau- and the Malopolska Terrane were detached from the an- russia. cestral Crimea-Dobrogea region (Scythian Platform) and According to Nikishin et al. (1996, 1999) the Scyth- dextrally transferred along the margin of the Laurussia ian orogen (see Fig. 2) that fringes the southern margin during Variscan time (Lewandowski 1993, 1994, Grygar of the East European Craton includes the Scythian, Great 1998, Belka et al. 2000). Unrug et al. (1999) and Nawroc- Caucasus (Karpinsky Kryazh fold belt), Pontides and ki (2000), on the other hand, stressed the importance of Moesian domains. It is viewed as being the eastern pro- late Silurian Caledonian movements. longation of the Variscan orogen of Western and Central The prolongation of the Malopolska Terrane to the SE Europe. may constitute the Dobrogean part of the Moesian Ter- The Istanbul zone (Okay 1989, 2000, Okay et al. 1994) rane (Unrug et al. 1999). A correlation between the Moe- lies within the western Pontides in northern Turkey. It is sian and the Moravo-Silesian (Brunovistulian) Terrane, assumed that it was located originally along the Odessa based on similar structural position with regard to the East shelf between the Moesian Platform and Crimea and drift- European Craton, has been proposed by Burchfiel (1975) ed southward along the major trasform faults following and Matte et al. (1990). According to Banks and Robin- an oblique slip on the TESZ, to form the western Black son (1997) the Moesian Terrane was sinistrally displaced Sea Basin during the development of the western Black Late Cretaceous Oceanic crust Alpide orogens Regional fold arc magmatism trends Fig. 2 Tectonic map of the Black Sea re- Hercynian zones Late Cimmeride Suture lines gion showing the position of the Moesian Early Cimmeride zones zones and Zonguldak terranes. Modified after Okay et al. (1994). Major post-Eocene thrust Strike-slip fault 84 Journal of the Czech Geological Society 47/34(2002) Sea
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