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Geodynamic Evolution of the Orogen: the West Carpathians and Ouachitas Case Study

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Geodynamic Evolution of the Orogen: the West Carpathians and Ouachitas Case Study Annales Societatis Geologorum Poloniae (2003), vol. 73: 145-167. GEODYNAMIC EVOLUTION OF THE OROGEN: THE WEST CARPATHIANS AND OUACHITAS CASE STUDY Jan GOLONKA1, Andrzej SL^CZKA1 & Frank PICHA2 1 Jagiellonian University, Institute o f Geological Sciences, Oleandry Str. 2a, 30-063 Krakow, Poland ~ 650 New Haven Court, Walnut Creek, CA 94598, U. S. A. Golonka, J., Sl^czka, A. & Picha, F. 2003. Geodynamic evolution of the orogen: the West Carpathian and Ouachitas case study. Annales Societatis Geologorum Poloniae, 73: 145-167. Abstract: Twelve time interval maps have been presented which depict the plate tectonic configuration, paleogcography and lithofacies for the circum-Carpathian area from the Late Carboniferous through Neogene and for the circum-Ouachita region from Late Cambrian through Early Permian. The following geodynamic evolutionary stages can be distinguished in these two orogens: Stage I - rifting of terranes off the major continent, forming oceanic basins (Triassic-Early Cretaceous in the Carpathian region, Cambrian-Devonian in the Ouachita region); Stage II - formation of subduction zones along the active margin, partial closing of oceanic basin, development of deep-water flysch basin associate with this rifting on the platform (passive margin) with the attenuated continental crust (Late Cretaceous-Paleocene in the Carpathian region, Early Carboniferous in the Ouachitas); Stage 111 - collision, perhaps terrane-continent, with the accompanying conver­ gence of two large continents, development of accretionary prisms, Eocene-Early Miocene time in the Carpathian region, Late Carboniferous in the Ouachitas; and Stage IV - postcollisional, (Miocene-Present-future? in the Carpathians, Permian-Triassic in the Ouachitas). Both, Carpathians and Ouachitas are accretionary prisms formed in response to terrane-continent and continent-continent collision. The paleogcographic approach we have taken shows how these mountain belts were constructed through the orogenic cycle, which reflects complex plate tectonic processes. Carpathians and Ouachitas record complete and homologous Wilson cycle. Key words: Plate tectonics, paleogeography, orogen, accretionary prism, Wilson cycle, Ouachita, Carpathians. Manuscript received 12 March 2003, accepted 5 November 2003 INTRODUCTION The aim of this paper is to compare the plate tectonic mas, 1989). The history of the whole circum-Carpathian evolution and position of the major crustal elements of the realm is more complex (e.g., see Golonka et al., 2000, Carpathians, and Ouachita Mountains within a global 2003a), if we concentrate however on the West Carpathians, framework and to show the relationship between tectonic the orogenic cycle is also clear and evident. Thus, these two processes and sedimentary record during their orogenic cy­ orogens could provide a good example to compare the mod­ cles. The Carpathian and Ouachita Mts are geographically ern and ancient orogens. distant. The age of the formation of each orogen is also quite Twelve time interval maps have been presented which different. The Carpathians mountain belt formed during depict the plate tectonic configuration, paleogeography and Mesozoic and Cenozoic time, while the Ouachitas formed lithofacies for the circum-Carpathian region and adjacent in the Paleozoic; their tectonostratigraphic history, how­ areas from the Late Carboniferous through Neogene and for ever, displays striking similarities. the circum-Ouachita region from the Late Cambrian Both orogens have been the subject of numerous classic through Early Permian. sedimentological studies of the deep-water flysch deposits The maps were constructed using the following defined (Ksiqzkiewicz, 1954; Dzulynski & Slqczka, 1958; Dzu- steps: lyriski et al., 1959; Dzulynski & Walton, 1965; Cline, 1960, 1. Construction of the base maps using the plate tec­ 1970; Lowe, 1976, 1989; McBride, 1975; Morris, 1974, tonic model. These maps depict plate boundaries (sutures), 1989; Moiola & Shanmugan, 1984; Pescatore & Sl^czka, plate position at the specific time and outline of present day 1984; Shanmugan & Moiola, 1995; Picha, 1996). The coastlines. Ouachita orogenic belt was also a subject of a tectonic syn­ 2. Review of existing global and regional paleogeo- thesis from the point of view of Wilson cycle (Viele & Tho­ graphic maps. 146 J. GOLONKA ET AL. 100 km ~EASTER ESIAN PLATFORM Tertiary Molasse Zone Flysch Belt B Pieniny Klippen Belt Pre - Neogene of inner Neovolcanic areas ' Neogene basins orogenic zones Fig. 1. Tectonic sketch map of the Alpine-Carpathian-Pannonian-Dinaride basin system (after Kovac et al, 1998; simplified) 3. Posting of generalised facies and paleoenvironment the rotation of crustal (basement) elements, rotation of database information on base maps. blocks separated by dextral faults (e.g. Marton et al., 2000) 4. Interpretation and final assembly of computer map or rotation of thrust sheets (e. g. Muttoni et al., 2000b). files. Measurement in flysch deposits could also indicate the ar­ The maps were constructed using a plate tectonic rangement of magnetised grains (domains) by turbiditic cur­ model, which describes the relative motions between ap­ rents. For example, the magnetic declination of Podhale proximately 300 plates and terranes. This model was con­ Flysch in Poland records perhaps the sedimentological ar­ structed using PLATES and PALEOMAP software (see rangement of grains (see the maps of sedimentological Golonka et a/., 1994, 2000, 2003a) which integrate com­ transport in the Carpathian flysch, e.g. Ksiazkiewicz, 1962) puter graphics and data management technology with a changed by the crustal rotation of the Inner Carpathian plate highly structured and quantitative description of tectonic re­ to the present position. The crustal rotation in a range of lationships. The heart of this program is the rotation file, 20-30° agrees with the general geodynamic evolution of the which is constantly updated, as new paleomagnetic data be­ area (Golonka et a l, 2000). come available. Hot-spot volcanics serve as reference points Information from several general and regional paleo- for the calculation of paleolongitudes (Golonka & Bocha­ geographic papers was filtered and utilized (e.g., Ronov et rova, 2000). Ophiolites and deep-water sediments mark al., 1984, 1989; Dercourt et a l, 1986, 1993, 2000; Ziegler, paleo-oceans, which were subducted and included into fold- 1988, 1989; Stampfli et a l, 1991, 1998, 2001; Stampfli, belts. Magnetic data have been used to define paleolatitu- 2001; Kovac et a l, 1998; Plasienka, 1999; Neugebauer et dinal position of continents and rotation of plates (see e.g. a l, 2001; Golonka & Ford, 2000; Golonka et a l, 2000, Van dcr Voo; 1993; Besse & Courtillot 1991; Krs et a l, 2003a). The authors of this paper also used unpublished 1996). An attempt has been also made to utilise the paleo­ maps and databases from the PALEOMAP group (Univer­ magnetic date from minor plates and allochtonous terranes sity of Texas at Arlington), PLATES group (University of (see e.g. Patrascu et a l, 1992, 1993; Pechersky & Safronov Texas at Austin), University of Chicago, Institute of Tec­ 1993; Beck & Schermer 1994; Channell et al., 1992, 1996; tonics of Lithospheric Plates in Moscow, Robertson Re­ M auritsch et al., 1995, 1996; Feinberg et al., 1996; Krs et search in Llandudno, Wales, and the Cambridge Arctic al., 1996; Marton and Martin 1996; Marton et al., 1999, Shelf Programme. The plate and terrane separation was 2000; Haubold et al., 1999; Muttoni et al., 2000a, b; Gra- based on the PALEOMAP system (see Scotese & Lanford, bowski, 2000). The nature of rotation indicated by paleo- 1995), with modifications in the Tethys area (Golonka et magnetism measured in sedimentary rocks in allochthonous a l, 2000, 2003a). The calculated paleolatitudes and pale­ terranes remains somewhat uncertain. It could be caused by olongitudes were used to generate computer maps in the Mi­ WEST CARPATHIANS AND OUACHITAS 147 European platform general Inner Carpathian Paleogene + + + === Alpine-Carpathian foredeep Inner Carpathian Paleozoic and Mesozoic Outer Carpathian flysch Neogene Volcanics Pieniny Klippen Belt Neogene of Pannonian and Vienna Basins Fig. 2. Geological map of West Carpathians and adjacent areas. (Modified from Wessely and Liebl, 1996). Abbreviations: ZG - Zglobice-Wieliczka Unit, CA - Chamahora-Audia Unit, PC - Porkulec-Convolute Unit crostation design format using the equal area Molweide pro­ known as the Outer or Flysch Carpathians (Mahel, 1974; jection. Ksi^zkiewicz, 1977; Sl^czka & Kaminski, 1998). At the This paleogeographic approach shows how a mountain boundary of these two ranges lies the Pieniny Klippen Belt belt was constructed through the orogenic cycle, which re­ (PKB) (Fig. 2). The Inner Carpathians are regarded as a pro­ flects complex plate tectonic processes. Some unsolved longation of the Northern Calcareous Alps, and formed part questions and problems could be answered by a comparison of the Apulia plate in regional sense that is a promontory of between one and another orogen. the African plate (Picha, 1996). They are divided into the Tatric, Veporic and Gemeric nappes (Fig. 2) that are the prolongation of the Lower, Middle and Upper Austroalpinc TECTONIC SETTING nappes respectively (Pescatore & Sl^czka, 1984). The Inner Carpathians nappes contact along a Tertiary strike-slip boundary with Pieniny Klippen Belt (Fig. 2, 3). The Pieniny WEST CARPATHIANS Klippen Belt (PKB) is composed of several successions The Carpathians form a great
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