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Miocene plate tectonic activity created regions of relatively restricted marine sedimentation—the Mediterranean and the Paratethys Seas—which evolved from the Tethyan Ocean. These resulting configurations brought about periodic faunal exchanges between central Europe, the marine realms of the Indo-Pacific and the terrestial realms of Africa. Rapid change in marine depositional environments occurred during the middle Miocene in the Paratethys Sea. After a peak in marine sedimentation during the early Badenian, there was a widespread desiccation in the late middle Badenian in the Carpathian foredeep and eastern intramontaine basins. This "salinity crisis" was caused by the closing of the marine seaway to the Indo-Pacific and gave rise to the brackish water "Spaniodon" beds of the Karaganian Stage of the eastern Paratethys Sea. Late Badenian floral and faunal assemblages indicate that the seaway to the Indo-Pacific was reopened and the Paratethys area again flooded, whereas the seaway to the Mediterranean had disappeared. Finally, within the late Miocene and Pliocene the Paratethys area was isolated from any marine influence and has become progressively more fresh since that time. INTRODUCTION Application of the concepts of plate tectonics to the Alpine System demonstrates that during the Tertiary a change in relative African-European plate motions occurred during which earlier counterclockwise rotation and trascurrent motion became mainly convergent motion (Dewey et al., 1973; Hsü, 1971; McKenzie, 1970; Neev, 1975). This collision broke up the Tethys oceanic realm which had existed since the early Mesozoic and resulted in the (T 9—Tethys phase of Dewey et al., 1973) formation of several relatively small basins and troughs during the Neogene. These basins and troughs are the Mediterranean and Paratethys seas, the Mesopotamian Basin, and the oceanic trough which stretches towards the Indo-Pacific Ocean. Continuing compressional forces from the Oligocene onward, markedly increased subduction, transform faulting, and thrusting developed several sedimentary regions within the Central Paratethys: the AlpineCarpathian foredeep and a number of intramontaine basins (Senes et al., 1971). The evolution of progressively differentiated faunal assemblages within these Neogene seas resulted in the development of regional stage concepts for the Mediterranean, and the central and eastern Paratethys (Figures 1 and 2). Investigations of nannoplankton and foraminifera of DSDP Leg 42A revealed major differences in the middle Miocene faunal assemblages between the Paratethys and the Mediterranean seas and raised questions which led to the following study. EARLY MIOCENE SEAWAYS Early and middle Oligocene faunal assemblages are more or less uniform throughout Europe. The beginning of faunal differentiation began in the late Oligocene in the northern and western Mediterranean and Paratethyan-faunal realms. The early Miocene of the Paratethys area (Eggenburgian/Sakaraulian and Ottnangian/Kozachurian) is characterized by uniform, widespread faunal renewal. The fauna includes a most distinctive and diverse molluscan fauna, which includes numerous "giant" taxa as a result of exlosive evolution and migration during that time (Steininger et al., 1975). This fauna indicates a connection existed with the Indo-Pacific Ocean and its deposition is generally concurrent with a worldwide transgressive phase, probably related to an accelerated spreading rate in the early Miocene. The seaway can easily be traced from the Persian Gulf and western Iran, including the Quom Basin, across Iraq and the Mesopotamian trough to eastern Turkey and across southern Russia (Crimea area) into the Paratethys. Moreover, it can be traced across the Mesopotamian Basin and northwest Syria into the

Middle Miocene Salinity Crisis and Paleogeography of the Paratethys (Middle and Eastern Europe)