1. INTRODUCTION Paratethys was the intercontinental bioprovince, which began to evolve in the Oligocene due to the counter- clockwise rotation of Africa that caused the closure of the Tethys Ocean. It extended from the western Mo- lasse Basin in Switzerland and the Rhone Basin in France towards Lake Aral in Asia. Paratethys is subdi- vided into Western Paratethys, Central Paratethys and Eastern Paratethys. The Central Paratethys extended from Bavaria to the Carpathian mountain chain (LAS- KAREV, 1924; SENE©, 1979; STEININGER & RÖ- GL, 1979, 1984; RÖGL & STEININGER, 1983, 1984; RÖGL, 1998, 1999) (Fi g. 1). The nature of the evolu- tion of Central Paratethys and the occurrences of an endemic fauna has necessitated the establishment of local Miocene stages (Fig. 2). In the geotectonical sense, the largest part of Central Paratethys is represented by the Pannonian Basin Sys- tem, formed due to continental collision and subduction of the European plate under the African (Apulian) plate (HORVÁTH & ROYDEN, 1981; ROYDEN, 1988; TARI et al., 1992; HORVÁTH, 1995; KOVÁ» et al., The South-Western Boundary of Central Paratethys Davor PAVELI∆ 1998). The Pannonian Basin System is surrounded by the Alps and Carpathian mountains, and by the Dinar- ides which existed as land between the Mediterranean Sea and Pannonian Basin System during its evolution. The southwestern part of the Pannonian Basin System consists of the North Croatian Basin and the Northern Bosnia region (PAVELI∆, 2001). The Dinarides represent a mountain complex, which formed during the Tertiary and Quaternary due to tec- tonic activity, which caused disintegration and uplift of the Mesozoic carbonate platform. In the Tertiary, com- pressive movements culminated with orogenesis of the Dinarides. Further neotectonic activity caused uplift and transpressive deformations of the older structure. These tectonics strongly controlled the formation of many small Neogene basins within the Dinarides which were characterized by fresh-water sedimentation and an endemic fauna. That tectonic activity has been strongest along the recent eastern Adriatic coast due to the conti- nental collision of the Adriatic microplate and the Dinarides. This collision caused the compression and uplift of blocks which is represented by a mountain chain known as the High Karst Belt, the highest peaks of which reach from 1400-1913 m (BAHUN, 1974; PAPE©, 1985; HERAK, 1986, 1991, 1999; ALJINO- VI∆ et al., 1987; BLA©KOVI∆, 1991, 1998, 1999; HE- RAK & TOMI∆, 1995; MARIN»I∆ et al., 1977; MA- TI»EC et al., 1997, 2001; PAMI∆ et al., 1998; DRA- GI»EVI∆ et al., 1999; KUK et al., 2000; DRAGI»E- VI∆, 2001). Several papers deal with the palinspastic reconstruc- tion of Central Paratethys, or some parts of it during it’s evolution (STEININGER & RÖGL, 1979, 1984; RÖ- GL & STEININGER, 1983, 1984; MARINESCU, 1992; K O V A » et al., 1998, 2001; RÖGL, 1998, 1999; MAGYAR et al., 1999; GULYÁS, 2000; PAVELI∆, 2001). In some of these articles the southwestern Cen- tral Paratethys boundary was constructed in the area of north Bosnia and central Croatia. However, these boundaries were not located in detail, and are, in part, incorrect due to a lack of data from this area, and a lan- guage problem. The locations of these boundaries also imply that the Neogene fresh-water basins within the Dinarides do not belong to Central Paratethys, neglect- ing the view of ANI∆ (1951-1953), who suggested that these basins might be a part of that realm during Sarma- tian time. The correlation of Neogene sediments and fauna of fresh-water basins within the Dinarides with Geologia Croatica 55/1 83 - 92 4 Figs. ZAGREB 2002 Key words: Neogene, Dinarides, Central Paratethys, Mediterranean. Institute of Geology, HR-10000 Zagreb, Sachsova 2, Croatia; e-mail: dpavelic@igi.hr Abstract Small Neogene basins within the Dinarides were never invaded by marine transgressions during their evolution. The fresh-water sedi- mentation, endemic fauna and their position between the Adriatic region and the Pannonian Basin System explain why these basins have not been considered as parts of the Mediterranean or Central Paratethys realm. The correlation of sediments and fauna of these fresh-water basins with the Pannonian Basin System and Adriatic region suggests that Dinaridic fresh-water basins may be considered as a part of the Central Paratethys. This consideration locates the southwestern boundary of Central Paratethys within the High Karst Belt. 84 Geologia Croatica 55/1 the North Croatian Basin and Northern Bosnia region, and with the Adriatic region, supports the suggestion that these fresh-water basins may be considered as a part of Central Paratethys, although there was no marine sedimentation. 2. THE NORTH CROATIAN BASIN AND NORTHERN BOSNIA REGION The evolution of the North Croatian Basin and North- ern Bosnia region, as a part of the marginal zone of the Pannonian Basin System was generated by continental rifting processes. The main depressions in this area rep- resent elongated half-grabens formed by tectonic subsi- dence along the listric faults and strike-slip faults (TARI & PAMI∆, 1998; LU»I∆ et al., 2001; PAVE- LI∆, 2001). Formation of the North Croatian Basin and Northern Bosnia region started in the Ottnangian, with fresh-water deposition. The first phase was character- ized by accumulation of coarse-grained breccias and conglomerates, with subordinate sandstones and silt- stones. Deposition took place in braided alluvial fans, which were strongly influenced by synsedimentary tec- tonics (PAVELI∆ & KOVA»I∆, 1999). In the central part of Mt. Papuk a salina-type lake developed (©∆AV- NI»AR et al., 1983). During the second sedimentation phase a hydrologi- cally open fresh-water lake was formed in this area (K O C H A N S K Y - D E V I D É, 1979; PAVELI∆, 2001; PAVELI∆ et al., 2001), in which silts and sands with sporadic layers of gravel were deposited, together with peats along the lake margins. The lake had an endemic fauna of molluscs and ostracods, such as C o n g e r i a f u c h s i, U n i o sp., and H e t e r o c y p r i s sp. (Fig. 3). Lacus- trine deposits contain remnants of mammalian species Prodeinotherium bavaricum , Gomphotherium angusti - d e n s and Brachypotherium brachypus (RADOV»I∆ et al., 1998). During Karpatian time lacustrine conditions were replaced by marine environments due to a minor marine transgression caused either by the opening of a Parate- thyan seaway to the Mediterranean as a consequence of the tectonic activity within the Dinarides (S T E I N I N- GER & RÖGL, 1979; HAMOR & SZENTGYÖRGYI, 1981; RÖGL & STEININGER, 1983, 1984; RÖGL, Fig. 1 Location of the Central Paratethys. 1 9 9 8), or eustatic sea level rise (KOVA» & H U D A »- K O V A, 1997; KOVA» et al., 2001). Deposition was characterized mainly by marls and silts with temporary input of coarse-grained siliciclastics into the basin, and sandy facies in the coastal environments (PAVELI∆ et al., 1998). The marine regime is indicated by foramini- feral and mollusc associations which are presented by Pappina bononiensis , Quinqueloculina triangularis , Quinqueloculina akneriana , Ammobaculites aggluti - n a n s, Triloculina scapha , Dorothia gibbosa , A m m o n i a b e c c a r i i , Elphidium macellum and others (Fig. 3). Dur- ing Ottnangian and Karpatian time volcanic activity gradually increased, from pyroclastics to trachyan- desites (shoshonites) (P A M I ∆ et al., 1992/1993; PA- VELI∆, 2001). Marine environments continued into the Badenian. The Early Badenian was characterized by a sea-lev- el rise well correlated with the global sea-level rise at the beginning of the Middle Miocene (RÖGL & STEI- NINGER, 1983; HAQ et al., 1987; STEININGER e t al., 1989; RÖGL, 1996, 1998; KOVA» & HUDA»KO- VA, 1997; PAVELI∆ et al., 1998). Coarse-grained sili - ciclastic material was transported into shallow marine environments, and also to the relatively deeper marine environments, where marls and gravelly calcarenites were deposited (PAVELI∆ et al., 1998; VELI∆ et al., 2000). Favourable ecological conditions resulted in expansion of shallow- and deep-water benthic and planktonic species, such as Amphistegina sp., Lenticuli - na cultrata , Cibicidoides ungerianus , Uvigerina pyg - m o i d e s, Globigerina praebulloides , G l o b i g e r i n o i d e s trilobus a n d Preaorbulina glomerosa (Fig. 3). Intense volcanism produced sequences a few hundred metres thick in some places. During the Late Badenian, the last Miocene marine transgression flooded this area. It was connected with the broad re-opening of the Indo-pacific seaway (RÖGL & STEININGER, 1983, 1984; ST E I N- INGER et al., 1988; RÖGL, 1996, 1998), and coincides with a temporary sea-level rise at 13.4 Ma (HAQ et al., 1987). Sedimentation was similar to that during the Early Badenian. The most important Late Badenian species are Bolivina dilatata , Pappina neudorfensis , Ammonia beccarii and Spirorutilus carinatus . Due to the beginning of the isolation of the basin during the Sarmatian, brackish-water environments developed, resulting in deposition of shallow water gravel, biocalcarenites and limestones, and general dominance of fine-grained deposits in the deeper parts of the basin. Typical Sarmatian foraminiferal species are Elphidium macelum, Elphidium josephinum, A n o m - alinoides badenensis and Porosononion granosum . Ervilia dissita dissita , Musculus sarmaticus a n d C a r d i - um vindobonense belong to the molluscan association. In the Early Pannonian the environment became “caspi-brackish”, locally even fresh, followed by expansion of endemic species of molluscs and ostra- cods, as a consequence of definite basin isolation (STE- ININGER et al., 1988). The Pannonian deposits consist of littoral lacustrine limestones, and deep water marls. The Pannonian fossil association contains Radix croati - ca , Congeria banatica , Clivunella sp. and Hemicytheria c r o a t i c a . In the Pontian a gradual shallowing took pla- ce, reflected by increased terrigenous material. The spe- cies are also endemic, including Paradacna okrugici , Paradacna abichi , Congeria croatica and C o n g e r i a rhomboidea. 3. DINARIDIC FRESH-WATER BASINS The Neogene basins in the Dinarides, i.e. in Bosnia and Herzegovina and in central and southern Croatia, repre- sent depressions generated by tectonics (Figs. 1 and 4). They started to form at the end of the Palaeogene and 85PaveliÊ: The South-Western Boundary of Central Paratethys Fig. 2 Chronostratigraphic correlation of the Mediterranean and Central Paratethys Miocene, and calcareous nannoplankton biozonation (after RÖGL, 1996, and BERGGREN et al., 1995). 86 Geologia Croatica 55/1 Fig. 3 Geological columns of the North Croatian Basin (Pannonian Basyn System), Sarajevo-Zenica Basin and Livno-Duvno Basin (Dinar- idic fresh-water basins), and Koraljka-I Well (Adriatic region). I 'i~~ i I n~~ft • I Q : I j I ~ j I : j ~ I ~ : ~ I! I ~ ~ ,Iii z lUi ! i 0:00 ~ I : ~ I I [). a ~ '. , I I)! DI:: I • 0(1: I: • • I I ~ [)<; 0() I :: : I o· ~ , +. i I ~ . • {f~ I' + . I I _!Q I' :_n I "'ll'III ~ _;r{I lilLTiI'lll iil l 1 87PaveliÊ: The South-Western Boundary of Central Paratethys continued to evolve through the Neogene. The time of onset and the end of evolution of different basins was unequal, as was subsidence which varied from a few hundred to a few thousand metres in the deepest depres- sions (PAPE©, 1985). These basins occur in many areas, with dimensions which range from a few kilome- tres up to 70 km long and 18 km wide, such as the Sara- jevo-Zenica Basin in central Bosnia (Fig. 4). Basins were temporarily connected during their evolution, and occupied much wider areas than at present (JURI©I∆- POL©AK & SLI©KOVI∆, 1988). However, the strong neotectonic activity generated by the continental colli- sion of the Adriatic microplate and the Dinarides caused uplifting of the Dinarides to the recent eleva- tions, erosion of the Neogene sediments, and reduction of the dimensions of fresh-water basins (PAPE©, 1985; ALJINOVI∆ et al., 1987; BLA©KOVI∆, 1991, 1998, 1999; MATI»EC et al., 1997, 2001; PAMI∆ et al., 1998; DRAGI»EVI∆ et al., 1999; KUK et al., 2000; DRAGI»EVI∆, 2001). Thicknesses of the Neogene deposits in fresh-water basins vary from a few hundred metres to 1900 m in the Livno-Duvno Basin and 2600 m in the Sarajevo-Zenica Basin (Fig. 4). Siliciclastics dominate but marls and Fig. 4 Approximate locations of the south-western shoreline of the Paratethyan Sea, and the south-western boundary of Central Paratethys. 88 Geologia Croatica 55/1 limestones also occur. Some sediments are coal-bearing (Fig. 3). Neogene basins in this area were of fresh-water. Some sediments are determined as alluvial, lacustrine, or marsh and swamp, but there have been no detailed sedimentological data. The main geological problem of these basins is the dating of sediments. Basins did not have any connec- tion with the sea during their evolution, and endemic species with no chronostratigraphic value developed. Therefore, the Neogene is subdivided on the basis of local mollusc and ostracod associations, superposition, lithostratigraphic correlation, flora, and occasional mammal occurrences (Fig. 3). However, these strati- graphic interpretations are almost highly speculative, sometimes very confusing, and partly incorrect, and are therefore of little use for detailed correlations with Cen- tral Paratethys and Mediterranean stages. Neogene sediments overlie the pre-Neogene base- ment or Oligocene deposits, and are characterised by frequent lateral and vertical variations, and different sedimentary thicknesses as a result of the independent local basin evolution. Columns for the Sarajevo-Zenica and Livno-Duvno Basin are shown in Fig. 3. The following general description of sediments and fossil associations is summarized from several works, without a critical stratigraphic approach (S O K L I ∆, 1957; »I»I∆ & MILOJEVI∆, 1977; PAPE©, 1975; ÆI- VANOVI∆ et al., 1975; MARIN»I∆ et al., 1977; JO- VANOVI∆ et al., 1978; KOCHANSKY-DEVIDÉ, 1976; KOCHANSKY-DEVIDÉ & SLI©KOVI∆, 1978; PAMI∆ et al., 1978; POL©AK et al., 1978; SOKA», 1980; JURI©I∆-POL©AK, 1984; RAI∆ et al., 1984; ÆAGAR-SAKA» & SAKA», 1984; JURI©I∆-POL- ©AK & SLI©KOVI∆, 1988; ©U©NJARA & SAKA», 1988; JURI©I∆-POL©AK et al., 1993; OLUJI∆, 1999). The oldest Neogene sediments are dated as the upper part of the Oligo-Miocene. Siliciclastics predomi- nate, the most frequent include conglomerates, sand- stones, marls and clays. Characaean limestones and coal beds occur sporadically. A mollusc association c o n t a i n s Helix rugulosa , Helix geniculata , L y m n a e a s o c i a l i s, Lymnaea dilatata , P l a n o r b i s sp. and P i s i d i u m sp. Lower Miocene sediments are more widespread than Oligo-Miocene ones. They consist of clays, lime- stones, marls, sandstones, conglomerates and coal inter- calations. Tuff is found in some basins. Dacite-andesite tuff beds in the Sinj Basin are interpreted as a conse- quence of volcanic activity in Bosnia (©U©NJARA & ©∆AVNI»AR, 1974) (Fig. 4). A fossil association is very rich in Lower Miocene sediments. Molluscs are represented by Congeria pernaeformis , Congeria jad - r o v i, Orygoceras corniculum , Lymnaea dilatata , L y m - naea socialis , Sphaerium sp., Unio sp., Helix sp., Bythi - n e l l a sp., Planorbis obtusus and Planorbis subcingula - t u s. Floral species include Carpolithes floveatus, G l y p - tostrobus europeus , C i n n a m o m u m sp. and C e r a t o p h y l - lum sinjanum. Mammalian species, such as D y n o t h e r i - um bavaricum, occur. The Middle Miocene sediments show a low degree of diagenesis. During the Middle Miocene marls, lime- stones, sandstones, clays and conglomerates were depo- sited. Coal beds occur in some places, pyroclastics too. The most frequent molluscs belong to the genus Conge - r i a : Congeria pernaeformis , Congeria jadrovi , C o n g e - ria dalmatica , Congeria drvarensis , Congeria bosni - a c a , Congeria bihacensis etc. Gastropods include O r y - goceras bifrons , Planorbis cornu , Clivunella katzeri, Fossarulus tricarinatus , Prososthenia schwartzi , M e l a - nopsis geniculata , Melanopsis inconstans, M e l a n o p s i s lanzae, Melanopsis euristoma, Melanopsis kispatici and Melanopsis pilari. »I»I∆ & MILOJEVI∆ (1977) men- tion mammals found in Bosnia and Herzegovina, such a s Mastodon angustidens, Mastodon longirostris , D y - notherium bavaricum and Rinoceras sansaniensis , but it is now clear that some of these species are of a differ- ent Neogene age. In the Sinj Basin (Fig. 4), M a s t o d o n a n g u s t i d e n s sp. and A c e r a t h e r i u m sp.aff. i n c i s i v u m were determined (OLUJI∆, 1999). The Upper Miocene and Pliocene deposits are char- acterized by marls, clays, siltstones, sandstones, con- glomerates, limestones and coal beds. A molluscan association consists of Congeria dalmatica , C o n g e r i a z o i s i, Orygoceras dentaliforme , Orygoceras cornucopi - a e, H y d r o b i a sp., V a l v a t a sp., L y m n a e a sp., P i s i d i u m o v u l u m, Melanopsis acanthica , Melanopsis defensa, Prososthenia tournoueri etc. Some ostracods have been found, such as Paralimnocythere rostrata , P o t a m o c y - p r i s sp. and C a n d o n a sp.. The youngest Pliocene to Pleistocene newly determined molluscan species are Odontohydrobia croatica and Limnidia likana ( J U R I- ©I∆-POL©AK et al., 1997). The Upper Miocene and Pliocene sediments are overlain by Quaternary deposits. 4. THE ADRIATIC REGION In a region of the Adriatic, as a part of the Mediter- ranean, marine deposition was almost continuous from the Paleogene into the Neogene, although transgressive contacts have been registered at some localities. Sedi- ments of Neogene age are almost of marine origin and the occurence of fresh-water sediments which include endemic species, such as on Pag Island (KOCHAN- SKY-DEVIDÉ & SLI©KOVI∆, 1978), are very rare. The unconformities between sediments observed in several places belong to different stages, and are conse- quences of emergence due to local tectonics (TURK, 1971; JENKO & BISTRI»I∆, 1978; KALAC & BAJ- RAKTAREVI∆, 1989; MILETI∆ et al., 1995). The emergence was particularly long-lasting during the Oligocene and Early Miocene, and resulted in the for- mation of a land corridor for mammalian migration from the Dinarides to Apulia (DE GIULI et al., 1987; J. RADOV»I∆, pers. comm.) 89PaveliÊ: The South-Western Boundary of Central Paratethys Generally, carbonates and fine-grained sediments prevail, and the thickness of the Neogene deposits reaches eight hundreds metres (D. MILETI∆, pers. comm.) which is much less than in the Dinarides, North Croatian Basin and Northern Bosnia region, suggesting minor tectonic controls (Fig. 3). The stratigraphy of the Neogene deposits in the Croatian part of the Adriatic region is based on foraminiferal associations (JENKO & BISTRI»I∆, 1978; KALAC & BAJRAKTAREVI∆, 1989; MILETI∆, 1994; MILETI∆ & BAJRAKTARE- VI∆, 1995; MILETI∆ et al., 1995). A geological col- umn of the Koraljka-I well, which was located in the central Adriatic, is presented in Figs. 3 and 4. Early Miocene sedimentation is characterized by a dominance of carbonates, i.e. limestones and marls (Fig. 3). A foraminiferal association consists of G l o b o - quadrina dehiscens , Globigerinoides trilobus , G o b - igerinoides primordius and Amphistegina lessonii. Sed- imentation was open marine. During the Middle Miocene marl sedimentation dominated, but limestones and sandy limestones were also deposited (Fig. 3). In a foraminiferal association Praeorbulina glomerosa , Orbulina suturalis , A n o m a l i - noides pompilioides, Lenticulina vortex, S p i r o p l e c t i n e l - la carinata , Globoquadrina langhiana , Orbulina uni - versa, Globorotalia praemenardii , Globorotalia mayeri and Globorotalia menardi prevail. This association sug- gests open marine deposition. In the Late Miocene, sedimentation was similar to that of the Middle Miocene. However, at the end of the Late Miocene evaporites were deposited in shallow lagoons. These deposits may be a result of a sea level fall due to the tectonic generated closure of the Atlan- tic-Mediterranean gateway. This event is known as the Messinian salinity crisis (RÖGL & STEININGER, 1983). From the foraminiferal association, G l o b i g e r i n a n e p e n t h e s, Lenticulina costata , Uvigerina rutila , E l p h i - dium crispum, Elphidium complanatum, G l o b i g e r i n o - ides extremus, Globorotalia conomiozea , G l o b i g e r i n o - ides bollii and Ammonia beccarii dominate. Marls, siltstones and sandstones characterize Plioce- ne sedimentation. Conglomerates are very rare and only occur sporadically. Deposition was open marine. The cause of the sea level rise in the Pliocene was a re- opening of the Atlantic-Mediterranean gateway in the beginning of the Pliocene (RÖGL & STEININGER, 1983). The most important Pliocene foraminiferal spe- cies are Globorotalia margaritae , Uvigerina rutila , Globorotalia puncticulata , Anomalina helicina, G l o b o - rotalia aemiliana , Globorotalia crassaformis , Globoro - talia inflata and Epistomina elegans. 5. DISCUSSION AND CONCLUSION The faunal characteristics of species which occur in sediments in the Neogene fresh-water basins within the Dinarides is almost endemic and can not be correlated with a marine fauna in the Adriatic region. However, they show many similarities to endemic species found in deposits of the North Croatian Basin and Northern Bosnia region, i.e. Central Paratethys. The most fre- quent endemic species which occur both in the North Croatian Basin and Northern Bosnia region, belong to the molluscan genera Congeria , Unio, Lymnaea, Pisidi - u m, M e l a n o p s i s, P l a n o r b i s , Valvata and Clivunella , and the ostracod genus Candona . Sedimentation in the North Croatian Basin and Northern Bosnia region, and in the Dinaridic fresh- water basins also show similarities. Frequent changes of different types of sediments, including siliciclastics, coarse-grained deposits, coal-bearing beds, pyroclas- tics, emersions as well as mammalian occurrences are characteristic of both areas. The thickness of sediments in the Dinaridic fresh-water basins is also more compa- rable to the North Croatian Basin and Northern Bosnia region than to the Adriatic region. The strong tectonic control on sedimentation is also similar. Similarities between the North Croatian Basin and Northern Bosnia region with Dinaridic Neogene basins suggest that these small basins show many faunal and depositional characteristics of Central Paratethys, and may be considered as a part of this realm. This means that the south-western boundary of the Central Parate- thys may be constructed within the High Karst Belt, the mountain chain which separated the Mediterranean from Central Paratethys (Fig. 4), similar to ANI∆’s (1951-1953) idea. In this sense, the boundary located in the northern Bosnia and central Croatia represents only the south-western shoreline of the sea or large lake which occupied the largest part of the Central Paratethys (Fig. 4). Acknowledgements The review of the manuscript by Z. BAJRAKTARE- VI∆, I. DRAGI»EVI∆, K. ©IKI∆, D. VRSALJKO, M. M I K N I ∆ and J. BULI∆ is gratefully acknowledged. I am indebted to R. AVANI∆, D. MILETI∆ and I. SLI©- K O V I ∆ for providing helpful suggestions. This paper profited from journal reviewers F.F. S T E I N I N G E R (Frankfurt), Z. JURI©I∆-POL©AK (Zagreb) and J. RA- DOV»I∆ (Zagreb). 6. REFERENCES ALJINOVI∆, B., PRELOGOVI∆, E. & SKOKO, D. (1987): Novi podaci o dubinskoj geoloπkoj grai i seizmotekton- ski aktivnim zonama u Jugoslaviji.- Geol. vjesnik, 40, 255-263. ANI∆, D. (1951-1953): Starost naslaga sa smeim ugljenom u Bosni, Hercegovini i Dalmaciji.- Geol. vjesnik, 5-7, 73- 110. BAHUN, S. 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