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Home , Abtenau, Adriatic Plate, Angerberg, Diekholzen, Filakovo, Fur Formation

Palaeogene and Neogene

MICHAEL W RASSER, MATHIAS HARZHAUSER (co-ordinators), OLGA Y. ANISTRATENKO, VITALIY V. ANISTRATENKO, DAVIDE BASSI, MIRKO BELAK, JEAN-PIERRE BERGER, GIANLUCA BIANCHINI, SAFET CICIC, VLASTA COSOVIC, NELA DOLA.KOVA., KATICA DROBNE, SORIN FILIPESCU, KARL GÜRS, SA.RKA HLADILOVA., HAZIM HRVATOVIC, BOGOMIR JELEN, _ JACEK ROBERT KASINSKI, MICHAL KOVA.C, POLONA KRALJ, TIHOMIR MARJANAC, EMÖ MA.RTON, PAOLO MIETTO, ALAN MORO, ANDRA.S NAGYMAROSY, JAMES H. NEBELSICK, SLAVOMIR NEHYBA, BOJAN OGORELEC, NESTOR OSZCZYPKO, DAVOR PAVELIC,, RAJKO PAVLOVEC, JERNEJ PAVSIC, PAVLA PETROVA, MARCIN PIWOCKI, MARIJAN POLJAK, NEVIO PUGLIESE, REJHANA REDZEPOVIC, HELENA RIFELJ, REINHARD ROETZEL, DRAGOMIR SKABERNE, VUBOMIR SLIVA, GERDA STANDKE, GIORGIO TUNIS, DIONYZ VASS, MICHAEL WAGREICH & FRANK WESSELINGH

Over the last 65 Ma, our world assumed its modem shape. This Miocene to Plioeene sueeessor Lake Pannon. At its maximum timespan is divided into the Palaeogene Period, lasting from 65 extent, the extended from the Rhöne Basin in Franee to 23 Ma and the Neogene, which extends up to the present day towards Inner Asia. Subsequently, it was partitioned into a (see Gradstein & Ogg (2004) and Gregory et al. (2005) for smaller western part eonsisting of the Western and the Central diseussion about the Quaternary). Paratethys and the larger Eastern Paratethys. The Western Throughout the Cenozoie Era, Afriea was moving towards Paratethys eomprises the Rhöne Basin and the Alpine Foreland Eurasia in a northward direetion and with a eountercloekwise Basin of Switzerland, Bavaria and . The Central Para- rotation. Numerous mieroplates in the Mediterranean area were tethys extends from the in the west to the eompressed, gradually fusing, and Eurasiaunderwent a shift from Carpathian Foreland in the east where it abuts the area of the a marine arehipelago to eontinental environments, related to the Eastem Paratethys. Eurasian eeosystems and landseapes were rising Alpine mountain ehains (Figs 17.1 & 17.2). Around the impaeted by a eomplex pattern of ehanging seaways and land Eoeene-Oligoeene boundary, Afriea's movement and subduetion bridges between the Paratethys, the and the Mediterra- beneath the European plate led to the final disintegration of the nean as well as the western Indo-Paeifie (e.g. Rögl 1998; Popov aneient Tethys Oeean. The Indo-Paeifie Oeean eame into ex- et al. 2004). This geodynamieally eontrolled biogeographie istenee in the east while various reliet marine basins remained in differentiation neeessitates the establishment of different ehron- the west. In addition to the emerging early , ostratigraphie/geoehronologic seales. another reliet of the closure of the Tethys was the vast Eurasian The geodynamie ehanges in landscapes and environments were Paratethys Sea. further amplified by drastie climate ehanges during the Cenozoie. The Oligoeene and Mioeene deposits of are The warm Cretaeeous elimate eontinued into the early Palaeo- largely related to the North Sea in the north, the Mediterranean gene with a distinet optimum near the Palaeoeene-Eoeene Sea in the south and the intermediate Paratethys Sea and its late boundary (Palaeoeene-Eoeene Thermal Maximum) and the 1032 PALAEOGENE AND NEOGENE 1033

,'~'~.-._."- included a single result from stable Central Europe, or more recentty by Besse & Courtitlot (2002, 2003) who used five. (all representing the 16.5-34 Ma time interval). Thus, the Cenozoie apparent polar wander eurve (APWC), which serves to represent .•.. the displacements of stable Europe with respect to the present- ; day north and its shift in latitude, is a synthetic one computed by using palaeomagnetie data from all eontinents and transferred to stable Europe through a plate tectonic reconstruction model (e.g. Besse & Courtitlot 2002). Palaeomagnetie directions eomputed from the synthetic APWC suggest that stable Europe travelIed a few hundred kilometres northward during the Cenozoic, but did not change its orientation (within the limit of the resolution of palaeomagnetic observations, whieh in this case is c. ::i:5°).This implies that the expeeted stable European declinations are more or less aligned with the present meridians. The actually measured declinations at several points in stable Europe (e.g. France, , Poland, Czech Republic; Global Palaeomagnetic Database 2005) deviate more from the present meridian than the coeval deelination computed rrom the synthetic APWC. Nonetheless, these devia- tions cannot be interpreted in terms of tectonics, since the Fig.17.2. Maiß physiographie and geological units ofCentral Europe. studied rocks, without exeeption, are igneous rocks, where Grey line marks the horder between the European Plale and the Alpine- securar variation of the Earth's magnetic field and poor control Late (Priabonian)35 Ma Carpathian orogenie system. Abbreviations correspond to official country on loeal tectonics can cause bias from the direction of the code plates. geomagnetic field. The stable European pattern of Cenozoic declinations breaks 500 km Transition indieated by the eooling of surfaee waters and the down as soon as we enter the North Alpine Foreland Basin at the expansion of the East Antarctic ieesheet (Shevenell et al. 2004). southern margin of stable Europe and south of this. The pattern A final trend reversal during the Early Pliocene is reflected by a here suggests large-scale movements during the Cenozoie Era, gentle warming until 3.2 Ma (Zachos et al. 2001) when the onset aceompanied by counterclockwise (CCW) rotations of variable of permanent Arctie glaciation heralded the Pleistoeene iee ages angles and timings; observations for dominant clockwise rota- (see Litt et al. 2008). tions are known only from the Apuseni Mountains (Romania) o The Cenozoie history of Central Europe is ehronieled in a and from the area between the Periadriatie and faults. dense pattern of Palaeogene and Neogene basins. In addition to Sedi~ents Iying directly on the stable European margin exhibit the more stable North Sea Basin, the majority of these basins moderate CCW rotation (Scholger & Stingl 2004; Mi\rton et al. were strongly influenced by the Alpine eompressive tectonics 2003a). The mean angle of rotation is the same in every segment which caused a general uplift of Europe during the Cenozoic (Fig. 17.3), which is remarkable, since the age of the studied (see Froitzheim et al. 2008; Reicherter et al. 2008). The marginal sediments varies between 20 and 7 Ma. The termination of the position of the seas eovering the area and the eonsiderable rotations is not eonstrained in any of the segments. Therefore, synsedimentary geodynamie eontrol resulted in ineomplete strati- there are alternative solutions to explain these observations. One graphie sequences with frequent uneonformities, erosional sur- is that thc rotations were simultaneous between longitudes of faces and depositional gaps. 12°E and 23°E. In this case, the Bohemian Massif (which is This chapter deals with the and Neogene ("Ter- considered to be part of stable Europe) must have been involved tiary") geological development of Central Europe and its in rotation. The other possibility is that the rotations are not adjaeent areas. It is struetured aeeording to the maiIl..geological eoeval and the sediments were detaehed from the stable regions relevant for the Cenozoie: (1) The European Plate; European basement. In either ease, the observations would ""i"i"i-~~I~ilerr~:n$~~m",,>,,",,~.," (2) the Alps and Alpine Foredeep; (3) the Carpathians, their require dramatic modifieation of existing tectonie models. foredeep and the Pannonian Basins System; and (4) the Southern As we move into thc mobile part of Europe, the palaeo- MiddleMiocene(Langhian) 15 Ma Latesl Miocene(Messinian) 6 Ma Alps and Dinarides. Eaeh subchapter is arranged from west to magnetie picture beeomes fairly eomplicated. During the Palaeo- east, and north to south. gene, there is no palaeomagnetic evidence for mobility, apart from a general northward travel for all tectonic units (Märton Land I;ÜHtbl Deep shelf f1~~1Anhydrite, gypsum 200 I). Rotations begin in the Miocene. Some of these can be D Palaeomagnelism and palaeogeography (KM.) related to tectonie escape from thc East Alpine realm, others to Deep shelfal depression, Freshwater lake, I?'I 11II contlnental slope and ~ marshes Central Europe is eomposed of two tectonically contrasting subduetion pull in the Carpathians and the rest to the motion of Shallow shelf basin bottom regions: a northem Variscian region and a southem Alpine region the Adriatic micropiate (Adria). ~ (Figs 17.2 & 17.3). The former is called stable Europe in the Notable cases with rotations related to escape tectonics are palaeomagnetic literature, sinee the generally accepted view is known rrom the Eastem Alps and from the Periadrialic-Sava Fig. 1'.". Palaeogene- Neogene palaeogeography of Cenlral Europe (after Popov el al. 2004). that Europe, north of the Alpine rront, behaved as a rigid plate system (Fig. 17.3B, areas 10 and 11). In the first case, e. during the Cenozoie Era. However, the number of palaeomag- 30° of the CCW rotation observed in the sediments of the netic results supporting this view is surprisingly few and most of Miocene intramontane basins (Fig. 17.3B, area 10) are related to Early Eocene (Early Eocene Climate Optimum). A gradual 2003). A renewed warming trend that began during the Late them were acquired hefore 1980. The scarcity of good data is lateral extrusion (Marton et al. 2000a); in Ihe second (Fig. decrease in temperature during the later Eocene culminated in Oligocene continued into the Middle Miocene with a elimax at especially notable for stable Central Europe. The situation is best 17.3B, area 11), the non-uniform, but dominantly clockwise the formation of the first icesheets in Antarctica around the the Mid-Miocene Climatic Optimum. The turning point at around characterized by data sets used for calculating stable European rotations are attributed to right-Iateral strike-slip movements Eocene-Oligocene boundary (Zachos et al. 2001; Prothero et al. 14.2 Ma led to the onset of the Middle Miocene Climate Cenozoic palaeomagnetic 'poles by Van der Voo (1993) who (Fodor et al. 1998). .';l 1034 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1035

12' N (slab) pull accounts for most of tbe rotations (Fig. 17.3B, area 13), up to 90' in the counterclockwise and in observed for the Carpathians aud far the . These the clockwise sense, respectively. Middle and Late Miocene rotations occurred duri'.'g 18.5-17.5 Ma and 16-14.5 Ma (Ma- rocks from the same areas are characterized by moderate A gura unit of tbe Outer Western Carpathians (Marton el al. rotations (c. 25-40'). 2000c); Central West Carpathian Flyscb basins (Mmon er al. Age control on the tennination of the youngest rotations is 1999a); North Hungarian-South Siovakian Palaeogene basin lacking, except for the Nortb Hungarian-South Siovakian 1~2 (Marton & Mmon 1996; Marton e/ al. 1996; Marton & Pecskay Palaeogene basin (14.5 Ma) and for the Apusern Mountains 'jffJ>. 1998); Transdanubian Range (Mmon & Fodor 2003», c10se to (12 Ma). Thus, tbe possibility of large-scale neotectonic move- ••• + ••• the Palaeogene-Neogene boundluy (e.g. Apuseni Mountains; ments remains to be explored, especially in the southernmost part Panaiotu 1998) and at 14-12 Ma (o.g. East Siovak Basin (Marton ofEurope. e/ al. 2000b) and Apuseni Mountains; (Panaiotu 1998)). The 48' resulting rotations are CCW, except in the Apuseni Mountains. Tbe European Piste: overview (M, W.R.) As sooo as subductien terminated in the Western Carpathians, at c. 14 Ma, a push from Adria and, subsequently, rotation of The European Plate represented tbe so-called stable European 28' 12' 14' 16' 26' 18' 24' 52' Adria witb respect to Africa (Mmon e/ al. 2003b) became the continent during tbe Cenozoic northward drift of Africa. It dominant driving force for displacements in the Alpine realm. A comprises a large epicontinental sedimentation area extending series of palaeomagnetic observations. from tbe intramontane from NW Europe towards Ukraine (Fig. 17.4). During most of N B basins of the (Märton el al. 2000a), from the Mura the Cenozoic it was separated from the Alpine-Carpathian chain •..~~~~ depression (Marton el al. 2002a) and from Northern Croatia by the Alpine-Carpathian Foreland Basin - often referred to as '" ~~\\~., 50' (Marton e/ al. 2002b) indicate that c. 25' of CCW rotation the Molasse Zone or - aud its precursors as a occurred in the circum-Adriatic region, elose to tbe Miocene- part of the Palaeogene Tethys, or Oligocene-Miocene Paratetbys. Pliocene boundary (Marton 2005). Moderate CCW rotations Tbe North Sea Basin (NSB) is a main element of the European observed at the eastern margin of the Eastern Alps and in tbe Plate. It comprises a belt of Cenozoic deposits in the northem bordering basins (Styrian and Vienna basins; Scholger & Stingl part of Central Europe, extending from to northern 48' 2003, 2004; Scholger el al. 2003) and tbe youngest rotation of Poland. The Polish Lowlands form its eastward continuation and tbe Transdanubian Range (Märton & Fodor 2003) were probably served as an occasional connection between the NSB and the also induced by tbe rotation of Adria. Eastern Paratethys. Furtber eastward lies the Volbyno-Podolian Rotations at1ecting the same tectonic unit are of a cumulative Plate forming Ibe SW margin of the East European (= Russian) nature. Repeated rotations in the same sense cao cause large Platform. Towards the south, the NSB is bordered by the Belgian declination deviation from the present north. The largest declina- and German low mountain ranges as weIl as by the Bohemian tion deviations in the subject area were measured on Lower Massif. Miocene and Palaeogene rocks in the North Hungarian-South The Upper Rhine Graben represents an approximately Siovakian Palaeogene basin (Fig. 17.3B, area 5), in the Transda- 1100 km long structural element between tbe shores of Ibe Nortb nubian Range (Fig. 17.3B, area 8) and in tbe Apuseni Mountains Sea and the western Mediterranean. It formed a complex N 44'

A1~n~'a8 :

10 : O:ztyn 15+16 . : , • • • + ••• .. \ Bialystok. 1

0-Ei ~ll. i~"-/-£'~ ", cO ., m"tli \ &&. ~~e ci Fig. 17.3. Palaeomagnetics. (A) Alpine and Carpathian Foredeep. Age of sediments of the four numbered segments from west to east are: 27.5-17.2 Ma, ~::3r::::: 17.2-16.4 Ma, 16.4-13.0 Ma, 13.0-10.0 Ma (for Paratethyan geologieal stages refcr to RögI1996). Tbe stereonet (right side) shows the mean .r'~;E palaeomagnetic directions (declination and inclination) for the segments. The size of the dots eorresponds to the size of the confidence circle for eaeh &I~ palaeomagnetie direetion. (8) Eastern Alps - Carpathians - Pannonian Basin. Numbered teetouie units are cbaracterized by regionally coberent rotations, whieh are due to teetonie escape or subduction poil. Rotations conneeted to teetonie escape are the first-phase Mioeene rotations in area 10 (intramontane basins of the Eastern Alps) and the rotations in area 11 (Periadriatie-Sava fault system). Rotations eonnected to subduction pull are those observed for areas 5 (North Hungarian-South Siovakian Paleogene basin), 6 (Central West Carpathian Paleogene Basin), 7 (Magura unit of the Duter Western Carpathians), 8 (Transdanubian Range), 12 (East Siovak basin), 13 (Apuseni Mountains). The stereonet shows the angle ofthe total rotation and that of the younger rotation for area 5, and the palaeomagnetie direction (declination and inclination) for areas 6 and 7. (C) Eastem Alps, Western Pannonian Basin. Rotations triggered by rotating Adria are observed for areas 8, 9 (border zone ofthe Eastem Alps and tbe Pannonian Basin), 10, 14 (Mura-Zala Dijon depression), 15 (Medvednica-Hrvatsko Zagorje), 16 (Slavonian inselbergs). The stereonet on the right side compares the palaeomagnetic direction • characterizing the post-Eocene rotation of Adria with those reflecting the youngest rotation of the above listed areas.

Fig.17.4. Main Palaeogene-Neogene sedimentary basins ofthe European Plate. 1036 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1037

Cenozoic rift system with sedimentation commencing during the Sedimentary a'nd stratigraphie development Middle Eocene. The Palaeogene development of the NSB can be divided into live During the and Eocene, the units formed phases (Figs 17.5, 17.6 & 17.7): Ibe Early-Middle Palaeocene . '" :ß ,; 10"I j - I'! i 1l>E C> the southem margin of tbe European Plate, Le. the northern was a eontinuation of the tropical settings of the , as Bolboforma .~~i ~~~ .2 al il 1l ~ i ~~~ .. = "'1- 'e: ~.@ i tl.8, IL ~~I '2 tQ "- . ~~I ia .2 j'l (ä-q) margin of the Telbys Sea. Towards the south, the Helvelic units witnessed by widespread carbonate platform deposits in the biostratigraphy ~~ii ~ 0 • I/)Cll • ' c: E 'i ~.~i 'E.~U: -ieE pass into .the Ultrahelvetic Unit and Ibe Rhenodanubian (Penni- £ I'j' i~i~ 15 '5 .; ~!~f c:lD c: ~ c: entire NSB. It was also a major regressive phase. During the 'E: ~ I s....,.~_ '" I'!' CD ro ": ::;;",'1 .2 '::tt,- Q) :l 2 Q. , • ::;;~ ä" 0" " nie) Flysch Zone. In late Palaeogene times, however, Ibe Helvetic ••••••• lIioc1l ~ !j O:.gf oE I ~~ii ~~H '2: • 'lC!Jo Early-Middle Palaeocene, carbonates were partly deposited in UJ ltj ä I:> units are also considered by several authors to have constituted a very shallow water as the Houthem, Ciply and Mons formations transition to Ultrahelvetic and Penninie deep~marine c1astic NS818 of Belgium. Tbe Hückelhoven Formation of the Lower Rhine " •••• 1<1

I~ ~ 1038 M. w. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE ~ ~ • 2 I, rtÄ ~ -l! ~ ! ~ >~ ~ '~ ~ ~/;: i il , J JtI -1 ' '. /I • h i / ! ~ ..- ~ 'J~j -- (!J E ~ 1 !11 ~ w~

.!: "a ~ S~ ;ijj i $CIl o~ Im .~~ ~E ~m cll€~ l.,'j1i i~ ~ ! m c'" :2 ~Ij Cl:: '<..( ! /;: //: j c::::J Cratonic areas _ Deeper marine //: I~'""I Mainly continental _ Deep marine (turbiditic) u~ 1~~;"c<1Deltaic, shallow-marine ~ Basalts c ~ ~~ f,.,.",,~cl Shallow marine (shales) "li'" • l ~ Fault zones i " ~ Jj'JJ j [l~ Fig. 17.7. Palaeogeography ofthe North Sea Basin: (A) Late Palaeocene; (D) Early Chattian; (C) Late Middle Miocene-Early Late Serravallian; (D) Early Messinian. Abbreviations: an, Antwerp Member (Mbr); ba, Bashek Formation (Fm); bit Biemenhorst Fm; br. Brejning Fm; co, Cottbus Fm; de, Delden Mbr; UOnBWJO:::l ua6uoQ il di, Diekholzen Fm; da, Doberg Fm; ei, Eibergen Mbr; fu, Fur Fm; he, Helle Fm; ho, Hodde Fm; la, Landen Fm; lü, Lübtheen Fm; me, Meuro Fm; ne, ,""u.:0 • Neureith Fm; od, Oldesloe Fm; og, Oberer Glimmerton; 01, Olst Fm; pr, Pritzier Fm; sö, Söllingen Fm; sü. SülsdorfFm; ue. Uedem Fm; ve, Veldhoven Fm; ~: Ili J vi, Ville Fm; vo, Voorth Fm; wa, Waseberg Fm. Redrawn from the palaeogeographic Ziegler maps, mo , 11 j li I! * ~VA' ~ ;jl Ni -• many regional formation names. In Gennany and Denmark the f ~ i ] During the EarIy Eocene, paralic conditions prevailed aJong ..i overlying Early Eocene clays (Rasnaes Formation upper part, 1, the SE and southem basin margins (e.g. Saxony, Sachsen-Anhalt Fehmam Formation) are intercalated by brown to reddish clays ;1,1 l and HalUlover area). In this environment, lignite seams inter- -f, S66~'1')8 UlU68J-a ~ with a rich microfauna (Fehmam and Lillebaelt formations). "fU01'i' finger with marine clays. Clays from tbe HalUlover area have UOZfJOIlOUOJlI30IQ 1111 I :Ii ~i f, Water stratification. with reduced salinity in the surface layers, is 115SOJOUU'U"I~ l1i IIWllI1~111 o been radiometrically dated by Ahrendt cl al. (1995) and range inferred for the dark grey c1ay intervals deposited in Denmark ,;I from 52.8 Ma to 46.0 Ma. Dinoflagellate cysts indicate zones ljJRW&Q (Schmitz cl al. 1996). During deposition of reddish clays, water ,t;UllWJ80 i ~ 3 D5b, D6b, D7a, D8nb and D9na, thus comprising nannoplankton 586el8 leuol8e~ ~ ~ u circulation was restored and a cOIUlectionto the Atlantic, via the lmITr i zones NP10 to NP13/early NP14. The youngest unit (Emmerstedt south of the UK, has been proposed by Bonde (1979). l Greensand) represents a substantial marine transgression dividing wn,.' ••.• n 1'1=11 Water depths during the Early Eocene wcre bathyal in the ,e81lJ1l leuol68l1 J ) ! i ~ tbe lower and the upper seam complexes of this lignite distriet. t • i basin centre and outer neritic towards the .south. Dill et al. " ~ ~ In the Lower Rhine area, marine conditions predominated during t (1996) demonstrated shallower environments in the area of the Early Eocene. However, the Antweiler Formation indicates ~ ~ ~ ~ ~ (Germany). However, their interpretation of the ~I~~ ~ ~ ~ ~ paralic environments in the south of the region. ~I~ ~ Late Palaeocene to Early Eocene sandy to clayey deposits, as 050lS I~~~ 5 ~ The climate of the Early Eocene in the NSB was subtropical ~ ~ ~ ~ ~ tidal f1ats and marshes deposited in an estuary (Dill cl al. 1996), I~ '1 to tropical (Krutzsch cl al. 1992). Palm trees and mangroves I z is not followed here. , 'dn [ .'1 tl3ddn '-310alrl I tl3MOl I ~3ddn [ tl3Moi ltl3ddn 310dWi tl3MOl 1 l::i3ddn r tl3Moi bordered the sea which was inhabited by tropica! faunas. S8!J9S l'Oand 3N300lVol 3N3:JO£lllO The development of Belgium is one of the classie 3N3:J03 3N3:J031Vd • Hooyberghs el al. (2002) postulated a climate optimum at the ~ models of sequence stratigraphy (Vandenberghe cl al. 1998). The WBlS,(S 3N3903N 3 N 3 9 0 3 1 ~ d ~ end of the Ypresian Iinked to the invasion of a southern fauna Ieper Clay Formation reveals the strong cyclicity of outer neritic into the basin. ~ sedimentation, while in Late Ypresian time middle to inner 0'3 :> o z o N 3 :> ,,; The Middle to Late Eocene witnessed a major sea-level fall neritie sands and days indicate shallowing of the sedimentation ~ and strong sea-Ievel oscillations. A subtropical c1imate with !lV1l1J1~ area (e.g. Egemcappel clay, Egem sands, Merelbeke and Pittem ~ ~ ~ ~ g g rainforest vegetation (Mai 1995) and carbonate sedimentation in ~ clay). the shallower marine basin parts has been deduced from . 1040 M. W RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1041 Lignite formation in the south of the basin (Leipzig-Bitterfeld- in vast amounts of sediment from the NE and east. Greater parts The Thule landbridge drowned during the Late Oligoeene and Halle distriet) led to the development of eeonomieally important of the Fennoscandinavian Shield were lowlands and low moun- at a time of low sea level around the Early-Middle Miocene a permanent connection to the North Atlantic was established lagerstätten. tains. boundary, a large braekish lake developed in the northem (Wold 1995). There is strong faunal evidenee for a direet In the NE of the German part of the basin, a sheif edge During the Chattian transgression, marine conditions were German Hamburg Trough (Hinseh 1988) represented by about eonneetion to the Atlantie in the SW for the entire Early 100 m of the Hamburg Clay. developed at the Early-Middle Eoeene transition (Heiligenhafen restored in large parts of the NSB. The NE part of Denmark and Mioeene to early Middle Mineene (Figs 17.1 & 17.7) (Janssen Formation, dated NP14; Martini 1991). The marked the Lower Rhine were slowly covered by river systems This lake was replaeed by the sea at the beginning of the 200 I; Janssen & Gürs 2002) and for the late Late Plioeene contents (radiolaria and sponge spieules) of the slope elays and and the eoastline retreated inwards (Dybkjaer 2004a). Northem Middle Mioeene. Shortly afterwards an easterly derived lIuvial (Marquet 2004). The Dover Strait opened at 4 Ma (Van Vliet- sills indieate upwelling ('Unter-Eozän 4'). The outer neritie parts of eastern Gennany were marine influenced throughout the system was onee more established (Upper Lignite Sands). Lanoe el al. 2002). A marine connection to the northern sediments are replaced to the south and cast by inner neritic, entire Late Oligoeene (Lotseh 1981; Standke 200 I, 2008a). In CoevaUy, the Moorken Seam developed in the Lower Rhine Paratethys eannot be entirely excluded for the late Middle partly ealeareous, glaueonite sands and sills (Glinde Formation, the SW a semicontinuous connection to the Atlantic developed Embayment (Zagwijn & Hager 1987). In the Lusatian Lignite Miocene as there are strong similarities in plankton successions upper part of Nedlitz Formation, Emmerstedt Formation). as shown by faunal evidenee (R. Janssen 1979). Other pathways, District the paralic and shallow-marine Brieske Formation was (pteropods and bolboforms) with those of the Carpathian fore- During the successive Middle Eocene transgressions the bath- such as the northern one around Scotland, have been discussed as deposited (Standke et a/. 2005; Standke 2006). Tbis transgression deep of the Central Paratethys (Gürs & Janssen 2002; Janssen & ya} Sevind marls were deposited aver a much broader area than the only eonneetion (Gripp 1958) but single tropieal molluses is known as the 'Hemmoor transgression' (Anderson 1964) since Zorn 1993). Fennoseandinavian uplift in the Oligoeene narrowed the Lillebaelt clays and neritie sedimentation shifted to the east, such as Morum, Perrona and Mitrolumna raulini septentriona/is the Hoerstgen Beds of northem Westphalia (upper Hemmoorian the basin from the north. Tbe centre of the shield experieneed where carbonate oe non-earbonate silts to fine sandstones of the lanssen 1979 require a southern connection. the latter showing age) diseonformably overlie Oligoeene strata. The Miste Beds some 3000 m of uplift (Overeem 2002) and beeame a' major Conow, Semo and Annenberg formations mark the shelf edge. an affinity to the Chattian of the . A warm and the Breda Formation in the Peel region (the Nethertands) sediment source for the NSB. Uplift of the Erzgebirge and the Tbese formations typieally have an age of late NPI5 to NPI6 climate led to the invasion of a nearly subtropical marine fauna. show the same transgressive history. In northern - BeIgium the Lusatia Block (Brause 1990), as weU as enlargement of eateh- (Köthe 1988). Deposition of the Sßvind marls eontinued with It is preserved in the Voort Sands of northem Belgium, the Antwerp and Zondershot sands diseonformably rest on older ment areas following the retreat of Paratethys in Central Europe, deereasing carbonate eontent until the Late Eoeene (NPI9/20). A Grafenberg Sands of the Lower Rhine Embayment, the Kassel strata. The first eould be dated as NN4 (Steurbaut & Verbeek led to a more marked fluvial influenee from the SE !Tom Late decrease in carbonate conten!, as weil as a coarsening-upward Sands (showing a strong ingression into the Hessian Depression 1988) and DN4 (Louwye et a/. 2000a). The geometry of the Miocene times. Another main sediment source was the enlarged trend, ean also be deteeted in the Upper Semo, Gehlberg and in the early Late Oligoeene) and the famous Stemberg erratie prograding tower to middle Miocene sediment bodies indicates Rhine eatehment in the south (Zagwijn & Hager 1987; Schäfer et water depths of more than 400 m in the eentral North Sea. Lower Schönewalde formations. Thus, a more oe less continuous boulders of Meeklenburg (Bülow & Müller 2004) and Glanko- a/. 2004). Uplift of the Rhenish Massif aeeeierated in the shallowing- upward trend ean be seen from Middle to Late nitsand in the Lusatia area (Standke 2006). Late Oligoeene During the early Middle to middle Late Mioeene a major PliQ~ene. Eocene times. During the Late Eocene, submarine erosion look sediments in northern Belgium are restricted to the Roennond transgression restored marine conditions in the NSB. This major The bathyal water depths in the basin centre prevailed until the pIaee aeross vast areas of the eastem NSB. Only in the Kysing I Graben and a smaH portion of the Central Graben area. Mioeene transgression (Reinbek transgression; Anderson 1964) Early Plioeene. Subsequently the basin was mainly filled with borehole (Denmark) is a more or less continuous section across Deep water conditions prevailed in the basin eentre. In the began at the NN4-NN5 boundary (SpiegIer 2002). In Denmark eroded clasties !Tomthe uplifting hinterland. the Eoeene-Oligoeene boundary known (Heilmann-Clausen et Late Chattian a coast with lagoons and barrier islands developed the deeper marine Hodde Clay (Rasmussen 1966) overlies the a/.2001). in middle Jutland and this was related to the Ringkebing-Fyn fluviatile Oddemp Formation and extends to the NE beyond the Palaeomagnetism The Early Lutetian Bmssel Sands of Brabant (Belgium) are High (Dybkjaer 2004a, b). Ringkllbing-Fyn High. To the east the predominantly marine Palaeomagnetic resuhs from the area have been presented by marine ineised valley fills showing a major hiatus with the Meuro Formation was deposited in Lusatia (Standke el a/. 2005). Kuhlmann (2004) for the Plineene of the central North Sea. To the south the transgression extended into the northem German underlying Ypresian clays (Vandenberghe et a/. 1998). Many Significant stratigraphie boundaries sand units disconformably overlie one another as a result of the low mountain range (Hinseh et a/. 1978). The maximum 1I00ding The famous Stevns Klint site in the eastern part of Denmark is Sedimentary and stratigraphie development of this transgression occurred duriog the late Middle Miocene, strongly oscillating sea levels. The eyclic sedimentation patterns situated where a continuous section across the Cretaceous- are also weil preserved in the northem Belgian KaHo Complex Tbe depositional system of the NSB during the Neogene was when the marine Neurath sands were deposited in the Lower Palaeogene (KlPg) boundary is developed (Birklund & Bromley where alternating glauconitic fine sands and clays can be traced dominated by the westward progradation of at least three river Rhine Embayment. At the same time the Eibergen and Biemen- :1; 1979). systems from the Baltic Shield. These rivers were integrated in over a vast area. The Late Eocene succession ends with the horst beds, the anoxie Tostedt clays of northern Lower Saxony :L Bassevelde Sands dated to zone NP19120 (Vandenberghe et a/. the Eridanos river system (Overeem 2002) whieh is a eomplex of and southern Schleswig-Hoistein, the glauconite bed between the 2003). Volcanism rivers, whose number, SOUTceareas and courses varied consider- Hodde and Gram formations in Denmark, and the 'HeUer The Late Palaeoeene and Early Eocene were times of significant ably over time. Neogene development can be subdivided into Middle Eocene paralic facies cover the famous Lutetian Horizont' (Bülow 2000) in Meeklenburg (11.8 Ma: Gürs & volcanic activity at the Thule ridge. This volcanism provided the four phases (Figs 17.5, 17.6 & 17.7). Geiseltal Lignite Distriet (Germany), the Bartonian Leipzig- Spiegier 2000) were deposited. Deposits !Tom this maximum NSB with enormous amounts of volcanic ash. Ash layers can be During the Early to early Middle Mioeene, major progradation Bitterfeld-Halle Lignite Distriet (Eissmann 1970; Eissmann & flooding .event have ooly recently been docwnented from .the traced as far south as northern Germany. Volcanism commenced Litt 1994; Blumstengel et a/. 1999; Rascher et a/. 2005) and the of the Scandinavian and Baltic rivers took place. During the Antwerp sands (Louwye et a/. 2000a). Despite the widespread in this region in the Late Cretaceous and ended in the late Lutetian Helmstedt Formation. Late Eocene paralic areas include earliest Miocene a transgression led to the deposition of the flooding, basin inversion in the Channel region resuhed in the Middle Eoeene (O'Connor et a/. 2000). In the Middle Eneene the Leipzig Lignite Distriet (Standke 2002). Tbe Helmstedt lagoonal Vejle-Fjord clays and sands of Denmark (Dybkjaer simultaneous closure of the southwestern connection with tbe voleanism began in the Eifel region (western Germany). On the Formation is eovered by the marine Middle Eoeene Gehlberg 2004a, b; Rasmussen 2004). This lagoon was soon infilled by the Atlantic Dcean. Tbe exact timing of the maximum flooding is SE margin of the NSB in the Erzgebirge and in the Lusatia Formation. The marine extension of the basin goes far to the NE ( fluvial Ribe sands. Marine conditions prevailed in southem plaeed between 12.3 Ma (van Leeuwen 2001) and ll.8 Ma (Gürs (eastern Gennany) areas, vo1canism started in the lowermost part where vast arnounts of Baltic amber are now found in the marine Denmark and Sehleswig (Klintinghoved Formation). In south- & Spiegier 2000). of the 01igoeene (Standke & Suhr 1998). clays, termed 'Blue Earths' of the Kalingrad area (Standke eastem Holstein and Lower Saxony (northem Germany) the In Late Miocene times, a continuous sea-Ievel fall (Michelsen 1998). middle neritie Lower Miea Clay (Aquitanian to Burdigalian) et al. 1998) and lower subsidence rates in eastern Gennany led overlies the Ratzeburg Formation of latest Chattian age (Hinseh to the emergence of vast areas. Sedimentation was limited to The Oligoeene began with a major transgression during NP21 North Sea Basin: Neogene (K.G., F.w., G,S.) whieh 1I00ded the Egeln-HaHe Lignite Distriet, the Leipzig I986a, 1994). During the Aquitanian peat formation took plaee areas of increased subsidence. While in the early Late Miocene in the Lusatian Lignite Distriet (Standke 2008b). Rieh maero- (Tortonian) large parts of Meeklenburg, Sehleswig-HoJstein, Distriet (Standke 1997), and large parls of the German Mittelge- Tectonic setting and development floras from these lignites indicate wann climate conditions (Mai birge (Ritzkowski 1999b). After a short regressive phase (Van- The Neogene was the time of infiUing of the NSB. Tectonic Lower Saxony and Denmark were covered by the sea, during the 1999, 2000). In the Lower Rhine Embayment the sediment load late Late Miocene (Messinian) the rivers bypassed these regions denberghe et al. 2002) a minor transgression was observed in the development was controlled by intraplate stress regimes resulting of the river system balanced subsidence. NSB in zone NP22 (Gürs 2005), whieh flooded the Upper Rhine from variable spreading rates along the Mid-Atlantie rift and and sedimentation was displaced towards the delta fronts to the A short interruption or slowing down of fluvial input occurred west. Burger (200 I) distingnished three heavy mineral faeies in Valley via the Hessian Depression (Martini 1973). The most Alpine compression. As a result. the NSB underwent basin in the NE and eastem parts of the NSB, after whieh rapid striking transgression took plaee in the early NP23 when the sea subsidence, some inversion and salt tectonism (Clausen et al. the Nieder-Oehtenhausen borehole (Lower Saxony, Germany) infilling eontinued (e.g. Bastrup and Odderup sands; Rasmussen belonging to different river systems with different souree areas, spread over vast areas of the low mountain ranges (Ritzkowski 1999). Strong subsidenee was restrieted to the Central Graben, 2004). Tbe Miocene transgression in northem Belgium com- of whieh only Norway with the Oslo fan ean be speeified. Uplift 1987) flooding the Leipzig Bay (MüHer 1983; Eissmann & Litt the Lower Rhine area, the Eibe Basin and rim sinks of younger meneed with the deposition of the Edegem sands in the Antwerp and deep erosion, with the formation of vaUeys of up to 100 m 1994), the Upper Rhine VaHey,the Lower Rhine Embayment and sah structures. Salt tectonism was especially common in northern region in the Mid- to Late Burdigalian (Janssen 200 I; Steurbaut depth, has been deseribed !Tomnorthem Belgium (Vandenberghe northem Belgium (Vandenberghe et a/. 2002). Germany (Weber 1977; Lange et a/. 1990). Glaeioeustaey- & Verbeek 1988). A seeond transgression in the Antwerp area is Neogene development of the NSB is a\ready evident in the eontrolled teetonism oeeurred !Tom 12.6 Ma onwards in the et al. 1998). These stmetures are filled with the marine Diest and represented by the Kiel Sands with a stratigraphie position Dessei sands of early Late Mineene age. In the Antwerp area, the Late Oligocene following a severe regressive phase when the northem NSB and beeame widespread after the Piaeenzian- between the Edegem Sands and the Antwerp Sands. At the end basin was clearly delimited to the east and river systems brought Gelasian boundary (e. 2.5 Ma) (Overeem 2002). coeval Deume Sands disconfonnably overlie the older strata. of the Early Mioeene, sediment input !Tom the east eeased and, In Early Pliocene times peat fonnation took place in the '-f:~ 1042 M. W. RASSER, M. HARZHAUSER ET AL. "ä PALAEOGENE AND NEOGENE 1043 g"j~:: central part of the Danish North Sea Sector (Rasmussen 2004). Neogene sediments developed on the Precarnbrian platform are c 1 !!l Sediment infill in the Lower Rhine Embayment increased rather thin, whereas slow continuous subsidence of the Palaeo- '5 '0 (Schäfer el al. 2004) and shallow-marine clastic environments zoic platform led to the formation of a much thicker sedimentary 0" prevailed across much of the Netherlands (e.g. Breda Formation; unit during Palaeogene and Neogene times. In addition, some \ a.-g£ Sliggers & van Leeuwen 1987). However, in the northem part of basins developed along major active structural lineaments and » the Netherlands the Astarte trigonata assemblages demonstrate a were later filled by thick continental deposits (up to 500 m). .c deeper environment, probably continuing until late Early Plio- During the Early Palaeocene, the PLB showed a marine ~ cene times. Early Pliocene sea-Ievel highstands are represented connection with the Denmark Basin, the East European Basin, by the Kattendijk Formation (northem Belgium), the uppermost and with western Europe across northern Germany (Fig. 17.1). c 0" Breda and basal Oosterhout formations (the Netherlands), and After a regressive phase, a Middle/Late Eocene transgression N the Coralline Crag Formation (UK). Late Pliocene transgressions from the NW created a conneetion with eold oeearne waters r .!!l j :0 are manifested in the Lillo Formation (northem Belgium), the across the Denmark area. At the same time, a eonnection with 0 upper Oosterhout and the Maassluis formations (the Netherlands) the Tethys was established. During the Oligocene, this connec- ! 0. l and in the Red Crag Formation (UK). During the latest Pliocene tion ceased. Central and eastern parts of the PLB were eonnected '0" the sea retreated from most of the basin and did not return to the with the Atlantic Ocean. The PLB was separated from the I!! \ 0 southem and eastern margins of the NSB until the late Middle Ukrainian and Belorussian basins by an area of shallow shoals LL C Pleistocenc. and islands. By the end of the Oligocene, brackish environments £'" Evidence of glacial conditions, including the presence of deep became widespread. The Neogene is characterized by increasing c e-'" "0 permafrost and icebergs in the southern North Sea off the Dutch continental development with the establishment of large ftood- N coast, have been recorded at marine isotope stages (MIS) 100- plains and lakes. Minor marine ingressions continued in the 'I U'" c 96 (Kuhiman 2004). These initial glacial intervals produced Pliocene. oS" widespread deposition of fine-grained clastics, derived from enhanced erosion of the deep regolith that formed over the NW Sedimentary and stratigraphie development European continent in the warm-temperate climates of the cacliee Neogene deposits are mainly continental, whereas the Palaeogene Neogene. In the tatest PHocene the rates of progradation and is mainly marine (Fig. 17.8). The onset of Palaeogene sedimenta- infill increased dramatically as a result of the increasing input of tion, however, is not synchronous in the Polish Lowlands. In the erosion products during glacial intervals. Three glacial and theee eastern part it began during the Palaeocene, while in the west it c :; interglacial periods are deteeted in northem Germany at this time commenced during the Middle Eocene or Late Eocene/Early "s £ £ (Litt el al. 2002). Oligocene (Rupelian). The thickness of the Palaeogene deposits £5'" E ~~~ ;t Several biozonation schemes have been elaborated for the is c. 50-100 m but can be up to 300 m in basinal areas. e."~ ,f ~~~ BI!! j ~ .cii-eJ : j.~ Neogene NSB. For open-marine settings, biozonations based on During the Palaeocene, marine deposition occurred across the ~g. .. ~g~ planktonic organisms (e.g. bolboforms: (Spiegier 1999), dinofta- entire NE part of the PLB ami, locally (Szczecin Depression), in :;a:0f.i 11° j i:{ gellates (Louwye el al. 2000a, b; Köthe 2003) and pteropods the NW. The Palaeocene PLB is littoral and shallow « 100 m), I- ~ ~ f:! (Gürs & Janssen 2002; Janssen & King 1988» allow a fine- warm-temperate (17-20°C on average) with normal salinity. '" 0 ~ o " o .j~ scaled subdivision of the strata. In nearshore marine settings, Palaeocene sediments mostly overlie Upper Cretaceous rocks ~ ~ biozonation schemes are mainly based on benthic molluscs (Maastrichtian, Campanian), separated by an erosional unconfor- jg O co ?:g & .~ & & ~glE g :11 (Hinsch 1986b; Gürs Weinbrecht 200 I; Gürs 2002; Gürs mity. Their mean thickness is 35 m, but areas with increased o oE g ~ "- E 0 '0 g "~~ 00 ~ ~ "'''- C'" ~,f Schnetler 2004), benthic foraminifera (King 1982; Gramarm & subsidence (Baltic Basin and Mazury High) can have successions co"- o •"~ "'''- ~ () , 0 ~ von Daniels 1988), bolboforms and dinoftagellates. For terrestrial of up to 100 m. The Danian Pulawy Formation comprises marine '" j E j ~.~l ~ ,f and paralic deposits, pollen zonations (Krutzsch 2000a, b; sediments, including marls and limestones with intercalations of ~ .00 Schäfer el al. 2004, and references therein) are available. glauconite and phosphorite. Absolute dating gave an age of .c .0"- .!!l ~ j ij ~ I 60.2 :I: 0.9 Ma (Pozaryska & Kreutzer 1978). Upper Palaeocene ~ 0. ,!l ~ (Selandian, Thanetian) sediments include marls, sands and Voleanism ! Same Neogene volcanism developed in the Lusatia and Erzge- siltstones (Slodkowska 2000). The Thanetian Odra Formation H00 ~ 0."- j birge regions from Early to later Miocene times (Suhr 2003). contains brackish/continental lignitic sands, siltstones and clays. I Early Miocene volcanism is known frorn the Hessian Depression Authigenic depösits are weathered crust with residual clays. sA4JOJeJed 0 !@ wOlse3 '2, 1 1 (Kassel and Vogelsberg) and the Siebengebirge in Nordrhein- Kaolinite covers of plutonic and metamorphic rocks can be up to S08l!l8 leuol8oy 111 d 'B ~i:~~ HIJ~~~ i ~ ~ Westfalia. In Pliocene times tbe Eifel volcanism recommenced. 74 m thick. These sediments are mostly abundant during the sA4JoleJed .~ Palaeogene and rare during the Neogene, I8JJUa::> o soßelS leuol6ay • Polish Lowlands (M.PL, J.R.K.) The PLB Palaeocene can be correlated with the planktonic jlm ~t J foraminifera zone NPFl, the benthonic foraminifera zone BI and t z The Polish Lowlands Basin (PLB) forms the eastward continua- the nannoplankton zones NP land NP3 (Pozaryska & Szczechura .~ z z z z z :l z tion of the North Sea Basin (Fig. 17.4). Towards the north it was 1968; Piwocki el al. 1996). Deposits from the Danian- Thanetian ~~z ~ z z " z ~ a61!lS ~I~"0 0 w Iii z bordered by the Fennoscandinavian Shield while to the south it boundary and the Thanetian were dated using phytoplankton 15w" üi " " '" " ~ w z '" ~ :r~ Ir ::: " Q. Cl was bordered by the Bohemian Massif including the assemblage of the D3 and D4 zones (Slodkowska 2000), which Ga. ~ ~ -'" :r il ~ '"w 11 I I >- Mountains, and by the South Polish Uplands including the Holy are correlated with the NP4 and NP8 nannoplankton zones ! " "' '" "dn " H3ddn I '"3100lW . & ~3MO' ~3ddn I ~3M01 IH3ddn 3100lW ~3MOl ~3ddn I ~3MO' t Cross Mountains (Meta-Carpathians Rampart). Towards the east (Costa Manom 1988). z S9!J8S '"::lOnd I it was connected to the Ukrainian Massif. Following a regression, marked by an erosional unconfonnity 3N3~Olrl 3N3~O()110 3N3~03 3N3~03l\fd between the Palaeocene and the Eocene, the palaeogeography of walS~S 3 N 3 903 N 3N3903V'Vd Palaeogeography and teetonie setting the Polish Lowlands did not change substantially during Early j The Polish Lowlands are framed by two structural units separated Eocene times. A Iocal transgression from the NW is restricted to ~ eJ3 ::I o z o N 3 ::I by the Teisseyre-Tonquist lineament. The NE part of the Polish the Szczecin Depression. A new transgressive influx from the ~ Lowlands belongs to the Precarnbrian European platform and the Ukraine and subsequently from the NW created a connection ewulawLl :" :" !l :G g SW part to the Variscan Palaeozoic platform. Palaeogene and with cold oceanic waters across the Denmark area. Another ~ ~ ~ :il :ß :il :ß ~ ~."

1044 '~ M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1045 transgression from the Tethys reached the Polish Lowlands from Mosina Formation towards the SE. The Czempin Formation (c. 5~,' significant structures there are the Volhynian and Podolian highs number of moHuses and foraminifers oceurs (Pishvanova et al. the west, and probably also from the south, during Middle/Late 25 m) comprises sillstones and silty sands with lignites. The which are oriented in a NW ~SE direction between the upper '..~.'..':. 1970). In the east of the VPP, biohermal and oolitic limestones Eocene times. The pelagic Eocene basin was c. 100-150 m deep deposits of the Upper Mosina Formation (c. 25 m) include parts of the Western Bug and the valley of the Southem Bug developed. The Early Sarmatian bryozoan bioherms cover the with eold-temperate and normal-salinity water. Average annual quartz-glauconite sands with silt and day intercalations. These river. In the north a terrace zone of 30-50 m separates the tops of the Badenian 'Toltry' . temperatures ranged between 16 and 20°C and salinity was not deposits are overlain by the Leszno Formation in the west, which ~~: Volhynian High from the Polessye Lowland. Upper Middle Miocene and lower Upper Miocene sediments lower th[!1131-36%0. Around the Eocene-Oligocene boundary, consists of silty sands. (= Bessarbian regional substage) are restricted to the east of the amber-hearing deltas developed along the coasts (Piwocki & Dating of the deposits is based on the occurrence of planktonic ..•.•.. :.'' Tectonic setting VPP. Oolitic limestones, nubeculariid-foraminifera limestones Olkowicz-Paprocka 1987; Kasiitski & Tolkanowicz 1999). foraminifers of the Rupelian NPF8 zone and of the benthic B6 • •••• The basement of the in the western and bryozoan bioherms formed parallel to the Badenian 'Toltry' Tbe oldest Eocene deposits (Lower Eocene), belonging to the zone spanning the Early-Late Oligocene boundary. Nanno- Ukraine consists of defonned Archean to Lower Proterozoic ridge (Vialov 1986; Paramonova 1994; Anistratenko 2000; Szezecin Formation, include quartz-glauconite sands with plankton assemblages of zones NP21-22 and NP24 have been rocks. To the west the erystalline basement is covered with a Anistratenko & Anistratenko 2005). The intensive uplifi of the gravel and clay intercalations (Ciuk 1973, 1974, 1975). The documented. 'J thick platform nappe, comprising up to 2700 m of Mesozoic- Carpathian Mountains during the latest Middle and early Late Middle Eoeene is represented by the Tanowo Formation, eonsist- Following the regression at the end of the Oligocene, con- Cenozoic sediments. From tatest Early Mioeene to latest Middle Miocene and teetonie reduction of the Subcarpathian Basin eut ing of lignitie clays, siltstones, and sands with thick lignite seams tinental and brackish sediments were deposited across the entire Miocene times, the Podolian-Subdniester Block suhsided result- off the marine connections to the VPP. (Ciuk 1974, 1975). Sediments of the Pomerania Formation (in basin. This led to the development of widespread coastal plains 1 ing in the formation of aecommodation space. With the begin- the north of the PLB) (Ciuk 1974) as weil as its lateral related to the North Sea Basin (Standke er al. 1993). The ning of ,the late Middle Miocene the western part was uplifted equivalents, the Jerzmanowice Formation (west and eentral part) continental deposits developed mostly as floodplains, meandering (up to 450 m) resulting in the erosion of Middle Mioeene Upper Rhine Graben (J.RD.) and the Siemieit Formation (in the east) have a Middle/Late river systems (Osijuk 1979; Kasiitski 1989) and in residuallakes deposits (Palienko 1990). The Upper Rhine Graben (URG) is part of the complex Cenozoic Eoeene age. The 20-m-thiek Pomerania Formation consists of with extensive lignite deposits. rift system of western and Central Europe that extended from the quartz-glauconite sands in the lower part and caleareous sands, Miocene Hthostratigraphic units include the Lower Miocene Sedimentary and stratigraphie development shores of the North Sea over a distance of some 1100 km into sillstones and claystones in the upper part. Tbe deposits of the Rawicz1Gorzow and ScinawaiKrajenka, the Middle Miocene Sedimentation of the VPP commeneed during the late Early the western Mediterranean (Fig. 17.4). The stratigraphie develop- Jerzmanowiee Formation consist of calcareous quartz-glauconite Adamow/Pawlowice, and the Upper Miocene/Lower Pliocene Miocene (Fig. 17.8). The basal Nagoryany beds (2 m) consist of ment of the URG varies in its southem and its northem part sands with gravel and phosphorite grains, and limestone inter- Poznan formations. These are continental lignite-bearing sedi- quartz-glauconitie sand and sandstones, with a diverse marine (Figs 17.9 & 17.10). Bergcr er al. (2005a) subdivided the calations within the uppermost part including molIuses, corals ments of fluviatile and limoic facies. Most of the fluvial deposits moHusc fauna. They discordantly overlie Upper Cretaceous lime- southem URG into three different units: (I) Southern URG and bryozoans. The deposits of the Siemien Formation comprise were related to the southem tributaries of the Baltic fluvial stones. The Nagoryany beds are presumably of Karpatian age (= (Basel Horst, Dannemarie Basin, Mulhouse Horst, Mulhouse ~ calcareous quartz-glauconite sands and sandstones with phos- system. Units of shallow marine and hrackish deposits with late Burdigalian). The discordantly overlying Berezhany heds Basin potassique, Sierentz~Wonschwiller Basin, Rauracian De- phorites and calcareous siltstones, partly with a rieh fauna of glauconite and marine microfauna and phytoplankton occur in (4.5 01) are freshwater limestones and marls, containing ostra- pression); (2) Southem-Middle URG (Colmar, Seiestat, Erstein, moHuscs and corals as weil as amber. the western part of the PLB. Lower and Middle Miocene deposits cods, characean algae and numerous freshwater gastropods. Zorn or Strasbourg Basin, Saveme Fault Zone, Ribeauville & Planktonic foraminifera assemblages of zones NPF6 and NPF7 comprise rather monotODOUSsandy/silty sediments with clay and The Middle Miocene (Badenian regional stage) begins with Guebwiller); and (3) Northem-Middle URG (Haguenau, PecheI- and the nannoplankton zones NP16-20 are documented (Piwocki lignite, while the Upper Miocene is represented by clays with the Baranov Formation (I m) comprising glauconitic sands and bronn, Rastall, Karlsruhe, Landau, Bruchsal- Wiesloch Fault , er al. 1996). The benthic molluscan assemblages of the Pomer- silty/sandy intercalations. Some upper Middle Miocene deposits sandstones with a rich moHusean fauna as weIl as coralline algae. Zone). The North Upper Rhine Graben includes the Mainz and Il ;~ ania and Siemien formations are located within the BMIIA and in SW Poland originated from a brackish marine embayment The Mykolayiv Formation (14.5 m) eonsists of quarlz-glauconitic Hanau basins. BMI3A zones (Piwocki 2002), which are characteristic for the connected with the Paratethys (Luczkowska & Dyjor 1971). " sandstones rich in bryozoans and serpulids, foraminifers, bi- A general synthesis on the Upper Rhine Graben was recently j Upper Eocene of NW Europe, and also for the Latdorfian facies , Pliocene deposits are represented by the upper part of the valves, brachiopods and rare echinoderms (Vialov 1986). Tbe published in the frame of the EUCOR-URGENT project ('Upper (Hinsch er al. 1988). !I Poznan and the Gozdnica formations together with their litho- Narayiv Formation (25 01) represents the most continuous hor- Rhine Graben Evolution and NeoTectonics', Behnnann et al. Around the Eocene-Oligocene transition, a marine trans- stratigraphie equivalents (e.g the Zi~bice Group; Dyjor 1966; izon. Dense coraIlinaeean limestones with huge rodoliths, peeti- 2000). The stratigraphy and palaeogeography, together with a gression encroached from the NW European Basin (Kockel Czerwonka & Krzyszkowski 200 I). Tbe Poznait Formation nids, oysters and an impoverished foraminifer fauna are typieal detailed reference list, were published by Berger er al. (2005a, 1988; Gramann & Kockel 1988) towards the Polish Lowlands comprises clays and silts with sandy intercalations and thin (Vialov 1986). The Rostotchya Formation consists of quartz b). This seetion presents an overview of these articles. Another (Piwocki & Kasiitski 1995; Ciuk & Pozaryska 1982). The lignites deposited mainly in fluvial (floodplain), lacustrine and ,.'.1 sands and sandstones with moHuses comparable to the Baranov study on the Rhine Graben examines the eorrelation of eustatic connection with the Tethys was severed during this time. A ! limnic settings. Continental sedimentation was interrupted by Formation (Vialov 1986; Kulchytsky 1989). A thin layer (10- sea-Ievel changes, rifting phases, palaeogeography and sedimen- shaHow epicontinental sea connected with the Atlantic Oeean marine ingressions, which periodieally transformed nearshore 15 cm) of limestones or calcareous sandstones constitutes tbe tary evolution (Sissingh 2003). covered the central and eastem parts of the Polish Lowlands. The lakes into brackish lagoons (Kasiitski er al. 2002). The Pliocene Kryvtehe Formation and represents an important marker horizon. seawater was relatively cold (l0-20'C) with normal salinity, but ~ deposits of the Poznan Formation were deposited under tempe- The upper Badenian Pidhirtsy Formation is restricted to the Palaeogeography and teetonic setting slightly oxidizing conditions (Buchardt 1978; Odrzywolska- rate and periodically cold-temperate and humid eonditions east of tbe VPP. It eomprises sandstones with molluscs, foramini- Palaeogeographic reconstructions of the URG were published by Bieitkowa er al. 1978). The Oligocene Polish Lowland sea was ~; (Stuchlik 1987). During sedimentation, the climate became fers and bryozoans (Pishvanova er al. 1970; Vialov 1986). The Kuhlemann & Kempf (2002), Sissingh (1998, 2003), Becker & [:,l' separated from the Ukrainian and Belorussian basins by an area increasingly arid. The Gozdniea Formation comprises sandyl upper Badenian Temopil beds (6 m) consist of corallinaceans Berger (2004) and Berger er al. (2005b). Following an initial of shoals and islands. The presenee of quartz-glaueonite sands gravelly c1astic deposits with fine silt and clay interealations (mainly rhodoliths), grading into clayey glauconitic sand and fluviolacustrine phase of sedimentation (Middle Eocene), the records a regression at the end of the Early Oligocene. A developed under conditions comparable to the Poznan Formation. limestone. Tbe general charaeter of the fauna is the same as in URG was affected by an initial rifting phase that was responsible subsequent short transgression extended as far as the west of the the underlying units, but additionally a biohermal limestone for the development of large conglomeratic fans along the PLB. By the end of the Oligocene, the marine development Volcanism (Podolian Toltry or Miodobory), dominated by coralline algae eastem, western and southem graben margins. The axis of the ceased. The last regression was connected to the uplift of the The Lower Silesian volcanics comprise basic volcanic and and vermetids, is found (Vialov 1986). evolving URG was occupied by salt basins in its southern areas Sudetes Mountains. pyroclastic rocks (up to 200 m) which belong to the eastem part The uppermost Badenian is represented by the Bugliv Forma- with brackish (with local sall) to lacustrine facies developing in Oligoeene deposits are common on the Polish Lowlands with of the Mid-European Volcanic Province. This extends over 700 tion (Grischkevich 1970) representing an offshore facies. It its central parts, and fluviatile to lacustrine facies in its northem thicknesses ranging from several metres up to >100m. They km in front of the Alpine-Carpathian system. Most of the includes an impoverished marine fauna with the endemic bivalve part and in the Mainz Basin. commence with the Lower Mosina Formation comprising green loealities are situated on the Fore-Sudetic Block along the margin Parvivenus konkensis media (Sokolow) and can be eorrelated Ouring the Early Rupelian, a general transgression came from quartz-glauconite sands, gravels, phosphorites, siderite eoncre- of the Sudetes Mountains. Vo1canic rocks include basalts, with the Konkian regional stage in the eastern Paratethys (Vialov the North Sea; following a regressive phase marked by laeustrine tions and rare amber grains (Ciuk 1970, 1974). The Eocene- trachytes, tephrites, basanites, phonolite basanites, quartz latites, 1986). (north) and sall (south) deposition during the middle Rupelian, Oligocene boundary is difficult to determine hut may be placed phoideferous basalts, nephelinites, dolerites, basanitoides, lim- Tbe late Middle Miocene sediments of the Sarrnatian regional the sea again invaded the entire basin during the Late Rupelian, within the lower Mosina Formation (Odrzywolska-Bieitkowa er burgites, ankarites, trachyandesites and trachyphonolites (Wierz- stage are transgressive attaining a thickness of 25-100 m (Vialov resulting in a possible connection with the Paratethys Sea via the al. 1981; Piwocki er al. 1985, 1996). The marine Rupelian cholowski 1993). 1986). In the NE of the VPP the Sarmatian can be clearly North Alpine Foreland Basin. During the Late Oligocene, (100 m) crops out in the western part of the Polish Lowlands. lt correlated with the Volhynian and Bessarabian regional substages fluviolacustrine sedimentation prevailed, with loealized marine eonsists of siltstones and claystones with sphaerosiderites and of the eastem Paratethys (Grischkevich 1970; Pishvanova er al. ingression in the northem part of the URG. moHusc remains. Similar deposits are eommon in Gennany and Volhyno-Podolian Plate (0. Y.A., V.V.A.) 1970). The lower part of the the Sarmatian deposits consists of During the Early Miocene, the southem URG was affected by are named the Septaria Clays. These deposits interfinger with the The Volhyno-Podolian Plate (VPP) (Fig. 17.4) represents the SW sand (1.2 01) and ooHtie sandstone containing a rich endemie uplift and erosion. In the northem URG, brackish (rarely marine) brackishlcontinental Czempin Formation and the marine upper margin of the East European (= Russian) Platform. The most moHusc fauna. Up-section, a coarse-grained sand with a huge sedimentation prevailed. In the Late Burdigalian, the basin w"as 1046 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1047 U Basement

.w.:Jqee, SM : Schwarzwald l~ (Brack Forest) massif .W.:J 6u!J9J\. &t ~Volcanoes

"' c SSle4S J u V : Vogelsberg ~ 4:)sAl.:tlatI66@M 5 ~o 4:>S~I;Jla6IWnf) :I:~ ! Cenozoic sediments Fr: Frankfurt w 1. Southern URG M: Mainz J 2. S-Middle URG H: Heidelberg 4:;)S~.::I:l"a"I

"-~.l! ~~

c 1! Fig.17.10. Geology ofthe Upper Rhine Graben. ~g~ :::J .~z & affected by two important volcanic events (Kaiserstuhl and west, sorne undated conglomerates are tentatively assigned to tbe Vogelsberg events). Lutetian and the Priabonian (Duringer 1988). c Reftection seismic data, ealibrated by weHs, indicate that south 1l On the Mulhouse Horst, brackish marls and lacustrine lime- ~~£ of the city of Speyer a regional erosional unconfonnity of mid- Co stones, probably ranging from Lutetian to Priabonian in age, are Burdigalian age cuts progressively deeper southwards into Burdi- ~~~ present. The Melanien Limestones are of Priabonian age (MP 18) galian and OIigocene sediments. Ihis unconfonnity is related to :E at Brunstatt (Schwarz 1997; Tobien 1987). In the eastern part of a: the uplift of the Vosges-Black Forest arch, including the south- the basin, some conglomerates (locally dated by mammals ern part of the URG (Roll 1979; Dezes el a/. 2004). During the sA:lualBJBd (MP 18; Tobien 1987)) probably accumulated during the Priabo- leJlUG:) Late Miocene, the sedimentation was essentially continental, niaß. Sla8elS leuol6a~ brackish and lacustrine. In the Mainz Basin Langhian-age In the Colmar-Haguenau area a similar development occurs, sediments are absent. In conjunction with progressive uplift of and includes iacustrine limestones, Lymnaea Marls and salt ~ the Vosges-Black Forest arch, the central and soulhern parts of formation. A brackish complex (Zone Dolomitique) generally ~ I the URG were subjected to erosion. •6e1S '''r~~ ~I~ overlies these deposits, but it has not been dated. Conglomeratic 5 ~ iIi~ "z ; m :5 I facies are present at both basin margins (particulary from the Priabonian onwards). Towards the north, the Lower Pechelbrnnn "dnJ-, ~3ddn 31001~ l:l3MOl l:l3ddn ~3MOl 31001~ Sedimentary and stratigraphie deveJopment SBlJaS ~3ddn l:l3MOl l:l3ddn 03MOl Beds are partly dated by mamma!s as Priabonian (MP20; Tobien :JOnd 3N3~OIV\l ~ 3N3008110 3N3003 3N30031Vd Eocene sedimentation in the southem Upper Rhine Graben (987). generally commences with Middle to Late Eocene sideroIithic wa~s,(s 3 N 3 9 0 3 N 3N3903"'''d Early Rupelian sedimentation is represented by: (l) the Middle 1 deposits (MPI9). These are overlain by various sedimentary and Upper Sall Formation (Dannemarie Basin); (2) the Middle ~ facies whose deposition was inftuenced by tectonic processes in eJ3 :l o z o N 3 :l ~ and Upper Pechelbronn beds (Colmar-Haguenau areal (NP22; the URG. Accumulation of brackish sediments (Lymnaeemner- Griessemer 2002); (3) the Zone fossilifere and the Streifige eWU!IlWU ~ gel) and salt (Lower Sah Formation) took place. Tbeir ages ~ ~ ~ ~ ~ ~ g s :gl ~ Mergel (= Marnes en plaquettes) as weil as the Haustein - the probably range from the Lutetian to the Priabonian (NPI2 to latter is dated as NP21-22 (Schuler 1990) and MP21 (Altkirch NPl?). However, it is not clear if sedimentation was continuous fi: (see Storni 2002; Hinsken 2003), Mulhouse Horst); and (4) the '" or if a gap occurred during the Bartonian (Sissingh (998). In the conglomeratic facies at both basin margins. 1048 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1049 The Zone fossilifere and the Middle Pechelbronn Beds the Sprendlingen Horst), the famous Messel Formation accumu- 1986; Semmel 1983). Late Plioeene sediments probably exist in limesIones) indicating the beginning of subsidenee during the represent the first Rupelian transgression from the North Sea lated in a maar lake (Harms 2001). These sediments are dated by the Heidelberg and Frankfurt areas (Hottenrott el al. 1995). Early Eoeene (perhaps Palaeocene) in eastem Switzerland and (partly corresponding with the global sea-Ievel rise following the mammals as MPII (Tobien 1988). The Priabonian Lower during the Middle Eocene in the west; subsidenee was accom- Ru I sequence at 33 Ma; see Hardenbol el al 1998). In the Pechelbronn Beds (Rüsselsheim Basin) and 'Green marls-Rote Helvetle units: western pari (J.P.B.) panied by prominent normal faulting creating different structural Middle Rupelian. the most important marine transgression Leitschicht' (Mamheim Bay) overlie the Eocene basal sediments. blocks. The timing of this faulting, associated with eustatie sea- (second marine Rupelian transgression from the North Sea, The 'Green marls-Rote Leitschicht' correlate with the Lutetian Prior to their tectonic incorporation into the Alpine orogenie level ehanges, was responsible for the sedimentation in the corresponding with the global sea-Ievel rise between sequences Embergeri Zone and the Priabonian Veclensis Zone (Schwarz system during the Eocene, the Helvetic units were part of the Helvetic domain, as demonstraled by Menkfeld-Gfeller (1995). Ru2 and Ru3; see Hardenbol el al. 1998) flooded the entire 1997). Along the margins of these basins, terrestrial alluvial-fan stable European continent and fonned its southem margin. From the Lutetian to the Priabonian, these shaIlow-marine URG. The sediments associated with this transgression constitute deposits aecumulated during the Lutetian to Early Rupelian ~:f Towards the south, the Helvetic units pass into the Ultrahelvetic units were eovered by mieaceous Globigerina marls and shales the classical succession from tbe Foraminiferenmergel to the (Grimm & Grimm 2003). Eocene sediments are absent in the Unit and the Penninie Flysch Zone (see below) (Figs. 17.11 & (Stad Schiefer) with an anoxie facies occurring in the NW Fischschiefer and partly 10 Ihe Meletta-Schichten. These sedi- Hanau Basin. 17.12). Due 10 the Alpine causing overthrusting and (Melella Shales). Lutetian to Priabonian deep-marine sediments ments range from NP23 to NP24 (Grimm 2002). They are During the Rupelian, the sedimentary history was similar to increased subsidence of the Helvetie units, deeper marine are present in the (Einsiedeln Formation, combined wilh the Late Rupelian brackish-marine Cyrenenmer- that of the Southem URG, with the deposition of the Middle Globigerina-rich marls and shales were deposited during the Late Steinbaeh-Gallensis Formation,Bürgen Formation,Globigerinen- gel into the so-called Graue Serie (= Serie grise), representing Pechelbronn Beds (first marine Rupelian transgression), the Eocene. This is, herein, considered to be a transition to the mergel, Flysch sudhelvetique, Mames a Foraminiferes, Hohgant an important seismic marker. During tbe Early Chattian, the Upper Peehelbronn Beds, the Alzey, Bodenheim, Stadecken and foreland sedimentation of Ihe North Alpine Foreland Basin (see Formation). In addition, eoastal facies (Klimsenhom Formation, fluviatile sediments of the 'Molasse alsacienne' interfingered to Sulzheim formations (seeond and third marine Rupelian trans- below). Wildstrubel Formation) and brackish environments (Couches a the north (Tüllinger Berg) with lacustrine or brackish marls and gression, eorresponding with the 'Serie grise' in the Southem Cerithes, Couches des Diablerets, Sanelsch Formation) of the II with the fluviolacustrine Niederroedener Beds. During' the Mid- URG), Ihe Niederroedener Beds and the brackish Cerilhium beds Sedimentary and stratigraphie development same age are also recognized (see Herb el al. 1984; Herb 1988; i~ die and Late Chattian, the lacustrine limestones of the 'Calcaires (Grimm el al. 2000; Reichenbacher 2000; Grimm & Grimm The sedimentary history of the Helvetic units eao be summarized ,li Menkfeld-Gfeller 1994,1995,1997; Weidmann el al. 1991). delemontiens' and the Tüllinger Kalk were deposiled. The 2003). in a number of stages (Fig. 17.9): (I) continentai residual fissure- :ru The western part of the Palaeogene Ultrahelvetie domain is 'Calcaires delemontiens' are weil dated as MP29 to MNI in Ihe The Upper Cerilhium Beds cross the Chattian-Aquitanian filling (= siderolithic) and freshwater limestones of Middle charaeterized by deep marine sedimentation. This is described Jura Molasse (Becker 2003; Picot 2002), and the Tlillinger Kalk boundary. The brackish-IagoonaI sediments of the Oberrad Eocene age; and (2) shallow-marine sediments (Le. nummulitic and discussed below. can be eorrelated by eharophytes with the Middle Chattian 't~1 Formation (= upper part of the Upper Cerithium Beds; see Stephanochara ungeri Zone. These deposits are overlain by the Schäfer & Kadolsky 2002) are of Aquitanian age (MNI, MN2; brackish-lacustrine Cerithium Beds. Engesser el al. 1993; Försterling & Reichenbacher 2002). The From the Aquitanian onwards, the southem and middle parts overlying braekish-laeustrine marls and limestones of the Rüssin- o UH : Ultrahelvetic Flysch G : Gurnigel Flysch of the URG were subject to erosion. Sediments may have been gen Formation (= Inj/ala Beds) still belong to the Aquitanian UHm : Meilleret Flysch Gs : SchlierenFlysch '] deposited up to the onset of the uplift of the Vosges and the (MN2a; Engesser el al. 1993). In the uppermost part of the UHh : Höchst Flysch Gv : Voirons Flysch Black Forest (Burdigalian), or the non-deposition may already Rüssingen Formation, biota indicate a further braekish-marine Gf : Fayaux Flysch ~ have commenced during Middle and Late Aquitanian times, as ingression from the south (Reichenbacher 2000), which was M : Medianes Flysch - Gn : Niremont Flysch proposed for the Jura Molasse (see Picot 2002; Becker 2003). again followed by an ingression from the North Sea (Martini E'Z2Zl o : Ortler nappe ~i Sedimentation locally resumed during the Early Tortonian, with 1981). This ingression characterizes the base of the Wiesbaden N : Niesen Flysch (Chesselbach) the deposition of Ihe Dinolherium and Hipparion sands (daled by Formation (= Lower Hydrobia Beds; see Reichenbacher & - W : Wägital Flysch mammals as MN9). No Messinian sediments are known. In the Keller 2002), which mainly eonsists of bituminous marls and o (+ Lichstentein-Vorariberg Flysch) northem part of the URG, sedimentation continues during the limestones and is of Aquitanian age, exeept perhaps in its - Aquitanian with the deposition of the brackish Upper Cerilhium uppermost part. ~ P : Prättigau Flysch j Beds, which are overlain by the Rüssingen Formation (formerly During the Burdigalian, brackish sedimentation was progres.- Inj/ala Beds), and are followed by the Wiesbaden Formation sively redueed and replaeed by laeustrine and fluviatile deposits. "'11 B Basement (Mt-Blanc/Aiguilies Rouges + Aar/Gothard) 1 (formerly Lower Hydrobia Beds). According to its correlation During the Langhian and the Early Serravallian, sedimentation (actual position) ,; with the Mainz Basin (MN land MN2; see Reichenbacher 2000), was essential1y eontinental, braekish or lacustrine in the Northern this succession appears to be Aquitanian in age. The Upper URG and the Hanau Basin (e.g. Staden Formation, Bockenheim Hydrobia Beds are still present and may be attributed to the Formation; see Grimm & Hottenrott 2002). A plateau-basalt Early Burdigalian (MN3). During the Late Burdigalian an !il layer ('Maintrapp'), with a radiometrie age of 16.3 Ma, is found ~i important volcanic event took place at Kaiserstuhl. Following a between the Staden and Bockenheim formations (Fuhrmann & significant gap (Burdigalian to Messinian), sedimentation was Lippolt 1987). In the Mainz Basin, no Upper Burdigalian to 1 resumed during the Pliocene. Upper Serravallian sediments are known. The presenee of An importantsedimentary event is represented by the Sundgau limnofluviatile Tortonian deposits is _represented by the Lauter- Gravel, which may be Middle Plioeene (MNI5-16) in age, based sheim Formation, the Dinotherium sands and the Dom Dürkheim on comparison with the Bresse Graben mammal localities (Petit Formation, whieh are dated at several localities within the Mainz el al. 1996). Locally, the Arvemensis Gravel is present (MNI4- Basin (MN9 and MNll). The presence ofseveral unconformities MN16; Tobien 1988). Plioeene deposits (dated by spores and (Lower Serravallian- Tortonian, Tortonian-Lower Messinian as pollens) are also known from the vicinity of Colmar and weil as below the Piacenzian Arvernensis Gravels) is still Strasbourg. Following a gap (Burdigalian to Messinian), sedi- controversial; field and borehole observations iodicate three mentation in the northern part resumed in Pliocene times (e.g. breaks in sedimentation, whereas seismic lioes do not show any Haguenau area). uneonformity during the Mio-PHocene in Ihe northem part of the During Ihe Eocene and Early Oligocene, the northem Upper URG (Dezes el al. 2004). Rhine Graben was not yet developed and the main structures Uppennost Mioeene to Plioeene sediments are known from Gv were influenced by pre-Palaeogene tectonics. From north to some areas of the Mainz Basin and the western part of the south, pre-rift struetures incJude the Rüsselsheim Basin, the Northem URG. They are represented by the 'White Mio- Palatinate-Stockstadt Ridge, and Mamheim Bay (Grimm & PHocene' and Bohnerz c!ays (Rothausen & Sonne 1984; Grimm UH Grimm 2003). In Ibe Rüsselsheim Basin, Mamheim Bay and the & Grimm 2003). Piaeenzian-age fluviatile sediments are repre- UHm UHh southerly eonnected northem URG, sedimentation eommeneed sented by the Arvemensis Gravels and the Weisenau Sands of UH with the terrestrial 'Eozäner Basiston' and 'Basissand'. On the the northemmost URG and the Mainz Basin and dated by Palatinate-Stocksladt Ridge (particulary on its eastem part, Le. magnetostratigraphy and heavy mineral associations (Fromm Fig. 17.11. Flysch deposits in Swilzerland. 1050 M. RASSER, M. HARZHAUSER Er AL. w. PALAEOGENE AND NEOGENE 1051 LaIe Paleocene Palaeogeography 'Gryphaeenbank'). Glaueonite is generally abundant and in- ized by coarse~grained, poorly sorted, limestones containing iron .Bern From north to south, the central and eastem part of the Helvetic creases up-section. The coarsening-upwardtrend and the termi- ooids and larger foraminifera. In Bavaria, this member had been Unit (HU) passes into the Ultrabelvetie Unit (UU), the Rhenoda- nation by ooid-bearing sandstones suggest a shallowing of the mined for its iron (Gümbel 1861; Hagn & Wellohofer 1973). The nubian (= Penninie) Flysch Unit (RFU), and the Austro-Alpine depositional system from the Danian to Thanetian. This relative units ineluding the Gosau Basin. Weitwies Membe~ (= 'Fossilsehicht') comprises glauconitic bio- sea-Ievel fall corresponds to a long-term eustatie sea-Ievel fall, elastic limestones rich in larger foraminifera. Towards the top Geneva• Most authors suggest that the Palaeogene depositional envir- which iodicates that subsidence duringthe Palaeocene was low. these grade ioto glauconitic marls with nummulitids and mol- onement of the HU as weil as the adjaeent UU and RFU was The glaueonitie sands of the Kroisbaeh Member pass upwards luses. In the Haunsberg area it also eonlains phosphate nodules morphologieally determined by the presenee of several submar- 11' into red-algae-dominated limestones (eompare Kuhn (1992) and (Traub 1953). ine highs and island ehains. The northernmost high is the modifieations by Rasser & Piller (2001» of the Thanetian The entire Lutetian succession represents aperiod of eustatic Intrabelvetie High (Hagn 1954, 1981; Vogeltanz 1970), whieh l,1 :;t Fackelgraben Member. This member is eharaeterized by bedded sea-Ievel fall. Sinee the deseribed facies paltern indieates a separates a northern (Adelholzen faeies) and a soothern (Kres- rhodolith and red algal detritie limestones with thin marly relative sea-Ievel rise, Rasser & Piller (2001) have suggested that senberg faeies) Helvetie faeies unit. Emersion of this high from interealations. It develops gradually from the pyenodont sands the increased subsidence rate continued during the Lutetian. This latest Maastriehtian to Middle Eocene times, resulted in the below and still eonlains detritie glaueonite. :\f eoineided with the ftooding of the northern Helvetie Unit, whieh development of a sedimentary gap in the northern HU, while Near the Palaeoeene- Eoeene boundary a deepening of the represents a backsteppingtypieal for transgressions on carbonate sedimentation eontinued in the southern HU (Hagn 1981). The environment is indicated in western Austria by the shift from the ramps (cf. Dorobek 1995). This feature is typical for foreland Pre-Vindelieian island ehain (Traub 1953) marks the transition red-algae-dominated limestones towards a globigerinid facies basins and was related to the ongoing subduetion of the from the HU to the Uu. The UU ean be subdivided into a f' • Bern Middle-Lale Eocene (NP9, after Oberhauser 1991). Due to an angular uneonformity, European Plate below the Afriean-Adriatie Plate . northem Ultrahelvetie facies, eharacterized by marls, and a 1, these deeper-water sediments are absent in . This would Lutetian shallow-water carbonate deposition was terminated southern Ultrahelvetic faeies, characterized by carbonate-free jj; suggest that tilting and erosion took plaee elose to the Palaeo- by Bartonian to Priabonian deep-water conditions, and the so- elays (Hagn 1981). The southern Ultrabelvetie facies was ~! eene-Eoeene boundary. Rasser & Piller (2001) argued that the ealled 'Stockletten' (globigerinid marls, >100 m thiek) overlay separnted from the adjaeent turbiditie RFU by the Cetie Island ;;1 r~ angular unconformity was related to a tectonic pulse within the the Kressenberg Formation. This succession represents an on- Ridge (Hagn 1960, 1981). ~. Alpine system to the south ('Laramide 3' of Tollmann 1964) going baekstepping of facies belts of the ramp towards the north. The UU represents a depositional realm to the south of the \ whieh eOITesponds to a rapid westward shift of the Alpine The autoehthonous subsurfaee of the later North Alpine Foreland HU. It is characterized by the Cretaceous to Eocene 'Buntmer- { Nappes (Oberhauser 1995). Consequently, the Basin was covered by Bartonian-Priabonian shallow.water car- gelserie' , comprising marls which contain olistoliths and turbi- began to affect the sedimentation in the HU elose to the bonates, which were reworkedas olistoliths into the 'Stockletten' dites probably derived from the Cetie Island Ridge (Faupl 1977). rf, Palaeocene- Eocene boundary. (Buebholz 1989; Darga 1992; Rasser 2000). Further Eoeene- , The Thanetian to Lutetian KressenbergFormationis charaeter- Oligocene shallow~water carbonates of the circum-Alpine area, Tectonic setting istic for the earlier Eocene of the HU. The Ypresian cornmences inelude occurrences of the RU, were summarized by Nebelsiek j The Palaeogene development of the Helvetie shelf was influ- with the mainly ferrugenie Frauengrube Member (= 'Ro- el al. (2003, 2005). The long-term eustatie sea-Ievel fall ! eneed by the Alpine Orogeny. CollisionaI proeesses led to the terzschichten'). This is eharacterized by massive, iron-ooid 1QOkm eontinued until the Early Priabonian and was followed by a J subduction of the European Plate below the Afriean-Adriatie bearing, nummulite limestones and coarse-grained sandstones to continuous rise up to the Eocene-Oligocene boundary. Plate within the Penninie Realm. Subduction resulted in the fine-grained conglomerates. Quartz grains are frequently coated I Fig. 17.12. Palaeogeography ofthe Swiss Flysch after Caron el al. formation of the Alpine Foreland Basin with a more or less by iron, while most bioelasts are completely ferruginized. Flat !' (1989). Abbreviations: GL, gumigel; SA. Sarine Slices; SL, Schlieren; east-west striking basin axis aod a corresponding east-west and unfragmented lacger foraminifera indieate very low energy Alps and Alpine Foredeep: overview (M.W.R.) va, Voirons. striking shoreline (Prey 1980; Wagner 1998). Sedimentation in conditions. However, tbe oceurrence of high~energy iron oöids Tbe Alps are a mountain ehain formed during the multiphase the HU ceased in the Late Eocene, when it was eompletely and ferruginized allochems in the same sediments suggest the Alpine Orogeny (see also Froitzheim el al. 2008; Reieherter el I overthrusted by the northward-moving Alpine nappe system opposite. Consequently, this faeies has been interpreted by Rasser al. 2008). They are separated into the Western Alps situated west (Hagn 198/). l & Piller (2001) as representing a mixture of two different of the Rhine Valley, and the Eastem Alps between the Rhine environments (e.g. input of iran ooids from ooid bars into the Valley and the Vienna Basin (Fig. 17.13). The Carpathians Sedimentary and stratigraphie development l Helvetic units: eastern part (M. W.R.) relatively deeper water where the larger foraminifera Iived). The representtheir eastwardcontinuation.During the Palaeocene and Sediments in Austria and Bavaria show a more or less continuous Ypresian-age ferrugenic sedimentationceased with the formation Tbe Helvetic units in Austria and Bavaria are part of the Eastern Eocene, the Alpine system formed an arehipelago ineluding the development from the Jurassie to the Late Eoeene (Fig. 17.9). A of sand bodies of the Sankt Pankraz Member. In the Haunsberg Alpine Foreland, and form a narrow, cast-west trending belt Gosau basins. The Penninie tectonic units together with the generalized seetion of the Palaeogene Helvetie Unit comprises acea, it is characterized by up to 32 m of matrix-free, fine- north of the Alpine orogenie wedge. Sedimentary successions in Rhenodanubian Flysch Unit, formed the northern eontinuation of Danian to Upper Thanetian silicielastic pelagic sediments, grained sandstones without fossils. Its development in Bavaria is the Vorarlberg area (westemmost Austria) are comparable to the Gosau basins and representthe main element of the Alpine followed by uppermost Thanetian algal limestones. These are characterized by a coarse-grained sandstone to fine-grained those of Switzerland (see above). Therefore, this section focuses Foredeep. The Helvetie Unit (see above) formed the northern overlain by Ypresian to Lutetian ferruginous larger foraminiferaI conglomerate, rieh in larger foraminifera.In the Haunsbergarea, on the occurrences in Bavaria, Salzburg and . continuation of the Penninie units. Towards the east, the Flysch limestones and siliciclastic sediments. Deep-marine conditions these sands represent subtidal sandbodies which show a marked Overviews have previously been published by Richter (1978), Zone continues into the CarpathianForedeep. During the Eocene, occurred from the Bartonian to the Priabonian;.they are ehar- fluvial influence, as weil as a high degree of reworking Prey (1980), Tollmann (1985), Oberhauser (1991, 1995), Kurz el the Alpine Orogeny led to subduetion of the Penninie oeeanie aeterized hy the marly 'Stockletten". Sedimentation eeased atthe (Vogeltanz 1970). The facies sueeession indieates a shallowing- al. (2001) and Rasser & Piller (2001). Most oeeUITenees of the erust and related units beneath the Alps. Together with the Eoeene-Oligoeene boundary. upward from ooid bars (Frauengrube Member), surrounded by Helvetic Zone in western Austria are tectonically isolated; all of Helvetie Unit these were ineorporatedinto the Alpine orogenie The Palaeogene suecession begins with Palaeocene marls and deeper foraminifera-rich sediments, up to the sandbodies of the them are considered to be part of the southem Helvetic faeies. wedge, resulting in the tennination of sedimentation in the marly sands of the Olehing Formation. They developed direetly Sankt Pankraz Member. The Middle Ypresian age of these Classic studies based on the Bavarian occurrences, such as the Penninie and Helvetic units, and the Gosau basins during the above Upper Cretaeeous sediments (Traub 1953, 1990). The ferruginous foraminiferal limestones (P7?, after Kuhn 1992) Kressenberg (Gümbel 1861; Schlosser 1925; Hagn 1967, 1981; Eocene. Sedimentary environments and processes changed re- Danian- Thanetian Olching Formation (Pla-P5; Kuhn & Wei- coincides with a long-term eustatie sea-Ievel fall beginning Hagn & Wellohofer 1973; Ziegler 1975, 1983; Rasser & Piller markably during Oligoeene and Miocene times. dich 1987; Kuhn 1992) represents one of the most fossiliferous during the Middle Ypresian. The rates of siliciclastic input can 200 I), have been published. However, only rare publieations deal Palaeoeene units with respect to macrofossils (e.g. Schultz be eorrelated with a short-term eustatie sea-Ievel fall during the with other Bavarian loealities, such as Grünten (Reis 1926; 1998).118 depositional depth was c. 50-150 m (Kuhn 1992). The ratest Ypresian. The accornmodation spaee neeessary for the units: flysch zones in Switzerland (J.RB.) Ziegler 1983) and Neubeuem am Inn (Hagn & Darga 1989). abundanee of sands and sand beds interealated with the marls deposition of the ferruginized limestones and the 32-m-thiek Occurrenees in Salzburg and Oberösterreich (Austria) ace domi- Caron el al. (1989) presented a delailed overview of the increases upward. The Olching Formation is overlain by the sandstones requires an inereased subsidence rate at that time, nated by sediments altributed mostly to the Southern Helvetie palaeogeographie development from the Turonian to the Late Thanetian Kroisbaeh Member, whieh represents the basal part of suggesting that the subsidenee rate was mueh higher than during faeies. They are best developed in the Haunsberg area, north of Eoeene subdividing the sueession into three areas (Figs. 17./1 & the Kressenberg Formation. This member is characterized by the Palaeoeene and the Early Ypresian. Salzburg (Traub 1953, 1990; Gohrbandt 1963; Vogeltanz 1970; 17./2): (1) Ultrahelvetie Unit and Niesen- and Medianes Flysch quartz sandstones rich in iron coneretions, iron ooids, small Lutetian limestones are representedby the KressenbergMem- Prey 1980, 1984; Kühn & Weidich 1987; Kühn 1992; Sehultz with a north-Tethyan eharneter; (2) the Gurnigel Flysch of brachiopods and pycnodont bivalves, as weil as coarse-grained ber and the Weitwies Member (Rasser & Piller 2001). The 1998; Rasser & Piller 1999a, b, 2001). Central Tethyan origin; and (3) the south Tethyan Flysch, sands partieularly rieh in pyenodont bivalves (formerly known as Kressenberg Member (= 'Schwarzerz Schichten') is eharneter- restrieted to the Cretaceous. During the Late Eoeene, the I 1052 l M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE i , 1053 1!i gravity flow processes to occur. Petrographical and structural to override the Ultrahelvetic unils and Pre-Alpes Medianes, but A analyses clearly demonstrate the £oIe of compressive tectonics on later reverse fauhing has emplaced the front of the Pre-Alpes Munieh. the 'flysch' sedimentation (Caron et a/. 1989). However, as Medianes over the rear of the Gumigel Nappe (Caron et a/. i postulated by Stuijvenberg (1979), eustasy was also responsible 1980). Several loca1 names have been proposed within this unit, I for the accumulation of the Gurnigel Flysch. such as the Voirons Flysch (Stuijvenberg 1980), the Fayaux ! Flysch (Stuijvenberg et a/. 1976), the Niremont Flysch (Morel Sedimentary and stratigraphie development 1980) and the Schlieren Flysch (Winkler 1983). Tbe various stmctural units which make up the Pre-Alps (from This flysch is mainly composed of turbiditic shales and thin the Arve River in France to Lake Thon) may be situated sandstones with fine-grained carbonate turbidites, hemipelagic palaeogeographically in aseries of basins extendiug from the shales with bentonite layers as weil as rare thick.bedded European margin of the Tethys across an oceanic acea and ooto sandstone channels and conglomerates. The thickness ranges .~ the southem margin (Adria); from NW to SE these are (Figs. from 1.5 km (Gumige1-Schlieren areal tu 2.5 km (Voirons). Tbe 17.9, 17.11 & 17.13): (I) the distal Helvetic shelf with the original substratum is unknown. The upper limit corresponds to Ultrahelvetic Unit; (2) the Valais Trough as an oceanic basin an erosional surface. Tbis flysch comprises classicaJ Bouma-type 1I 47'N- ineluding the Niesen Nappe and North Penninie Melange; (3) the turbidites and bears the entire facies speclrum of Multi & Rici Brian~onnais Microcontinent containing the Pre-Alpes Medianes Lucchi (1972). The depositional environment was an abyssal, and Breche Nappes; (4) the Piedmont-Ligurian Ocean including deep-sea fan. The dominant palaeocurrent trend is trom west to 11 the Gumigel Flysch and Dranses Nappes; and (5) the South east (Wildi 1985). The congiomerate elasts are composed of 20% Alpine margin with the Simme Nappe. The orogenie faeies of metamorphic, 50% magmatic and 30% sedimentary rocks with the Pre-Alps (i.e. flysch) were first deposited during the Cretac- two dominant populations: (I) tonalite, quartzite, and dolomi- 1I eaus, extending to Middle-Late Eocene times. Olistostromes and crites () with various other Mesozoic and basement rocks; melange formations, which are related to tectonic phases, (2) granite, granodiorites and cherts, together with other sedi- I! constitute chaotic units which have been tenned 'wildflysch'. mentary, metamorphic and crystaUine rocks. The basement is of ,I Same of these important nappe systems are presented below. South Alpine origin, the Mesozoic elasts were derived from L : Penninie units C==:J Austroalpine units ~ Northern Caleareous Alps The Ultrahelvelic nappe. (Lutetian-Bartonian) occur in platforms to deep basins situated in the South. and Austro- 11 tectonically complex units, together with Triassie to Laie Eocene Alpine units. The heavy mineral association comprises gamet, •• Helvetie units __ outcrops of the Gosau Group fonnations. These units oecur on and between the Helvetic apatites and staurolite (Wildi 1985). Several bentonite layers 1I nappes, between the Niesen and Wildhorn nappes, and between (Winkler et a/. 1985) have their acme in the Late Maastrichtian the Gumigel Nappe and the sub-Alpine Molasse. The Meilleret and the Early Eocene. +~:~:+:~:~:~:~:~: Flysch (Homewood 1974) is composed of pelitic and arenitic The Wägital Flysch is recognized in central and eastem 11: Jura Molasse ~ + + : + ~B6H{MIÄN : + turbidites, which are cut by caarse clastics. Thc successions Switzerland. 1t is very similar to the Gumigel Flysch, and 4. : + : MASSIF : + : terminate with microbreccias and conglomerates containing probably represented the geographie transition from the Gumi- 3Iii1,;~.tl Plateau Molasse ++:::::::: abundant shallow-marine fauna (algae, foraminifera, bryozoans gel-Schlieren area to the Rhenodanubian Flysch Unit (Trümpy 2~ Subalpine Molasse s.1. + .•. ++++ and corals). The Höchst Flysch (Ferazzini 1981) contains thick- 1980). li + + bedded coarse arenites and conglomerates. According to benthic Helvetie Paleogene and planktonic foraminifera as weil as nannofossils, the age of From flysch to wildjfysch and to fore/and basin sedimentation (only Switzerland) these deposits is Middle to Late Eocene. The conglomerates are Until the 1980s, many geologists equated the terms 'flysch' and 1. composed of elasts derived from the Variscan basement and thc 'turbidites'. Therefore, 'flysch' was used for each turbiditic unit Triassic-Cretaceous cover. Thc heavy mineral association COffi- found in the perl-Alpine realm. Thus, several sedimentary units prises ziecon, tourmaline, barite and TiOz. Tbc depositional studied in the He1vetic nappes and the sub-Alpine area have been environment was a moderately deep-water environnement, with a m;med according to this phi10sophy, as for example the 'North tectonically active source in the south, and a short transport Helvetic Flysch' (with the weil known locality of Engi, rich in distance. 6sh remains) or the 'Subalpine Flysch'. Incorporating the ,I D Basement Tbe Niesen Nappe is essentially of Maastrichtian age, with a geodyoamic controJ between the earlier and later stages of the ~. ~ Alpine thrust Lutetian upper part (Chesselbach Flysch; Ackermann 1986). This Alpine Orogeny, Homewood & Lateltin (1988) published an unit is thrust directly over the Ultfahelvetic Unit and is overlain exhaustive review of these units and placed them into a molasse I by a melange (zone submediane; Weidmann et a/. 1976). The (foreland~basin style sedimentation) geodynamic context, with Chesselbach Flysch is composed of arenitic turbidites and shales, the erection of the Taveyannaz and Val d'Illiez formations ,I with north-south palaeocurrents. Its maximum thickness reaches replacing the North Helvetic Flysch and the Subalpine Flysch, o km 100 200 m. The top of this unit is dated as Middle Eocene by benthic respective1y. The Val d'IlIiez Formation passes upward to the foraminifera. Deposited in a deep-marine environment, this liUoral faeies of the Lower Marine Molasse. Thus, the original I' flysch contains a heavy mineral association composed of tounna- conception of the Lower Marine Molasse extended to the Val I, ~ line, zircon, Ti02 and apatite. d'Illiez and Taveyannaz formations. {~ B Tbe Medianes nappe. are of ?Early to Middle or Late Eocene age (NP15 is recorded), probably even younger (Caron et a/ Rhenodanubian Flysch Unit (M. W.R.) 1980). This flysch is in stratigraphie continuity with the hemi- Fig. 17.13. Geology of (A) the Eastem Alps and adjacent areas and (8) the western part of the North Alpine Foreland Basin and the Swiss part of the 11 pelagic marls of the Couches Rouges Group (Palaeocene-Middle Western Alps. The Rhenodanubian Flysch Unit (RFU) is part of the Alpine- Eocene; Guillaurne 1986). It is highly deformed and commonly Carpathian Foreland and received its name from the equivalent I:: assoeiated with (and covered by) chaotic wildflysch deposits occurrences in the Swiss Western Alps. The RFU fonus a narrow 11 thrusting of the Penninic nappes ooto the European Foreland ',d The term 'flysch' was defined in Switzerland as a rock (flysch :i lentilles de Couches rouges). The heavy minerals are zone along the northem front of the Eastem Alps (Fig. 17.13). marked the end of the deep-marine clastic sedimentation and the stratigraphie unit in the Alpine front ranges (Studer 1827). From domina ted by gamet, zircon, tourmaline and Ti02. With a length of 520 km it strikes in a west-east direction from creation of the North Alpine Foreland Basin. Increased subsi- a geodynamic point of view, the formation of

Palaeogeography In Salzburg, the Palaeocene-Eoeene boundary interval is Graben (URG) (perhaps during NP23; see Berger 1996; Kuhle- sidenee leading to the ereation of Ibe foreland basin; (2) the During Ibe Palaeogene, the Northern Calcareous Alps (NCA) present within the Anthering Formation (NP9/P6 to NPll; Egger mann & Kempf 2002; Diem 1986; Berger 1995; Picot 2002). A Lower Freshwater Molasse (= 'Untere Süsswassermolasse', ;'I! were part of the Austro-Alpine Micropiate (for summary Faupl 1995). Egger cl al. (1997) subdivided the Anthering Formation marine eonneetion between the URG and the NAFB was only USM) is eomposed of freshwater and rare braekish sediments; 11I & Wagreich 2000; Wagreich 200 I; see also Froitzheim cl al. into mud turbidites, hemipelagites and bentonites. The mud possible via the central and eastern parts of the Swiss Foreland (3) the Upper Marine Molasse ('Obere Meeresmolasse', OMM) 2008) situated between the European Plate to Ibe north and Ibe turbidites are dominated by silty marls and marls, while sand- Basin, since its western part was covered by fluviatile sediments represents general marine sedimentation occurring in the entire I to the south (Channel cf al. 1992). The RFV was stones and sillstones typieal of the Altlengbach Formation are (Berger 1996) while in its eastem part (Bavaria), open marine basin; and (4) the Upper Freshwater Molasse (= 'Obere Süsswas- 1 part of the Alpine Foredeep to the north of the NCA. Siope subordinate. Turbidite beds are up to 2 m thiek. Hemipelagie conditions oeeurred. Following a regression during the Early sennolasse', OSM) represents freshwater sedimentation extend- deposits of the NCA Gosau Group formed Ibe southern margin daystones are usually bioturbated, eontain abundant agglutinated Chattian, fluvial sedimentation prevailed in the Swiss part of the ing to the Tortonian. The NAFB is also traditionally subdivided of Ibe RFV (Wagreich 2001; Trautwein cl al. 2001). Ta the foraminifera, and have relatively high organie carbon content. In NAFB. Alluvial eonglomeratie fans, derived from Ibe Alps, were into a Sub-Alpine (thrusted and folded units, originally deposited north, it was bordered by Ibe Ultrahelvetic Unit. The RFU was contrast to the turbidites, the hemipelagic daystones generally drained by a SW-NE orientated fluviatile system referred to as further to the south) and a 'Plateau' or 'Foreland' molasse, which part of the Northern Alpine Foredeep and was formed from lack planktonic organisms, benthie foraminifera and- bioturbation. the 'Genferseesehüttung'. The fluvial drainage joined the marine is relatively autoehlbonous. The distal part of Ibe Swiss NAFB is eroded material of the rising Alpine mountain chain. In this These are, therefore, interpreted as having formed in an oxygen- development still present in Bavaria. Part of this system eon- generally called 'Jura Molasse', representing the connection with respect, it was functionally replaced by the North Alpine Fore- deficient environment. Several bentonite layers were found in the tinued into the southern URG through the Jura Molasse, as the Upper Rhine Graben. 11' land Basin during the Oligocene and Neogene. The palaeogeo- type area of the Anthering Formation and were interpreted as evidenced by the heavy minerals of the 'Molasse Alsaeienne' In the Sub-Alpine Molasse: the UMM deposits eomprise the 1, graphie origin of the RFV as part of the Valais palaeogeographic volcanie ashes. Egger cl al. (1997) suggested a short perioLower Austria (Egger the Molasse Basin - was part of the Alpine-Carpathian Foredeep Equivalent sediments are unknown for the western part of the some of them dated by mammals (Engesser & Mödden 1997; 1995). Overviews on the tectonies, stratigraphy and palaeogeo- forming a west-east trending basin in front of the prograding Swiss NAFB, where 2000 m of Mioeene sediments were probably Hooker & Weidmann 2000). Few laeustrine deposits of Rupelian graphy have been published by Egger (1992, 1995), Oberhauser nappes of the Alpine orogenie wedge. lt can be traced from the eroded during the Plio-Pleistoeene (Kuhlemann & Kempf 2002). age are known from the Swiss Plateau Molasse (Caleaires (1995), Wagreieh & Marsehalko (1995), Adamova & Sehnahl Rhöne Hasin in the west via Switzerland and Bavaria to Austria Only relicts of marine middle Miocene deposits oceur in the inferieurs), whieh are generally dated by charophytes (Berger (1999) and Faupl & Wagreieh (2000). Aceording to these papers, (Fig. 17.13). western Jura Molasse (NN4-NN5; see Kälin cf al. 2001). During 1992). In the Early Chattian, fluviatile sediments (Untere Bunte the stratigraphie and sedimentary development of the area ean be the Serravallian, fluviatile sedimentation continued, with an Mergel) were deposited in the entire foreland basin. During the subdivided into various stages (see below). Palaeogeography important clastic souree located in the Vosges and Black Forest Middle and Late Chattian, lacustrine and brackish limestones, The Maastriehtian (CC25) to Palaeoeene (NP9) Altlengbaeh Several palaeogeographic reconstructions of the NAFB have been massifs, confirming continued uplift during this time. and gypsiferous marls oecur. In the NE distal part of Formation is known from both the central (Salzburg) and the published (Berger 1996; Sissingh 1998; Sehlunegger & Pfiffner The Tortonian drainage pattern is very difficult to reconstruct the basin, sedimentation probably did not begin before the western (Wienerwald, Lower Austria) parts of the RFU (Egger 2001; Kuhlemann & Kempf 2002; Beeker & Berger 2004; in Switzerland; a general west-east drainage of the Swiss NAFB middle Chattian (Müller cl al. 2002; Schlunegger & Pfitfner 1995). It extends from the Campanian-Maastrichtian boundary Berger cl al. 2005b). During the Lutetian, the sea was loeated in has been proposed (Giamboni cl al. 2004; Kohlemann and 2001). All mentioned units are relatively well datedby mammals, through to the uppermost Palaeoeene. The Palaeoeene parts of the area of north Italy and southern Switzerland, with its northern Kempf 2002; Liniger 1966; Petit cl al. 1996; Schlunegger cl al. charophytes, otolithes and magnetostratigraphy; see Berger et al. the Altlengbach Formation are restricted to the Acharting shoreline about 70 km south of Bem (Sissingh 1998). The Alpine 1998). This pattern is based on the uplift of the western and 2005a). Member, the deposition of which began during the Maastrichtian. front was probably situated c. 300 km south of its presen! eentral parts of the NAFB in eonjunetion with the folding of the In Germany, the UMM is represented by Ibe distal parts of The Aeharting Member is eharaeterized by rhythmie alternations position (Dezes el al. 2004). Most of the area of present-day Jura Mountains. In Gennany, fluviatile sedimentation persisted the Tonmergelschichten and Bausteinschichten (Rupelian). of fine-grained sandstones to siltstones and turbiditic mudstones. Switzerland was affeeted by erosion (marked by loeal siderolithie until the Early Tortonian (11 Ma; Kuhleman & Kempf 2002). During the Chattian, a freshwater to marine transition oe. Tbe sand- and siltstones have a high carbonate content and deposits). eurred (Doppler el al 2000; Sehwerd cf al 1996). A fluviatile inelude foraminifers and eoralline algal fragments. As revealed Subsequently, the sea transgraded along the northem front of Sedimentary and stratigraphie development facies characterizes the Aquitanian deposits of the Swiss from heavy minerals (Egger 1990), palaeoeurrents from the east Ibe Alps. During the Late Rupelian, the Paratethys regressed The NAFB is traditionally subdivided into four depositional Plateau Molasse (e.g. Molasse Grise de Lausanne, Obere prevailed up to the early Palaeoeene, changing to a westerly towards the east. It is most likely that during this time a marine groups (Fig. 17.9): (I) the Lower Marine Molasse (= 'Vntere Bunte Mergel, Granitisehe Molasse; Berger 1985; Keller el al. direetion during the later Palaeocene. eonneetion existed between the NAFB and the Upper Rhine Meeresmolasse', UMM) eommenced with the increase of sub- 1990). A marine transgression ftooded Ibe North Alpine I

1056 I, M. W. RASSER, M. HARZHAUSER Er AL. i~ PALAEOGENE AND NEOGENE 1057 Foreland Basin during the late Aquitanian (MN2) and Burdi- Bohemian Massif and by the overriding Rhenodanubian Flysch Puchkirchen Formation was deposited in a deep marine channel, show evidence of strong tidal influenee, ubiquitous reworking, galian. Its typical deposits comprise the OMM (Berger 1985; I: Unit and Helvetic Unit of the Alpine-Carpathian tbrust front in eomprising slumps, conglomeratie debris flows and turbidites, and submarine erosion (Faupl & Roetzel 1988). Close to the Homewood & Allen 1981; Keller 1989; Kempf er al. 1997, the south. The width of the c. 300 km long Austrian part of the ~ derived from both slopes of the NAFB (DeRuig 2002). Fre- margin of the Bohemian Massif, reworking of Egerian and 1 1999; Schoepfer 1989; Strunck & Matter 2002). In Germany, NAFB in Lower and Upper Austria ranges from 5 to 50 km. Tbe ~~ quently strong boUom currents reworked the turbidites into Eggenburgian sediments is refteeted in the presence of the a freshwater-marine transition prevailed during the Aquita- .1 present basin is only a narrow remnantof the original basin (Fig. "~~ eontourites (Wagner 1996, 1998). phosphorite-bearing Plesching Formation (Faupl & Roetzel j! nian. Fnllowing reduced sedimentation during the early Burdi- 17.13). ~S Continuous deep-marine sedimentation in the eastem NAFB 1990). In the eastern part of the NAFB, basinal days, silts and galian, the sea invaded the entire basin. In Switzerland, is eontrasted with the deposition of the Lower Freshwater sands of the Robulus Schlier and the so-called Sandstreifensch- marine sediments were confined during the Langhian to the ~,.~~: I Teetonie setting N' Molasse in Vorarlberg (western Austria) and Bavaria during the lier represent Eggenburgian to Ollnangian offshore deposits. In north and NE (Graf 1991); fluviatile sediments associated During the Oligocene, progradation of the Alpine-Carpathian t,' Egerian (see section ahove). Here, braekish environments the Ottnangian, at the margin of the Bohemian Massif, submar- I with alluvial fans are present in the south (OSM) and nappe system resulted in the passive margin of the Bohemian ! fonned in the Late Oligocene and overlie the shaHow-marine ine debris flows oceur (Mauer Formation). These interdigitate I, persisted until the Serravallian (MN7, ?MN8) (Bolliger 1992; Massif being transformed into a foreland molasse trough. In the deposits of the Baustein Beds. A westward prograding limnic- with tidal channel sands of the Prinzersdorf Formation (Kren- d Kälin 1993; Kälin & Kempf 2002; Kempf er a/. 1999). The south, emplacement of the Helvetic and Rhenodanunian Flysch '~: fluvial facies of the 'Lower Coloured Molasse' developed and mayr 2003a, b). I OSM is very weil represented in Germany, with conglomer- units formed the southern slope of the basin. During the Late this grades into the braekish swampy environments of the In the Late Ollnangian, the presenee of the widespread ales altemating with fluvial and lacustrine sediments. The Oligocene, these units became integrated into the Alpine tbrust 'Lower Cyrena beds'. A short-lived marine ingression (Prom- Rzehakia ('Oncophora') beds reflects a major regression. These I meteorite of the Nördlinger Ries impacted during the Early front. The Calcareous Alps formed the shelf on which debris berg Beds) is followed by the limnic-fluvial eonditions of the beds yield an endemie moHuse fauna with bivalves such as Serravallian (14.6 Ma). In Switzerland, no Upper Serravallian, from the Central Alps accumulated. In the north a fault system 'if 'Upper Coloured Molasse' in the latest Oligocene and early Rzehakia and Limnopagelia, which thrived in shallow brackish Tortonian or Messinian sediments are recorded. However, of conjugate NW -SE and NE-SW trending faults in the south- Early Mioeene. In the Early Miocene (Eggenburgian regional lakes. In the western NAFB, a pronounced phase of erosion took ! several authors suggested that an additional 700 m and up to em part of the Bohemian Massif resulted in the formation of a age) marine sedimentation was re-established, as evideneed by place up to the latest Early Mioeene. Subsequently, deposition of >2000 m of sediment were deposited in the east and west triangular crystaIline peninsula, which extended far south into the deposition of the shallow marine sediments of the Upper J limnic~fluvial sediments of the Upper FreshwaterMolasse eom- ; Swiss NAFB (see Kuhleman & Kempf 2002). the NAFB, separating the basin in the area ioto western and Marine Molasse. In eastern Austna, however, deep-water sedi- menced. ]ts basal parts comprise lignite-bearing clays, sands and .j The Palaeogene to Neogene Swiss Jura Molasse is pre- eastern parts. Tectonic activity within the thrustsheets and lateral mentation eontinued during the Late Egerian and Eggenburgian, gravels (Trimmelkam and Munderling beds), which are of served in a number of synclines in the Jura Mountains (Picot movements of the basement along the eastern flank of the and is typified by the debris flows, slumps and contourites of Middle Miocene age. After another gap the 'Lignite bearing 2002; Becker 2003). Eocene deposits are represented by Bohemian Massif are still ongoing. the Eggenburgian Hall Group. During the Eggenburgian and Freshwater beds', the Kobernausserwald gravels and the Haus- siderolithic units. Even though it has not been precisely dated, Ollnangian (Early Miocene), deltaie gravels and sands were ruck gravels were deposited in limnie-fluvial environments a Lutetian, Bartonian and Priabonian age is suggested based Sedimentary and stratigraphie deve/opment transported from the south into the NAFB, forming the duringthe Late Miocene. on correlation with ether siderolithic occurrences. The Swiss Tbe depositional history and stratigraphie development of the conglomerates of the Buchberg and Wachtberg, today partly In the eastern part of the NAFB shallow-marine conditions Jura Molasse was subdivided by Berger el a/. (2005a) into live eastern NAFB differs considerably from that of its western part located in the imbricated nappes of the NAFB. also prevailed in late Early Miocene times and are represented different areas. (I) SW Jura Molasse (Valserine, Joux, Auber- (see above) and may be subdivided into several stages. The Shallow-marine deposits are mostly absent in the western, by the pelitie and sandy sediments of the Laa and Nory Pferov 500, Travers, Val de Ruz): deposits of the Lower Marine oldest Cenozoic deposits in the NAFB are Upper Eocene fluvial Upper Auslrian part of the NAFB due to both submarine and formations (Roetzel 2003). In the early Middle Miocene, similar Molasse are absent. The USM is represented by the Chattian and shallow-marine sandstones, shales and carbonates of the later Alpine erosion. Erosional reliets of the Eggenburgian are sediments were deposited (Grund and Gaindorf formations). Calcaires inferieurs and the Aquitanian Calcaires de La Chaux Perwang Group (Buchholz 1989; Rasser 2000) (Fig. 17.9). As a best preserved along the eastern margin of the Bohemian Massif Sandy-gravelly and shelly intercalations within the predominantly (MN2b). OMM sediments are preserved as weil, but the OSM result of subduction of the Europeao plate beneath the Peri- in Lower Austna. There, the Lower Eggenburgian suecessions pelitic Grund Formation are interpreted as storm-induced event is absent. (2) NW Jura Molasse (Verrieres, Pont de Martel, Adriatic plate and the weight of the advancing Alpine nappe reflect a stepwise landward shift of the palaeoshoreline (Mandic deposits (Roetzel & Pervesler 2004). On topographie highs Locle-Chaux de Fonds): only deposits of the OMM and of the system, the downwarping of the foreland erust accelerated during & Steininger 2003). The marine sediments onlapped either eorallinacean limestone developed ( Formation). To the OSM are present; the latter is represented by the farnous the Early Oligocene and the NAFB subsided rapidly into a deep directly onto arelief formed by crystalline rocks of the SE south these sediments are correlated with submarine deltaic Oeningian facies. (3) Central-South Jura Molasse (SI. Imier, pelagic area. 81ack shales were deposited in Switzerland, Bavaria Bohemian Massif, as shown by the Fels Formation, or prograded eonglomerates (Hollenburg-Karlstetten Formation). Foraminiferal Pery-ReucheneUe, Tramelan-Tavannes, Balstahl, Moutier): thick and western Austria (= Fischschiefer). Towards the south, these towards the NW into the estuarine-fiuvial systems of the St. data document an Early Badenian age (= Langhian) for these units of fluviatile and lacustrine sediments accumulated during shales graded into the deep-marine deposits of the Deutenhausen Marein~Freischling Formation.Initial brackish-estuarinebiotopes deposits and suggest that marine deposition in the eastem NAFB the Oligocene (Calcaires inferieurs, Molasse alsacienne, Cal- Fonnation. An upwelling current system might have been estab~ of the Mold Formation were gradually replaced by fully marine continued until c. 14.5 Ma, when Middle Miocene uplift eaused caires delemontiens). After a gap during the Aquitanian, the lished during the Late Eoeene, affecting deposition along the conditions, typilied by the sandy Loibersdorf Formation, which the sea to retreat. OMM commenced with classic tidal sandstones. The OSM is northern slope throughout the Early Oligocene, as suggested by includes the historical holostratotype of the Eggenburgian stage The very last marine ingression into the already dry basin took essentially lacustrine (Oeningian facies) and conglomeratic. (4) the presence of nannoplankton ooze. at Loibersdorf (Steininger 1971). Continuing transgression onto place during the Early Sarmatian (= late SerravaLlian). The Central-North Jura Molasse (Soulce, Delemont, Laufen, Porren- The Southem Bohemian Massif acted as the northem margin the Bohemian Massif in the late Eggenburgian led to the marine Sarmatian is eonfined to a rather narrow,c. 40 km long truy, Liesberg): the UMM is represented by marine maris dated of the NAFB. During the Oligoeene it was drained towards the deposition of the moHusc-riehnearshoresands of the Burgschlei- west-east trending trough extending from the Bohemian Massif !! from NP22 to NP25, alternating with Oligocene freshwater south and east by fluvial systems, represented by the sands and nitz and Gaudemdorf formations. Following a prominent regres- in the west to the Vienna Basin in the east. The location was deposits (e.g. conglomerates, Molasse Alsacienne, Calcaires gravels of the Freistadt-Kefermarkt Beds and the SI. Marein- sional phase, the sandy bryozoan limestones of the Zogelsdorf controlIed by an older incised vaLley which beeame flooded f delemontiens). A sedimentary gap during the Aquitanian is Freischling Formation. During the Early Oligoeene (Kiscellian Formationwere deposited at the beginning of the new OUnangian duringthe Early Sarmatian.Clays, silts and sands were deposited 1I followed by the sedimentation of the OMM and lacustrine regional stage) vast mudflats and lagoonal embayments devel- transgre~sional cycle. Towards the east these shallow-water suggesting the formation of extended sandy to muddy tidal flats. OSM deposits. (5) East Jura Molasse (Mummliswil, WaIden- oped along the eoast formed by the Bohemian Massif (e.g. deposits interfinger with the offshore clays of the The dating of the Formation as Early Sarmatian is 11 burg): essentially USM and OMM are developed. OSM is only mol1use~rich pelites, lignites of the Pie lach Fonnation; Harzhau- Formation. During the Ottnangian, due to further westward based on the oeeurrence of several species of the endemic I ~ part1y preserved (Glimmersand). ser & Mandie 2001). Sandy sediments of the coeval and transgression of the sea ooto the Bohemian Massif, these off. gastropod Mohrenslernia (Kowalke & Harzhauser 2004) and rare 11 The Pliocene is principally represented by conglomerates overlying Linz-MeJk Formation refleet the marine transgression share clays were deposited above the nearshore sediments. E/phidium reginum (Papp el a/. 1974). Upper Sarmatian deposits (Ällere Deckenscholler, Graf 1993) in the NE of Switzerland. during the Oligoeene (Kiseellian and Egerian regional stages). Towardsthe west a transitionof the marine clays to the braekish are absent from the NAFB due to the final retreat of the ;, The only dated Pliocene deposits in this area are the karstie These comprise lagoon, rocky shore, sandy shoreface and tide- clays of the Formation ean be noted. In marginal ParatethysSea from that area. /,. lilling of the Vue des Alpes (MNI5; Bolliger el al. 1993), and influenced open-shelf environments. The interruption of this areas brackish-estuarinesediments with eoal seams were depos- The early Late Miocene of the NAFB in Lower Austria is the Höhere Deckenschotter from Irehels (MNI7, Bolliger el a/. transgression by the marked Lower Egerian regression is ited ( Formation) during the Ottnangian and were characterizedby a huge fluvial system often referred to as the li. 1996). In Germany, Pliocene sediments have been reported from evidenced by erosion surfaces, redeposition and intercaJationsof followed by marine nearshore sands (Riegersburg Formation). In I'; Palaeo-Danube. The corresponding deposits of the - the 'Hochflächenscholler' and the 'Hochschotter' (e.g. Schwä- lagoonal dark coaly pelites (Roetzel 1983). several of these marginalOttnangianunits, acidie volcaniclastics, Mistelbach Formation indieate a dominant gravel-rich fluvial bische Alb, NaabtaI). Along the western part of the northern margin of the NAFB, derived from the Carpatho-Pannonianregion, are present (Nehy- depositional environment, which grades into a braid-deltaenvir- ;,: the Oligocene shallow-water deposits interfinger towards the ba & Roetzel 1999). onment towards the east at the entrance to the Vienna Basin i~, Norlh Alpine Foreland Basin: eastern part (MoB., R.R.) south with offshore pelites of the Ebelsberg and Eferding In the Late Eggenburgian and Ottnangian the reopening of the (Nehyba & Roetzel 2004). The mosUy coarse-grained clastic ~/" formations. Due to the progressive Upper Oligoeene transgres~ NAFB towards the Rhöne Basin in the west led to a distinet ftuvial to deltaic sediments, extend, on the surface, in a WSW- The Austrian part of the North Alpine Foreland Basin (NAFB) is sion, these offshore pelites overlap the shallow-water deposits to change in the depositional environments. Consequently, in the ENE direetion from Krems in the NAFB towards the Steinberg il bordered to the north by the passive margin of the Variscan the north. Along the southern slope or the NAFB, the Egerian western part of the NAFB sands and sills or the Innviertel Group Fault in the Vienna Basin over a distance of >86 km. The width Ji ~i 1058 M. W RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1059 of this sedimeot body is between 3 and 14 km, and up to 20 km Carpathian Palaeogene' deep-water trough from (Wa- >- .c t:: E t:: :c Qi E w 0 Q)~ 0 ca E .~ TI .c i .>< .0 .c " ~ ca ~ .c," ca the south, a marine seaway from the 'Central Alpine' Gosau Basin , ~ .~ . " .c ~ :c .0 ~ff ~ ~ !; oe! ,".0 ;1l ca 0; 0 0 t:: ! e !:. s'" ca cn i!! Cl >- ~ Q) into the Southem Alps can be assumed, due to the occurrence of w U> ~ U> .9~ " " .c LL Qi '2 E Austro-Alpine Gosau basins (M.w.) cn :, '0 N (5 " ::;:" ca 0 :e1 Palaeocene-Eocene deep-water strata, in, for example, the Lom- " U> ~ ~ 0- U> ~ " .~ 0- Palaeogene strata in the Austm-Alpine parts of the Eastem Alps 35 0 'ö ca bardian Basin in northem Italy, where an Early Palaeocene hiatus U Ul PRIABONIAN 0 ~ (Nortliem Calcareous Alps (NCA) and Central-Alpine Zone ! ::;: :.:: is followed by the deposition of turbidites and marlstones of Z ~ (CAZ)) (Fig. 17.13) are partly continuous from the Upper Palaeocene-Middle Eocene age (Bersezio et 01. 1993). BARTONIAN Cretaceous successions. Following the work of Kühn (1930), - Ul " w ~ Palaeogene-age strata have been recognized from the Gosau Sedimentary and stratigraphie development Cl z g 0 w • Group of the NCA. Most of the NCA Palaeogene deposits are Formally defined lithostratigraphic subdivisions of Palaeogene 0 "0 lUTETIAN deep-marine (Wagreich & Faupl 1994; Wagreich 2001); shallow- deposits of the Austro-Alpine units have been established in the " W N Ul water sediments have only been reported from the southeastern Gosau area (Fig. 17.15) (based on Weigel (1937) and Kollmann « part of the NCA (Kambühel and Hochschwab areas; Tragelehn in Plöchinger (1982): Nierental Formation, Zwieselalm Forma- 50 0 ...• 1996), and from the CAZ (Krappfeld area; Wilkens 1989; Rasser tion), in the Gießhübl syncline (Gießhübl Formation; Plöchinger YPRESIAN 1994). Shallow-water carbonates are also found as olistoliths in 1964; Wessely 1974; Sauer 1980) and in the Grünbach-Neue « ! 55 deep-water strata (Lein 1982; Moussavian 1984). z Q. w Welt area (Zweiersdorf Formation; Plöchinger 1961). Paleocene THANETIAN Outcrops of the Palaeogene Gosau Group comprise only shallow-water carbonates of the Kambühel Formation, as defined ~ ~ erosional remnants of the widespread Palaeogene cover of the Ul " , SElANDlAN by Tollmann (1976), were investigated by Tragelehn (1996) who 50 0 NCA and the CAZ as evidenced by the widespread redeposition distinguished two members (SI. Lorenzen Member, Ragglitz w IKa of Palaeogene sediments into younger formations (e.g. Hagn OANIAN Member). Biostratigraphie data for the deep-water successions U ~ "~ Zwe 65 .. 1981). The Palaeogene deposits of the Gosau Group record the are mainly based on planktonic foraminifera and calcareous II ci ,..: geodynamic evolution of the Eastem Alpine orogenie wedge nannoplankton (e.g. Hillebrandt 1962; WiIle-Janoschek 1966; U> Ul W ll<: MAASTRIj:HTIAN fram a phase of deep-water sedimentation to renewed thrusting, :E ~ Wille 1968; Kollmann 1964; Wagreich & Krenmayr 1993; 70 U which culminated in the meso-Alpine Orogeny related to com- Hradeckä et 01. 1999; Egger et 01. 2004). ra I rnl pression between the European and the African-Adriatic plates The Palaeogene in the CAZ is subdivided into the Holzer during the Palaeogene (e.g. Dewey et 01. 1989; see also i Formation (Paleocene), the Siltenberg Formation (YpresianiLute- IIII shallow-water sHiciciastics ~ coarse debrites turbidites below CCO Froitzheim et 01. 2008). tian) and the Dobranberg Formation (Lutetian; Wilkens 1991; o SE Rasser (994) which includes several members. ~ shallow-watar limestones hamipalagites a turbidites Poloeogeography Four generalized facies associations have been distinguished The Palaeogene deposits of the Gosau Group of the NCA record within the Palaeogene part of the Gosau Group of the NCA Fig.17.1S. Lithofacies, lithostratigraphy and chronostratigraphic correlation ofmain successions of Palaeogene sediments ofthe Gosau Group ofthe deep.water sedimentation on top of the early orogenie wedge of (Wagreich 200 I): siliciclastic and mixed siliciclastic/carbonate Nortbem Calcareous Alps and tbe Palaeogene of the Central Alpine Zone. Abbreviations: Bru, Brunnbach Fonnation; Doh, Dobranberg Fonnation; Gie, the Eastem Alps, which evolved during Early to early Late turbidites, hemipelagites and pelagites, debrites, and shallow- GießhübJ Fonnation; Hol, Holzer Fonnation; Kam, Kambübel Formation; Nie, Nierental FOImation; übe, überaudorf Fonnation; Rot, Rotkopf Formation; Cretaceous Alpine deformation (Faupl & Wagreich 2000) (Fig. water carbonates of reef, lagoonal and forereef facies. The Sit, Sittenberg Formation; Wör, Wörschachberg Fonnation; Zwe, Zweiersdorf Fonnation; Zwi, Zwieselalm Formation. 17.14). Palaeogeographic reconstructions indicate a generally gravity-ftow-dominated facies association suggests deposition on northward-deepening slape. disseeted by depoeentres and structur- small submarine fans. Proximal fan areas are characterized by successions are known from Gosau, Gams and the Gießhübl Early Palaeocene (Wagreich & Krenmayr 1993; Krenmayr 1996; al highs forming slope basins along an active continental margin. channels filled with conglomerates and pebbly sandstones, Syneline. Palaeocurrent data point to southern source areas for the Egger et 01. 2004). South of Gams, in the Hochschwab area, To the south of the NCA, exhumation of metamorphic complexes whereas elassical turbidites indieate interchannel and distal fan turbidites (Faupl 1983), although basin-parallel, east-west trend- shallow-water carbonates and limestone olistoliths are present. of the Austro-Alpine basement formed a rising source area for depositional environments. ing flows are also recorded. Turbiditic sandstones ean be classified These remnants of shallow-water facies (Kambühel Formation) Palaeogene siliciclastics. This rising hinterland separated the During the Early Palaeoeene, turbidites and hemipelagites as lithic arenites and display mixing of silicielastic (mainly low- depositional area of the Gosau Group of the NCA from southern dominated the Gosau Group of the NCA, from the in the eontinue up to the eastern margin of the Alps (Kambühel near to medium-grade metamorphic elasts) and carbonate debris. CAZ basins such as the Krappfeld (Neubauer et 01. 1995; west (Multekopf area, Ortner 1994) to the Gießhübl Syncline in Ternitz). Palaeocene reef carbonates comprise baffiestonesl Carbonate clasts include bolh extracIasts from the underlying Wagreich & Siegl-Farkas 1999). Palaeogene deep-water sedi- the east (Sauer 1980). Several localities (Gosau, Gams, Laltenge- boundstoneslrudstones with abundant corallinacean and dasycla- strata of the NCA, and bioclasts from a contemporaneous ments, comparable to the Gosau Group, are also known from the birge, Gießhübl Syncline) displaya conformable succession of dacean algae and corals. Forereef facies include packstones rich carbonate shelf to the south. Ar/Ar dating of micas from pebbles in corallinacean algae. Third-order transgression-regression eastward continuation of the NCA into the Western Carpathians Maastrichtian to Palaeocene deep-water sediments, without major suggests significant erosion of pre-Alpine, Permian metamorphic (Wagreich & Marschalko 1995). Palaeogene deposition within the facies changes around the KlPg boundary (Lahodynsky 1988; eycles, marked by emersion horizons, have been reported by crystalline units of the Austro-Alpine basement to the south Tragelehn (1996). Reef growth stopped during the Middle CAZ can be interpreted as a continuation of the 'Central Krenmayr 1999). Several hundred metres of thick turbiditic (Frank et 01. 1998). Hemipelagites and pelagites (Nierental Thanetian, probably due to a sea-level fall and tectonism sin Formation; Krenmayr 1996, 1999) occur either as packages (Tragelehn 1996). several tens to hundreds of metres thick or as thin intervals within During the Thanetian to Lower Ypresian coarse debrites, Northerl' p.,lpineforeland Ba turbidite-dominated suecessions. Thin. to medium-bedded marly including olistoliths of Palaeocene shallow-water carbonates, are limestones, marls and shales with a generally high degree of widespread in the NCA. They occur either as debrite layers bioturbation (Zoophycus ichnofacies) predominate. The carbonate several metre thick associated with mixed silicielastic-carbonate content consists mainly of calcareous nannoplankton and plank- turbiditic successions (e.g. Gießhübl Formation), or as isolated tonic foraminifera. Intercalations of thin sandstone and debrite breccias ineluding olistoliths, up to 50 m in diameter, in the beds or slump deposits are common (e.g. Krenmayr 1999; Hochschwab area. Olistostromes, including metamorphic elasts, Wagreich & Krenmayr 2005). were reported from the lower '!lerdian' (PS) of the Salzburg- Within the Weyer Are area, carbonate-feee hemipelagic elays Reichenhall area and Ihe KaisergebirgelTyrol (Moussavian et al. within the turbiditic succession of the Brunnbach Formation 1990). The southern carbonate platform was probably dissected 9 k!TI turbidites below CCD 19°. record deposition below the loeal carbonate eompensation depth by canyons, enabling the siliciclastics to bypass the carbonate ~ shallow-water limestones ~ hemipelagites [illill] turbidites (CCO) (Faupl 1983). This deep-water basin received material environment. from two sources, building a sand-rich and a sand-poor submar- The Dccurrence of bentonites, originating from airfall, in the ine fan (Faupl 1983). To the south and SE of this deep basin, the Upper Palaeocene (NPIO) of Salzburg and Gams (Egger et 01. Fig. 17.14. Palaeogeographic sketch map for the Early Palaeocene (nannoplankton zones NPl-4) ofthe Northern Calcareous Alps with the main Gosau Basins. Arrows indicate palaeocurrent directions. Gosau Group of Gams, deposited in a slope basin-trench-slope 1996, 2004) suggest that there was a close connection of the basin setting, records deposition in bathyal depths during the depositional areas of the Gosau Group and parts of the Rhenoda- 1060 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1061 nubian Flysch, where similar bentonites of basaltic composition internal boundary of the Outer Carpathian Flysch Belt; sediments are known (Egger et al. 2000). of the Magura Unit form the northem margin of the basin. The In the CAZ a hiatus marks the top of the Late Maastrichtian to basement of the basin is formed by Alpine-Carpathian nappes. J Early Palaeocene sequence. This is followed by a (Late?) The maximum thickness of the Neogene basin /ill is 5500 m. ~ Palaeocene succession of terrestrial conglomerates, sandstones Since the basin is subdivided by a morphological high, the and clays including coals (Holzer Formation; Wilkens 1991). Spannberg Ridge, into a northern and a southem part, marine .... Eocene deposits of the Gosau Grollp are known from Gams sedimentation was restricted to the north (north of the Danube) ',(', E (Kollmann 1964; Egger & Wagreich 200 I), , the during the Early Mioeene and extended into the south only ~ . .:< Schom area near Gosau and Abtenau (Wille 1968), the Salzburg- ~I o during the Middle and Late Mioeene. Due to the eomplex fault ~ o Untersberg area (Hillebrandt 1962, 1981), and the Lower Inn system the basin was intemally subdivided into aseries of horst - :'1 tion are eharacterized by intercalations of alveoJinid and nummu- m. cn "li Moravian Central Depression. Synrift extension in the northem 'j: ~ CIl ~ 1y Cl I litid limestones with loeal intercalations of orthophragminid part of the Vienna Basin was enhanced by active elongation of the Q. - foraminifera (Wilkens 1989, 1991; Hillebrandt 1993). The ;}l , ! Western Carpathian Orogen during the Sarmatian due to subdue- :l 1 nummulitid foraminifera are Early Eoeene in age (Hillebrandt tion in front of the Eastern Carpathians. The Late Mioeene , 1993). Comlline algae and encrusting foraminifern dominate the ~: represents the post-rift stage in basin evolution. In the Late .:}~ middle part of the succession where they form huge aceumula- Mioeene (Pannonian) and Pliocene, the Vienna Basin was inverted ~ ~ I I tions ofrhodo1iths and acervulinid macroids (Rasser 1994) whieh and subsequently ooly minor amounts of sediment were deposited. •• E i ~: are thought to be Ypresian to Lutetian in age (Wilkens 1989; see Fault-controlled subsidenee in grabens at the eastem margin of ! also Moussavian 1984). ,; !-:'~ ! the basin (Zohor-Plavecky MikuläS and MiUerndorf grabens) 0, ca UJ_. documents a sinistral transtensional regime of this zone, lasting al ;;, J !! Vienna Basin and its satellite basins (M.B., M.K., R.R.) up to recent times, and accompanied by seismic aetivity. c: •• c: ~l '" c: '00 .~ ~j 'e: "Ci) ~ The Vienna Basin covers large parts of eastern Austria (Lower , Sedimentary and stratigraphie development c:o ro'" ro'" Austria, Vienna and ) and extends into the Czeeh j rj The initial phase of Miocene deposition in the present Vienna t: c 2 ~. Republie in the north and the Siovak Republic in the east (Fig. (tJ ro ••• .- Basin (Fig. 17.9) was related to the Eggenburgian transgression £1.'e Q) 3 gfjJ .s 17.16). lt is about 200 km long and 55 km wide, striking roughly "C 0 .0 0 and to the tectonic opening of depocentres in its northem part. c: C .c .- ] SW-NE from (Lower Austria) in the SSW to (tJ C 0 0 Piggyback basin depoeentres developed in the Outer Carpathian Napajedla (Czech Republic) in the NNE. As a c1assic Neogene ~ Flysch Belt zone, while in the Central Western Carpathians ~ 8:. ~ •.. g basin it has been the subject of hundreds of geoscientific studies wrench fault basins opened. Deposition commenced with the ,~ö.~~~~ sinee the early nineteenth century. £: E ~ .~ C cD ,., clays and sands of the fluvial Stnize Formation. The onset of 1 marine transgression is refiected by the boulder-sized Brezova .s Tectonic setting and development ~~-5~~~ conglomerates which pass into fine-grained conglomerates and C'lI(/J>e-:.::c. o The Vienna Basin is a rhombic Neogene-age pull-apart basin. Its - shorefaee sands. Upwards, sandy deposits eontaining a rieh ~ ~ ~ ~ ;. ~ -., SW border is formed topographically by the Eastern Alps and to ~ pectinid fauna are found. Laterally, to the south and east, the oE ~ ~ Q) .S \00 -- ] the NW by the Waschberg and Zdanice units. To the east it is "C 0 0 •.• C Q) Cl coastal facies passes into open-marine conditions marked by the C CD Q) ::J .~ C bordered by the Rosalia, Leitha and Hainburg hills, and the Male .,zZOa.~ ~ upper part of the Luzice Formation. Neritic sands and elays Karpaty Mountains, all four of whieh are part of the Alpine- (= 'Schlier') contain a rich deep-water foraminiferal assemblage, a Carpathian Central Zone. The Pieniny Klippen Belt represents an jD[lllD.~ yielding taxa that tolerated low-oxygen bouom eonditions. The ~ .~"

1062 M. W. RASSER, M. HARZHAUSER ET AL. - PALAEOGENE AND NEOGENE 1063 Eggenburgian-Ottnangian boundary is marked by a relative sea- Slovakia. In the eentral part of the basin, layers of Upper aetivity within the Alpine-Carpathian tbrust belt. This asym- comprising gravels, sands, oolitic sands and marls is typical level fall and reeorded by the basinward progradation of shallow- Badenian corallinacean limestones represent a shallow-marine metrie SSE-NNE orientated basin is c. 20 km long and attains a throughout the basin. Lake Pannon eovered the Eisenstadt- water sandy facies at the base of the OUnangian. In the northem shoal along the Spannberg Ridge that extended for more than maximum width of 7 km, but is strongly narrowedin its northem Basin duringthe Late Miocene, as shown by the presence Vienna Basin, the sandy Stefanov Member (150 m) represents a 150 km' (Kreutzer 1978). This topographie high aeted as a Late extension. A central high separates the southem part (c. 880 m of elayey marls and sands. During the middle Pannonian a small deltaie body entering the basin from the SW during this Badenian platform from wh ich a bird-foot delta spread into the deep) from a shallower northem depocentre (c. 530 m deep). river formed on the' supplying reworkedLower regression. The overlying OUnangian transgression is represented southem basin (Weissenbäck 1996). This delta was supplied with The basin margins are formed in the north by the Waschberg Miocene gravels into the basin. As in the Vienna Basin, the by the silts and silty sands of the upper Luziee Formation, whieh sediments from the eontinental North Alpine Foreland Basin. Unit and towards the south by the Rhenodanubian Flysch Unit. onlaps the slopes of topographie highs. withdrawal of Lake Pannon allowed the establishment of flood- The offshore sediments consist of marine calcareous clays These Alpine-Carpathian nappes are underlain by the autoehtho- plains and swamps during the latest Pannonian (all data from During the subsequent Karpatian a pull-apart basin began to (Studienka Formation). Oxygen-depleted bottom eonditions eom- nous basement fonned mainly by Upper Cretaceous and Jurassie Sehmid et al. 200 I; Kroh el al. 2003). open. Rapid subsidenee and sea-Ievel rise led to the development monly occurred in basinal settings but also on the carbonate units and by the erystalline basement of the Bohemian Massif. of offshore settings in the northem Vienna Basin, as refleeted by platforms (Sehmid el al. 2001). Sedimentation began during the early Mioeene (Eggenburgian) the pelites of the Laa and Laksiry formations. Sedimentation in The Badenian-Sannatian boundary is charaeterized by a and comprised shalIow-marine marls and sands (Ritzendorf Styrian Basin and Neogene intra-Alpine basins (M.H.) the southem part of the basin differed signifieantly, due to the major fall in sea level. Badenian-age corallinacean limestones Formation). The main phase of deposition, however, began in the Although situated along the eastern margin of the Eastem Alps presenee of a topographie barrier formed by the Spannberg were exposed and significant erosion look place along the late Early Mioeene (Karpatian), and is represented by marly silts the Styrian Basin (SB) is a sub-basin of the Pannonian Basin Ridge in the central Vienna Basin. Thus, in the southem Vienna margins of the basin. Renewed transgression in the Early and fine to medium sands (Korneuburg Fonnation). System (Fig. 17.16). The SB, situated in SE Austria, is c. 100 km Basin, sedimentation started during the Early Mioeene with the Sarmatianfilled incised valleys. This transgression is represented A connection to the Paratethyswas only warranted along the long and 60 km wide. lt is bordered in the west, north, and east deposition of the alluvial Bockfliess Formation comprising mainly by calcareous clays, silts, and rare acidie tuffs (HoHe northem basin margin, where the sea extended into the Alpine- by Alpine mountains such as the Koralpe, the G1einalpe and the lacustrine to brackish-liuoral environments. After a regressive Formation; Vass 2002). The lowermost Sarmatian deposits are Carpathian Foredeep. This situation is also reflected in the . The Southern Burgenland High, eonsisting on the phase at the end of the Early Karpatian this formation was reeorded from the Kuty and Kopeany grabens in the northem internai facies patterns. Thus, the smalI, elongated basin was surfaee of a SW-NE trending range of low hills, represents the discordantly overlain by the lacustrine.terrestrial facies of the Vienna Basin. Pluvial gravel was dcrived from the Northem divided ioto a southern, estuarine part with extensive tidal southern border. In the Early and Middle Mioeene, the .astem Gänsemdorf Formation. At the same time, up to 400 m of sandy Alpine Foreland Basin. In coastal settings unique bryozoan- mudflats aod Crassostrea biohenns, and a northern shalIow- part of the basin was eovered by the Paratethys and by Lake deltaie deposits (Sastin Member) prograded into the Siovak part serpulid-algal bioconstructions flourished, fonning reefoid struc- marine part with depth of 20-30 m. No Middle or Upper Pannon during the Late Miocene. In the western part of the into the Vienna Basin. The top of the Gänsemdorf Formation tures several metres high. These are welI preserved along the Mioeene deposits are known from the Komeuburg Basin (all data basin, swamps fonned during the Early Miocene, giving rise to grades into the overlying Aderklaa Formation without a major Male Karpaty and Leitha mountains in the eastern and southem from Harzhauser el al. 2002; Harzhauser & Wessely 2003). thick lignites, which have been exploited up to reeent times. unconformity. Sandstones, interbedded pelites and rare conglom- Vienna Basin and along the Steinberg Ridge. A subsequent The Eisenstadt-Sopron (Sub-)Basin is more or less triangular erates eharaeterize the deposits of the 1000 m thiek Aderklaa regressive phase in the Middle Sarmatian was ch~racterized by in shape and measures about 20 km. In the north it is bounded Tectonic selting and development Formation. Deposition took place in a limnic/fluviaI environment the progradationof a huge delta complex in the Matzen area in by the NE-SW trending Leitha Mountains and the assoeiated The SB is a small extensional basin located on top of an as part of a meandering river system. The Gänsemdorf and the central Vienna Basin and by erosion of Lower Sarmatian SE-dipping Eisenstadt Fault. In the east, the basin is bordered by eastward-moving crustal wedge, which contains c. 4 km of Aderklaa formations in the southern Vienna Basin can be biohenns. The renewed flooding during the Late Sannatian is the north-south trending Köhida Fault. The Rust-Fertörakos Neogene sediments. Basement comprises crystalline and low- correlated with the marine, brackish to freshwater Zavod Forma- reflected by the various mixed siliciclastic/carbonate deposits of Mountains separate the basin from the Danube Basin in the east. tion in the northernVienna Basin. grade metamorphicPalaeozoic rocks of the Austro-Alpine nappe the Skaliea Formation (Vass 2002). Extended oolite shoals (up to A crystalline ridge, covered by Lower Miocene gravels, extend- system. The tectonic evolution is divided into an Early Miocene A major regressive event at the Lower-Middle Miocene 30 m thiek) and eoquina shell beds formed in the entire Vienna ing from the Rosalia Mountains to the Brennberg, defines the (Ottnangian to Karpatian) synrift phase and a subsequent post- (Karpatian - Badenian) boundary, found in many Paratethyan Basin (Harzhauser & Piller 2004). southern margin. This topographical barrier also separates the rift phase. The SW-NE trending South Burgenland High nearshore settings, is also recorded in the Vienna Basin by At the Sannatian-Pannonian boundary, the Paratethys Sea Eisenstadt-Sopron Basin from the Styrian Basin. The develop- separatesthe SB from the Pannonian Basin. IntemalIy,the SB is erosional truncations of up to 400 m. The Vienna Basin became retreated from the Pannonian Basin area and the brackish Lake ment of the Eisenstadt -Sopron Basin is elosely linked with that subdivided by the Middle Slyrian and Auersbaeh highs into subaerial during this time, as reftected by palaeosol foonation. In Pannon was established. The Vienna Basin was dry and Middle of the Vienna Basin, although the thiekness of the basin fill is several small sub-ba,ins, ineluding the shallower Western Styrian the south, sedimentation recommenced during the early Middle Miocene deposits were eroded. Consequently, lowermost Panno. mueh less (c. 1500 m). Basin and the deeper Eastem Styrian Basin complex, which Miocene with the deposition of the Aderklaa Conglomerate, nian fluvial facies penetrated far into the basin, reworking older The oldest Neogene deposits in the present Eisenstadt-Sopron consists of the Mureck,Gnas and Fürstenfeld basins. which formed part of a braided river system. Similar conditions Sannatian strata. A ratheruniform, 50-100 m thick, monotonous Basin are of Early Miocene age. They comprise terrestrial, are doeumented by the Jabloniea Conglomerate in the north. unit of mari and sand of prodelta- and basinal faeies follows and fluvial and lacustrine deposits which are genetically related to Sedimentary and stratigraphie development During the subsequent Badenian transgression offshore pelites includes a 20-50 m thick marker unit of ostracod-bearing marly the fluvial system in the southem Vienna Basin. This suggests Sedimentation eommenced during the Early Miocene (Ottnan- (Baden Group) were deposited. This group eonsists of several elay at the top. The marly prudelta faeies is followed by a sandy that the Leitha Mountains did not exist as a barner at that time gian) (Fig. 17.9). In the Western Slyrian Basin fault-eontrolled fonnations, including the Lan.zhotFormation in the Slovak part succession up to 200 m thick with rare gravels representing a and that basin development was initiated not before the Middle limnie-/luvial deposits of the Eibiswald Member formed thiek of the basin. Corallinaeean limestones ('Leitha limestone') prograding delta of the palaeo-Danube in the northwestern part Miocene. The onset of subsidenee in the Early Badenian led to lignite deposits. In the Western Styrian Basin Miocene sedimen- frequently formed in areas with little elastie input. The first of the Vienna Basin. The oecurrence of the three-toed horse an initial marine ingression and the Leitha Mountains became a tation ended with the Middle Mioeene limnie-fluvial Stallhofen occurrences of Praeorbulina and of Orbulina suturalis within the Hippotherium within those deposits is an important biostrati- peninsula connected with the Alpine mainland in the east. Formation. Baden Group are important biostratigraphic markers (Rögl el al. graphie marker. '. Nearshore deposits of this transgression are represented along 2002). '~l'~ In the Eastem Styrian Basin, Ottnangian floodplain and coast- A major transgression followed and the elevated highs along the SE margin of the Leitha Mountains by the Hartl Formation al-plain deposits were overlain by a thiek Karpatian-age succes- During the early Badenian at c. 14.2 Ma a major sea-Ievel fall the western margin of the basin were ftooded by Lake Pannon which grades from reworkedgravel, through marine sandwaves sion deposited following a marine ingression from the P3lU1onian oeeurred. Several small deltaie bodies developed (e.g. Andlers- (Harzhauser et al. 2004). The Middle Pannonian deposits :1 inta corallinacean debris. During periods of high sea level in the Basin. Due to the extremely high subsidenee rate (30 emilOO a), dorf, Zwerndorf and Auersthal members). A seeond Badenian eonsist of c. 440 m of elays and sands (Bzenee Forma- Middle and Late Badenian, the Leitha Mountains were comple- related to synsedimentary fault tectonics, the shalIow-marine sequenee followed. Deltaie, fluvial and lagoonal settings devel- tion = Inzersdorf Tegel). The Upper Pannonian is eharaeterized tely eovered by water allowing the growth of thiek eorallinaeean setting evolved rapidly inta a deep-marine one (Sachsenhofer oped in the northern part of the Vienna Basin (Zizkov Formation). by the ubiquitous occurrence of thin lignite seams in its basal limestones and coral carpets. 1996). The corresponding 'Steirscher Schlier', a deep-marine This mostly freshwaterand brackish formation consists of calcar- parts and by a 200 m thiek sandy/marly upper part (Ciry Following a sea-level fall at the Badenian-Sannatian bound- shale succession with intercalated turbiditic sandstones and tuffs, eüus clays, containing lenses of cross-bedded sand bodies (c. Formation). During the Late Pannonian, the margin of Lake ary, the Leitha Mountains and their Badenian sedimentary cover formed in the upper bathyal zone under dysaerobic conditions 1200 m in the Moravian Centra! Depression). Thi, deltaie sueees- Pannon had retreated from the Vienna Basin. Floodplain became exposed and the mountain ridge onee again became an (Spezzaferri el al. 2002). Coastal areas along the emerging Alps sion passes upward iota littoral sandy clays with a marine fauna. deposits and freshwater lakes developed whieh were not island again until the withdrawal of Lake Pannon during the Late were affected by strong fluvial input of coarse clasties. Synchro- The following relative sea-Ievel rise is expressed by the deposition eonneeted to Lake Pannon. The basin fill terminates with a Miocene. Incised valleys developed and intensively eroded the nous with the synrift phase, andesitic island-arc volcanism or transgressive shelf sand bars and a baekstepping of the deltaie 450 m thick succession of marts, clays and silts with intercala- MiddIe Miocene limestone platforms. Lower Sarmatian deposits commenced and fonned huge shield volcanoes. The andesitic sediments. The littoral sands were subsequently overlain by the tions of sands, gravels, rare lignites and freshwater limestones from the Eisenstadt-SopronBasin consisting of pelites, sands and and shoshonitic volcanism continued into the early Middle calcareous clays of the neritic otfshore JakubovFormation. (Pannonian Gbely and Plioeene Brodske formations). In the serpulid limestones can be correlated with the HoHe Formation Miocene. A third Badenian suceession includes littoral and sublittoral southern Vienna Basin, Miocene sedimentation terminates with of the Vienna Basin. Correspondingly, the Upper Sarmatian Towards the end of the Early Mioeene, uplift (i.e. Styrian shoreface sands with eoralline algal biostromes at their base. A 1'1 the /luvial Rohrbach Conglomerate. Skalica Formation of the Vienna Basin extends ioto the Eisen- Tectonic Phase) led to basin shallowing and finally to the tilting 'i'i distinct flooding surface is preserved near Devinska Nova Ves in ~:i The Korneuburg (Sub-)Ba,in formed due to pull-apart stadt-Sopron Basin. A mixed siliciclastic/carbonate succession of older deposits. In marginal areas considerable erosion took '! "~i 11, !064 M. w. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1065

plaee and Middle Mioeene deposits are separated by a distinet south to the Lavanttal Basin. This basin, situated west of the the Outer Carpathian belt is an external tectonic unit, while the 11li of the Danube Basin is the Gabeikovo Sub-basin (Vass et al. unconformity from Lower Miocene ones. A renewed marine Styrian Basin, is a pull-apart basin located between the crystal- internal units are parts of two consolidated, palaeo-Alpine litho- 1990) with a maximum thiekness of Neogene sediments of ,11 ingression during the Early Badenian led to the establishment of line of the Sauaple and the Koralpe. Its development began in spheric fragments or micropiates (Alcapa and Tisza-Dacia miefO- >8500 m (Kilenyi & Sefara 1989; Hrusecky et al. 1993, 1996). shallow~marine conditions with widespread deveJopment of the Early Mineene with the fonnation of the c. 12 km long plates). These micropIates have a very complex movement The northem Vienna Basin and tbe northem Danube Basin Ili patch~reefs and corallinacean Jimestones (Weissenegg Formation) west-east trending Granitztal Sub-basin. Fluvial clastics and trajectory relative to their present-day positions (e.g. counter- shared a common tectonic evolution which is characterized by an l'j !!.j (Friebe ...1990). Corallinaeean platfonns developed along the limrtic clays of Ottnangian and Karpatian age were deposited. At clockwise rotation and movement of c. 150-300 km of the Early Miocene palaeostress jield with a NW -SE orientated shallow swells, and sublittoral to fairly deep-water marly and the Early-Middle Miocene boundary the basin geometty chan- Aleapa micropIate and clockwise rotation of the southem Tisza- principle compression. (P. Kovae & H6k 1993; P. Kovae et al. pelitie sediments were deposited in the deeper parts of the SB. ged considerably due to activation of the Pöls-Lavanttal Fault Dacia micropIates (Csontos et al. 1992; M. Kovae et al. 1994; 1994). During this time, a wrench fault elongate basin developed Aeeording to Friebe (1993), the Badenian of the Styrian Basin System resulting in the fonnation of a 27 km long NNW -SSE Kovae & Manon 1998). in the northem part of the present Danube Basin. cao be sllbdivided ioto three marine sequences which are related trending basin. A diverse mollusc and foraminifera fauna in the Five orogenie and basin evolution stages have been recognized An initial phase of rifting commeneed during the Iate Early to global sea-Ievel eyeles. marls of the Lower Badenian Mühldorf Beds is indicative of a in the Western Carpathians, each of which is characterized by its Mineene (Karpatian) following the extrusion of the Western A major drop in thc relative sea-Ievel occurred at tbc marine ingression. This short.lived conneetion to the Paratethys own tectonic regime (Koneeny et al. 2002). (1) The compres- Carpathians from the East Alpine domain (Csontos et al. 1992). Sannatian-Badenian bowuiary. Fault-controlled subsidence rates ended during the Middle and Upper Badenian when lluvial- sional regime is related to 'A-type' subduction at the Alpine- In the northern Danube Basin pull-apart depneentres opened in increased during thc Sannatian with thc extensive deposition of lacustrine and continental environments beeame dominant. A Western Carpathian orogenie front during the Early Miocene the Blatna and the central GabCikovo depressions/sub-basins marls. On topographie highs (e.g. South Burgenland High) and final transgression from the east took plaee during the Early (Eggenburgian to Ottnangian). (2) The transpressive-transten- (Hrusecky et al. 1996; Kovae et al. 1999). In the southern part of along thc coasts, bryozoan-serpuIid bioconstructions formed Sannatian. Shallow-marine to paralic conditions prevailed; rare sional tectonie regime is related to the escape of the Western the basin, north-south orientated normal faults were activated isolated carbonate bodies (Grafenberg Fonnation). Marine sedi- lignite seams within marls are typical deposits. Following a Carpathian lithospheric fragment (microplate) from the Eastern (Nemeok et al. 1989; Csontos et al. 1991; Tari et al. 1992; mentation was interrupted in the middle Sannatian by the Middle Sannatian hiatus, limnic pelites with lignites are found in Alpine area, aecompanied by its oblique collision with the North Royden 1993a, b; HruseekY et al. 1996). deposition of up to 100 m of lluvial sands and gravels (Car- the Upper Sarmatian, whilst the Pannonian is characterized by European platform edge in the latest Early Miocene and initial During the Middle Miocene (Badenian) the palaeostress field inthian graveI). The overlying Upper Sannatian units consist of lluvial deposits. A Pliocene magmatic phase, represented by the Middle Miocene (Karpatian to Badenian); initial rifting of the changed and NW-SE orientated extension prevailed (Csontos et the mixed siliciclastic/carbonate Gleisdorf Formation, which Kollnitz basalt, would appear to be related to a synchronous Pannonian backare basin oeeurred in a transtensional to exten- al. 1991; Nemeok et al. 1989; Nemeok 1993; Vass et al. 1993a). contains several oolitic beds. The upper part of the Upper voleanic phase in the Styrian Basin (Tollmann 1985; Strauss et sional regime. (3) The extensional regime is related to 'B-type' The Badenian synrift stage of basin development was character- Sannatian is characterized by repeated intercalations of thin al.2003). subduction at the Carpathian orogenie front, aeeompanied by the ized by structural unroofing of the deeply buried basement units, lignites and by a marker horizon with peneroplid foraminifera. synrift stage of the Pannonian backarc basin system during the especially along the western margin (Rechnitz-Sopron areal. In the Late Mioeene, the SB becarne llooded by Lake Pannon, Middle Miocene (Badenian to Sannatian). (4) Post-rift extension During the Late Badenian and Sannatian, north-south, NNE- Carpathians, Carpathian Foredeep and Pannonian and marls and silty sands of the Feldbach Fonnation were of the Pannonian backare basin system occurred due to thermal ssw and NE-SW nonnal faults were active in the northern Basins System: overview (M,K.) deposited. The overlying lluvial-limnic Paldau Fonnation repre- subsidence and the onset of isostatic uplift of the orogen during Danube Basin (Peniekova & Dvornkova 1985; Vass et al. 1993a). sents a second Pannonian sequence. The Upper Pannonian Despite being a part of the Alpine-Carpathian Orogen (Figs 17.2 the Late Miocene (pannonian to Pontian). (5) A Pliocene Duririg the early late Miocene (early Pannonian), tectonie sub- follows diseordantly and eomprises fluvial and limnic deposits & 17.16), the Carpathians are very different from the Alps, transtensional tectonie regime controlled isostatic uplift and sidence is documented ooly in the central and southern parts of the reflecting a total separation from Lake Pannon. A second mainly due to the presence of broad Neogene basins and tectonie inversion of the Western Carpathian basins; this was Danube Basin (Lankreijer et al. 1995). Predominantly 10w-angle magmatie phase is represented by tuff pipes and basaltic lava extensive acidie to calc-alkaline volcanic activity. Tbe differenee 'i~1 accompanied by the onset of a transpressional tectonic regime in nonnal faults were activated (Pogacsas et al. 1996). During the late llows of PliolPleistocene age. is caused by the tectonic evolution of the Carpathians, with a ;:4:; the Pannornan backare basin system. Pannonian and Pontian, thermal post-rift subsidence commeneed An overview of the tectonic evolution of the Styrian Basin has transition from 'A-type' subduction during frontal collision with ,:il (Becker 1993; Horvath 1993) and was followed by Pliocene basin been provided by Sachsenhofer (1996); detailed overviews of compressional regime during the earliest Mioeene, to oblique inversion, which was associated with minor compression from the 1tl. Danube Basin (M.K.) stratigraphy and depositional environments have been published collision with the European platfonn and 'B-type' subduction '.jr SW during the Late Miocene and Pliocene (Horvath & Cloetingh by Kollmann (1965), Friebe (1993), Gross (2003), Kosi et al. during the remainder of the Neogene (Tomek & Hall 1993; see .• :" The Danube Basin represents the NW part of the Pannonian 1996). Despite the Pliocene tectonic inversion, in some depocen- (2003) and Harzhauser & Piller (2004). also Froitzheim et al. 2008). backare basin system (Fig. 17.16). In Siovakia it is geographi- tres suhsidence still occurred. Subsidence in the Danube Basin The Fohnsdorf Basin, 22 km long and 1I km wide, fonned Tbe subduction in front of the orogen caused folding and cally tenned the Danube Lowland while in it is referred centre, in the Gabeikovo Sub-basin, is interpreted as being related to the NW of the Styrian Basin at the junction of two strike- nappe thrusting, which resulted in the development of an to as the Litde Hungarian Plain. It is situated between the to secondary 'sag basins', which are not superimposed on the older slip fault systems (Sachsenhofer et al. 2000; Strauss et al. accretionary wedge of the Outer Carpathians. In the foreland, the -i Eastem Alps, the Western Carpathians and the Transdanubiao Miocene basin depocentres (Wernicke 1985). 2003). These fault systems, the sinistral east-west trending Carpathian Foredeep developed on the slopes of the European Range in Hungary. -Mürz-Fault System and the dextral NNW -SSE trending Platform, due to the deep subsurface load of the downgoing plate Sedimentary and stratigraphie development Pöls-Lavanttal-Fault System, form the border of the eseaping and the loading of the accretionary wedge. The foredeep shows a Tectonic setting The Neogene sedimentation in the area of the present Danube crustal wedge which hosts the Styrian Basin. The evolution of significant pattern of depocentre migration from NW to SE The Danube Basin is c. 240 km long and 100 km wide and Basin began during the Eggenburgian transgression. The sea the basin, with a Neogene basin-fill of about 3 km, was (Meulenkamp et al. 1996). strikes roughly NE-SW. The western border comprises units of llooded the northern margin of the Western Carpathians and subdivided by Strauss et al. (2003) into three stages. The Subducting slab pull and the subsequent stretching of the the , the Leitha, Hundsheim and Male penetrated from the Alpine and Carpathian foredeep into the initial pull-apart phase (stage I) lasted from the Late Karpatian overriding plates were followed by basin opening in the Panno- ~~! Karpaty mountains. The northern margin is represented by the Vienna Basin, the Dobni Voda, Vad'ovce and Blatna sub-basins, to the Early Badenian and commenced with the deposition of nian backarc area under an extensional tectonic regime (Royden ...~! PovazskY Inovec and Tribee mountains belonging to the Central the Vilh river valley, the Birnovce Basin and the upper Nitra the Fohnsdorf Fonnation. This is characterized by up to 800 m 1988). In addition to the pull of the sinking slab and the j!,1 Western Carpathians. The Burda Mountains form the margin in Basin. A connection with the North Hungary-South Slovakia of alluvial sediments which terminate in a 15 m thick lignite subsequent stretching of the overriding plate, the evolution of the the NE while the Hungarian Transdanubian Range Mountains and East Slovakia basins can be documented (Kovae et al. 1998). seam whieh yields a typical 'Congeria' -coquina. Lacustrine to Pannonian backarc basins system was influenced by astheno- represent thc SE border of the basin. The pre-Cenozoic basement Coarse clastie littoral to shallow-marine deposits of the Dobm brackish prodelta and fan sediments were deposited in the late spheric mantle diapirism and by related deep structural unroofing is built up by the Austro-Alpine and Slovako-Carpathian units in Voda Conglomerate (Kovac et al. 1991) in the Blatna Sub-basin pull-apart phase and ennstitute the overlying 2000 m thick .~.l.'~.. and the Klaeno Conglomerate in the Banovce Basin represent the of the basement units (Tari et al. 1992; Horvath 1993). During _~Ji the western, northern and central part of the basin; the basement Ingering Fonnation. The brackish eonditions in the lower part the initial rifting and synrift stage of the backarc system, two "\ of the SE margin eomprises units of the Transdanubicum (Fusan basal part of the Eggenburgian Causa Formation. Up-section, the of the Ingering Fonnation suggest a connection to the marine types of basins developed: pull-apart basins (Vienoa Basin, East ~ et al.1987; Fülöp et al. 1987). 500 m thick Causa Formation consists of calcareous and sandy llooding of the Lavanttal Basin (see below) in the Early Siovakian Basin, Derecke Basin) and grabens or half-grabens The basin is divided inte several depocentres. Along the clays and silts with some tuff layers deposited in a deeper neritic Badenian. During the Badenian, the basin experienced a half- (Danube Basin, North Hungarian-South Siovakian Basin, Styrian ti northern margin these are from west to east: the Blatna, Risnovce marine environment (Cechovic 1959; Brestenska 1980; Kovac et graben stage (stage 2) and was covered by floodplain and Basin). The youngest late Miocene to Pliocene period is and Komjatice depressions (separated by the PovazskY Inovec al. 1999; H6k et al. 1995). lacustrine fan delta deposits. These immature conglomerates characterized by thennal post-rift subsidence, but in many places ~I and the Tribee mountains). In the NE part, the Zeliezovce Sub- Ottnangian and Karpatian terrestrial, ftuvial and lacustrine and sandstones ennstitute the Apfelberg Fonnation (Strauss et fault-controlled basin subsidence also occurred (Horvath & 1,"I basin is loeated between the Levice Horst and the Transdanubian sediments were deposited along the western margin of the al. 2003). The final compressive phase (stage 3)"began in the Cloetingh 1996). During Pliocene times, tectonic inversion of the } Range Mountains (Lankreijer et al. 1995). The southern, Hungar- Danube Basin and document the initial phase of rifting. These LateMiocene and was heralded by inversion and movement backare basin began. J; ian part of the basin is separated by the NNE-SSW trending sediments are known from the Sopron area in Hungary where, on along the Pöls-Lavanttal Fault System. For a fuller understanding of the Neogene geodynamic evolu- ; Mihalyi High into major sub-basins which parallel the Repce the slopes of the Eastern Alps, the coal-bearing Brenoberg The fault system controlling the Fohnsdorf Basin extends tion of the Carpathian Orogen it is necessary to understand that Fault in the west and the Raba Fault in the east. The deepest part Fonnation. (Csaszar 1997) was deposited during the Ottnangian J066 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1067

and was overlain by the f1uvia1to limnie gravels of the Ligeterdö southem parts were hundreds of metres deep (Kovae cl al. 1999). SSW orientated main eompression (Nemeok 1993). Compressive Ukrainian part of the Transearpathian Basin, the Tereshul Fonna~ Formation (Csasz,;,. 1997). Otlnangian and Karpatian marine The basin was gradually filled by deltaie deposits entering the tectonics led to the disintegration of the Early Miocene basin and tion is the equivalent of the Karpatian deposits in the East Slovak deposits are known from the Dobni Voda and the Blatna basin from the NNW, transporting clastie material from the to the development of baekthrusts in the Pieniny Klippen Belt Basin. sub-basins in the north and from the Transdanubian Range uplifting Alpine-Carpathian orogenie belt. The Upper Mioeene (Send 1956; Roth 1980; Plasienka el al. 1998). The Lower Badenian sediments in the eastern and central part Mountains. along the southem margin cf the Danube Basin. and Plioeene deposits, eontaining elays, siltstones and sand- During the late Early Mioeene (Karpatian), a palaeostress field of the ESB are represented by volcanidastie deposits of the CalcareQus siltstones cf the Ottnangian to Lower Karpatian stones, are up to 3500 m thiek in the Gabeikovo Depressiool with a north-south orientated main compression prevailed. NW- NiZnYHrabovee Formation. The formation is up to 600 m thick Planinka Formation were deposited in the Dobra Voda Sub-basin Sub-basin (Adam & Dlabae 1969; Vass el al. 1990). SE orientated normal and later right-Iateral strike-slip faults were and consists of manne c1ays, siltstones with sandstone intercala- (Kovae el al. 1992), and the Banovee Formation represents this In the Hungarian part of the basin, Lower Pannonian deposi- formed. During Karpatian and Early Badenian initial rifting, tion and rhyolite tuffs. In the western part of the basin the Lower facies in the Banovee Basin (Vass in Keith el al. 1994). In this tion began with the open-water marls of the Endröd Formation pull-apart depneentres opened in the eentral part of the ESB. Badenian is represented by the Mirkovee Formation with rnarked lauer basin, the Ottnangian part cf the sedimentary succession is (Vass 2002) indieating a water depth of up to 800 m. The Teetonically controlled subsidence shows a cyclic charaeter, with redeposition of Karpatian-age mierofaunas in its basal parts. In e. 300 m thiek while the Karpatian part is e. 250 m thiek. The overlying Middle to Upper Pannonian Ujfalu Formation was periods of high sedimentation followed by periods of basin the Ukrainian part of the Transearpathian Basin the Lower lower part was deposited in a brackish environment, with lowered deposited in delta-front to delta-plain settings. The Pontian to isolation and shallow-water evaporite deposition. Crustal exten- Badenian is represented by the Novoselytsa Formation. oxygen content, aod the upper part in a marine, shallow to deep Lower Plioeene Zagyva Formation represents alluvial plaiD, sion was associated with updoming of a lithospheric mantle During the Middle Badenian, cIays, siltstones, sandstones and neritic environment. The marine pelites ('Schlier') are character- ftuvial to laeustrine environments, and eomprises e. 1000 m of , diapir leading to struetural unroofing of the Inaeovo-Kritsehevo rare tuffs of the 600 m thiek Vranov Formation were deposited in ized by the appearance of foraminifer associations containing sands, silts and eoal-bearing days (Csaszar 1997). In the Siovak Peninie Unit (Sotak cl al. 1993). the central part of the basin. The sands were derived from the Uvigerina graciliformis. part of the Danube Basin the Lower and Middle Pannonian The Upper Badenian and Sarmatian tectonic regime of the uplifting Outer Carpathians in the NE. Tbe sedimentary environ- At the Early-Middle Mioeene boundary, rifting in the Danube sediments are represented by the Ivanka Formation (Harear cl al. ESB can be characterized as the development of an interarcl ment gradually changed from a deep-marine to a shallow-marine Basin was accompanied by calc-alkaline volcanic activity. The 1988), eomprising ealcareous days, siltstones and sandstones. baekarc type basin. The change from transtension, during initial ODe and the end of deposition is represented by the lagoonal stratovoleanoes are buried below the Middle-Upper Badenian The Upper PannonianiPontian, c. 100 m thiek Beladiee Forma- rifting, to pure extension, during the synrift phase, resulted in evaporites of the Zbudza Formation. In the Ukrainian part of the sedimentary fill in the northern and eentral parts of the present- tion (Hare';" el al. 1988) eonsists of ealeareous days and tectonically controlIed subsidence and a high sedimentation rate Transcarpathian Basin these evaporites are united in the Tereblya day basin aod document crostal extension during basin formation siltstones, with coal-bearing days and lignite seams. The Lower during the Early Sarmatian (Pereszlenyi el al. 1991). The main Formation and the lower part of the Solotvino Formation. (Hruseeky el al. 1996). From the Hungarian part of the Danube Pliocene Volkovee Formation eontains deltaie deposits of the depoeentres shifted to the SE. The basin development coineided The Upper Badenian transgression reaehed the ESB from the Basin younger Badenian, Sannatian to early Pannonian trachyte palaeo-Hron river in Komjatice and the Gabeikovo sub-basins. with inereased voleanie aetivity at this time (Lexa el al. 1993). south, from the Pannonian region. The deep-water pelitie facies voleanism is reeorded in the Pastori Formation (Csaszar 1997). The Upper Plioeene Kol,;,.ovo Formation (Dlabae 1960) repre- During the Upper Mioeene the thermal, post-rift phase began in the basin centre pass into eoarse dastic deltaie deposits Karpatian deposition commenced with terrestrial sediments in sents the palaeo- Vah river deposits in the Blatna Sub-basin. and the ESB beeame part of the Pannonian Basin System prograding from the NW margin of the basin. The lower part of the eentral part of the basin (c. 500 m thiek near Györ). The Quatemary deposits of the Danube Basin are represented by (Horvath cl al. 1988; Mattiek cl al. 1988). Subsidenee was the Upper Badenian sueeession is represented by the Lastornir Bajtava Formation, at the eastern basin margin, contains Lower loess deposition (up to 150 m) and Iluvial and alluvial deposits. eontrolled by north-south to NW -SE extension. The Plioeene Formation, atlaining a thiekness of up to 2000 m in the SE part Badenian marginal transgressive conglomerates, sandstones and was characterized by tectonic inversion and a palaeostress field of the basin. The formation consists of ealcareous clays with vo1caniclastics, overlain by calcareous days, siltstones and rare with NE-SW orientated compression whieh led to folding of the siltstone intercalations deposited in delta-slope and prodelta el a/. East Slovak Basin (M.K.) sandstones deposited in a neritic environment (Kovac Pannonian deposits (Kovae el al. 1995) and uplift of the youngest envirorunents. Tbe upper part of the succession is represented by 1999). In the NW part of the basin ealcareous days and The East Siovak Basin (ESB) is situated between the Western sediments in the East Siovak Lowlands (MofkovskY & Lukasova the Koleovo Formation (up to 1700 m thiek), whose deposition siltstones of the 3000 m thiek Middle Badenian Spaeinee Forma- and Eastern Carpathians (Fig. 17.16). The western border ofthe 1986, 1991). extended up into early Sannatian. In the Ukrainian part of the tion were deposited. In the Blatm, Sub-basin the delta-front sands basin is formed by the Tatrie and Veporie units of the Central Transearpathian Basin, the Upper Badenian is represented by the of the Madunice Formation indicate shallowing in the tatest Western Carpathians. The NE and eastem margins eonsist 01' Sedimentary and stratigraphie development upper part of the Solotvino, the Teresva and the Baskhev Middle and Late Badenian (Adam & Dlabae 1969). The Upper units of the Pieniny Klippen Belt, and the Humenne Mountains. The Lower Mioeene deposits are situated mainly in the NW part formations. Badenian part of Pozba Formation overlies the Spacince Forma- Towards the south the Neogene successioos pass ioto the of the basin, Middle Miocene deposits fill its eentral part, and In the Sarmatian, the depoeentre of the ESB widened towards tion. It is up to 2000 m thiek. This eonsists of ealcareous days, Hungarian Hemad Basin. The SWand SE margins are formed by the late Middle Mioeene and the Upper Mioeene depoeentres are the SE in the region of the Vihorlat Mountains and towards the siltstones and sandstones with volcaniclastics; in marginal areas the Siovak-Hungarian Zemplin area and the Ukrainian Seredne in the SE part of the ESB (Janaeek 1969; Rudinee 1978, 1989). SW in the Kosiee Sub-basin. Fan deltas and braided river system algal limestones developed. In the southem (Hungarian) part of area (Rudinee 1978, 1989). The following summary is based mainly on Vass & Cvereko deltas prevailed (Janoeko 1993). The Lower to Middle Sarmatian the basin, the Baden Clay Formation was deposited (Csaszar (1985), Zlinska (1992) and Rudinee (1978, 1989) for the Stretava Formation (1600 m thiek) is a monotonous unit of 1997). This eonsists of days and marls of open-marine facies, Teetonie setting Slovakian part and on Vialov (1986) and Andreyeva-Grigorovieh calcareous days with rhyolite tuff intercalations which was with a rieh thin-shelled maltuse fauna as weil as foraminifers. lts The ESB represents the NW part of the Transearpathian Basin cl al. (1997) for the Ukraine. deposited in a deltaie environment. Tbe delta prograded from the maximum thiekness is e. 1000 m. In the southem part of the which covers parts of Slovakia, Ukraine and Romania, reaehing The Eggenburgian open-marine sediments belong to the NW towards the SE. Its marginal facies are represented by the basin coralline algal limestones of the Rcikos Formation and 220 km in a NW -SE direetion. The ESB is generally up to Presov Formation and were deposited in a foreare basin environ- Kosiee Member (Kalieiak 1991). The overlying Upper Sarmatian marls of the Szilagy Formation were deposited; these have a 9000 m deep, although the Ukrainian depoeentres were only ment. The sueeession, which is up to 1000 m thick, consists of Ptruksa Formation, consisting of ca1careous sandstones and tuffs, eombined thickness of up to 100 m. At the NW basin margin 2000-3000 m deep (Rudinee 1989). Various struetural and days, siltstones, sandstones and eonglomerates. The end of is up to 300 m thiek. In the western part of the basin freshwater freshwater deposits with eoal-bearing elays and lignite seams of geological units belonging to the Western and Eastern Car- Eggenburgian deposition is marked by the Celovee Member systems prevailed, as indieated by the lignite-bearing Middle to Late Badenian age are also known (Vass el al. 1990). pathians form the basement of the ESB (Sviridenko 1976; where marine siltstones and days grade into lagoonal and Upper Sarmatian Kochanovce Formation. In the Ukrainian part The Badenian deposits are diseordantly overlain by the Rudinee cl al. 1981; Rudinee 1984; Vass el al. 1988; Sotak el al. freshwater deltaie deposits consisting of eonglomerates, sand- of the Transearpathian Basin the Sarmatian is represented by the Sarmatian Vnible Formation (Harear el al. 1988). Tbis offshore 1990 1993, 1994). Tbe NE margin is represented by the ti stones, siltstones and lignites. Ottnangian deposits have not been Dorobrotiv, Lukiv and Almash formations. facies eomprises ealcareous elays, siltstones and sandstones up to Mesozoie and Palaeogene units of the Pienniny Klippen Belt reeorded in the ESB. In the Ukrainian part of the Transearpathian The Upper Mioeene of the ESB eomprises up to 600 m of 600 m thiek (Adam & Dlabae 1969). In the nearshore areas whieh separates the units of the Outer Carpathians Flysch Belt Basin the Burkalo Formation represents similar early Miocene brackish to freshwater deposits. The Pannonian Secovce Forma- eonglomerates, sandstones, limestones, loeal lignites and tuffs from the Mesozoic complexes of the Humenne Mountains deposits. In the ESB, 1600 m thick Karpatian-age sediments tion consists of calcareous days, eoal-bearing elays, eoal seams were deposited. Tbe maximum thiekness (1300 m) of the (Mahel 1986). The NW part of the basin basement comprises the comprise the Teriakovce, Sol'na bana and Kladzany formations. and tuffs (Albinov tuff; Janaeek 1969) whilst the Pontian Senne Sarmatian strata is doeumented from the Risnovce Subbasin Central Western Carpathian Mesozoie and Palaeozoic units of The Teriakovce Formation is up to 500 m thiek and grades from Formation was deposited initially in f1uvial(PozdiSovee Member) (Biela 1978). In the southem, Hungarian part of the basin, the the <":iema Hora Complex, while the SW part consists of the eonglomerates and sandstones into siltstones and days deposited and tater in lacustrine, environments. Up to 200 m of days, equivalent of the Sarrnatian offshore facies is the Kozard Zemplin and Ptruksa eomplexes (Rudinee 1984; Vass el al. 1988; in a deep-marine, neritie to shallow bathyal environment. The sands, gravels (with andesite pebbles) and tuffs comprise the Formation with a maximum thickness of 150 m. Marginal Sotäk el al. 1993). overlying Sol'na bana Formation (400 m) is represented by Plioeene Ceeehov Formation. development is here represented by the Tinnye Formation The tectonic development of the ESB relleets ehanges both in evaporite deposition which took place in a shallow-water envir- In the Ukrainian part of the Transearpathian Basin the (100 m) with frequent oceurrenees ofmolluse-bearing caleareous terms of its geotectonic position, as weil as due to ehanges in the onment as a result of basin isolation. Renewed latest Early Pannonian Iza and the Pontian Koshelevo formations attain a sands and sandstones (Csaszar 1997). palaeostress field orientation (Kovae el al. 1995). The Lower ':1 Mioeene tectonie subsidence is refteeted by the deposition of joint thiekness of up to 400 m and represent the Upper Mioeene Pannonian and Pontian-age sediments of the Danube Basin Mineene (Eggenburgian) sediments were deposited in a foreare s; clastic material via turbidity eurrents of the Kladzany Fonnation. sueeession. The Pliocene is represented by the Dacian I1nitsa were deposited along the northem margin of Lake Pannon. The basin position on the margin of the moving Central Western Tbe succession eontains clays and siltstones with sands tone Formation, up to 500 m thiek, and the Pleistoeene by the clays, northernmost part of the basin was shallow, while the central and Carpathians. The palaeostress field refleets NE-SW to NNE- intercalations and attains a maximum thickness of 1000 m. In the sandstones and gravels of the Chop Formation (600 m). 1068 M. w. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1069

Volcanism During the laIe Early Mioeene, the development of the backare The development of the East Slovak Basin was assoeiated with basin eontinued (Vass el al. 1993a) and the Novohrad-Nögrad = voluminous volcanic activity related to backare extension and ., ~jji-I Dorog Suda Basin fonned. Gradual marine transgressions from the south in the Cl 'iiicS Zala I SW - I NE - I Salg61aljan I S - IAgglelek subduetion beneath the front of the Carpathian are. Extension- l! >. Q) J!I Basin Bakony basin mls basin Bükk mls Ottnangian are documented by paralie sedimentation in BOrSod .2"OeU (Q I W I Ul Ul Ul related acid rhyalite volcanism is known from the Lower and * I.~I I •. .. (northern Hungary) and by marine ingressions in southern Slova- &! Middle Mioeene sueeessions. The Middle to Upper Mioeene is kia. Basin subsidenee reached a maximum during the Karpatian, Ssrmatian predominantly ealc-alkaline andesite volcanism related to sub- ~ SERRAVALllAN followed by rapid regression. Tbe area was uplifted and erosion 0 duction processes. The Late Badenian and EarIy Sarmatian ci 0 was marked by lalest Karpatian times. The final transgression 's H I ;; LANGHIAN """""'" voleanie aetivity is of are type (Vass el al. 1988; Kalieiak & extended into the area of south Slovakia. in the early Middle 0 W Pospiiil 1990; Szabö el al. 1992; Lexa el al. 1993). During the z """''''''0_ Mioeene (Badenian). From Middle Badenian times onward the BURDIGAUAN Sannatian, the basin evolved into an interare basin and andesite Ulw w", region was emergent and subjected to intense weathering. 20 H u '" Eggenburgian voleanie aetivity eulminaied (Vass el al. 1988). The volcanie Z ~ ~ ;:;; AQUITANIAN chains cao be traced along the eastem margin of the basin Sedimentary and stratigraphie development towards the Gutin Mountains and along its southem border along Egenan This seetion is largely based on the work of Baldi & Baldi-Beke 25H W a now-buried area between Zemplln and Beregovo (Slavik 1968). 0 '" (1985), BaIdi (1986), Baldi-Beke & BaIdi (1991), Vass (2002), I z il' CHATTIAN W '5 Vass el al. (1979, 1983, 1987), Vass & Eleeko (1982, 1992), and u - North Hungarian-South Siovak basins (M.K., D. L.S., Ramor (1988). 0 v., 30 H N I I KiscelIian A.N.) W ~~I RUPELIAN .•.• 0 Zala Basin. Tbe southwestemmost Palaeogene deposits of the o ~ The North Hungarian-South Slovak basin is bordered to the Transdanubian Range area oeeur in the Zala Basin (Fig. 17.17). 0 Z north by the Western Carpathians (Fig. 17.16). The western 35 H The oldest member of the suceession is the littoral to neritic W PRIABONIAN Recsk Camp. margin is represented by the Transdanubian Range Mountains, ~ Upper Luletian Szöe Limestone (180 m). This formation is Z while the eastern margin consists of units of the Bükk Moun- overIain up to 600 m of calcareous and sandy marls of the Cl BARTONIAN I tains. In the south, it is bordered by the Mid-Hungarian region pelagie, epibathyal Padrag Mari, refleeting the period of maxi- 40 H 0 W "I whieh forms the boundary between the Aleapa and the Tisza- mum deepening during the Late Lutetian and EarJy Priabonian. W Dacia mieroplates. W z g I In the upper part of the formation, andesitie tuffs of the W ;; Zalat3rnok~Zalaszentmihaly voleanic centre are interbedded u 45H U I< 0 LUTETIAN Palaeogeography and teetonie setting (Szentmihaly Andesite). Near the basin eentre, a stratovolcanic ..J W Da",a5t6Fm. j Tbe pre-Cenozoie basement is formed in the north by units of eomplex more Ihan 1000 m thiek. has been penetrated. The I~ the Central Western Carpathians (Veporieum, Gemerieum, Siliei- ~ Qj>,...... - Eoeene deposits are eovered by up to 2000 m of Neogene 501-1 I< eurn, Meliaticum), in the west by units of the Transdanubieum Gant Fm. sediments (Körössy 1988). lL '" I: ~ YPRESIAN ii and in the east by unils of the Igal-Bükk Zone. The Slovak part 'l: 9 I! is geologieally not an individual basin hut represents the northern Soulh Bakony Mounlains. In the southern Bakony the Palaeo- ~il margin of three basin eomplexes whieh overlie one another: the ,~! 11 gene sequences begin with local bauxite deposits (Gant Forma- Buda Basin (= North Hungary Palaeogene Basin), the FiJ'akovo- 1 Fig.17.17. Palaeogene and lower Neogene lithostratigraphy ofthe Hungarian basins. See Figure 17.18 für legend. tion). Bauxite occurrences can be traeed along the northern and .:i,~1 ,.I! Petervasara Basin and the Novohrad-Nograd Basin. A detailed southern margins of the Bakony Mountains. The bauxite is '~iY i: overview including all relevant literature used in the present text overlain by the Lower Lutetian Darvasto Formation (e. 40 m) was published by Kovae el al. (2002). The entire region rotated comprising terrestrial days and quartzitic conglomerates in its I)" ~~ 50. eountercloekwise during the Early to Middle Mioeene lower part. Its upper part consists of neritic limestones and marls Buda Basln. The Lutetian transgression gradually flooded the Formation in Siovakia. In the Late Oligoeene (Egerian) the ~i (Marton el al. 1996). with a rieh Alveolina and Nummuliles fauna (Keeskemeti 1998). Buda Basin (Fig. 17.I7; North Hungary Palaeogene Basin) evolution of the Buda Basin eontinued with the deposition of the The Buda Basin (North Hungary Palaeogene Basin) began to The Oarvaslö Formation is eonformably overlain by the Upper forming lagoons in whieh lignite deposition (Obid Member, Lucenec Formation. Hs lower part consists cf up to 150 m of fonn following a long period of emers ion of the Transdanubian Lutetian to Lower Bartonian Szöe Limestone (e. 100 m). This Dorog Formation) oceurred. Shallow-water carbonate sedimenta. transgressive breccias, conglomerates and sandstones with a Range Mountains (Transdanubicurn units), as indieated by biogenie limestone contains various shallow-marine organisms tion and deposition on the Duter shelf is represented by the shallow-water marine fauna (i.e. Paniea Member). Stratigraphie lateritie weathering and the ereation of karst bauxite deposits such as corallinaceans, bryozoans, eehinoids and larger foramini- Priabonian limestones of the Szepvölgy Formation (Kazmer equivalents include the Hungarian Törökbalint Formation and the (BaIdi & BaIdi-Beke 1985). Its evolution was terminated by the fera. The Szöc Formation passes upwards into the pelagic, 1985) and the overlying marls of the Buda Formation. At the end Siovak Budikovany Formation. The Egerian offshore faeies is teetonie extrusion, post-Iate Oligoeene, of the Alcapa Mieroplate bathyal Padrag Mari (e. 250 m; Bartonian to Priabonian). Pebbly (~ of the Eocene, a regression in thc Transdanubian region led to a represented by shaly ealeareous siltslones up to 1000 m thiek from the Alpine-Dinatide domain towards the Carpathian- mudstones, sandy turbidites and tuffitic intercalations occur in its shift of the depocentre eastwards ioto thc region of the Buda (Szeeseny Member = Lower part of Szeeseny Schlier Forma- 0,':1,41 Pannonian realm. This led to the disintegration of the Palaeogene upper part. The top of the eroded Eoeene is uneonformably Hills. tion). Limestones and conglomerates of the Bretka Member, basin by right-Iateral displacement along the Mid-Hungarian covered by the terrestrial and fluviatile gravels and clays of the ,.f During the Oligocene, the Buda Basin rapidly deepened as containing Miogypsina gunteri, represent thc nearshore facies in .:"s' region. Two segments were ereated, Buda and Siovenia (Ljubla- Upper Oligoeene Csatka Formation (e. 120 m). indieated by the deposits of the Ci. Formation in Slovakia and the upper part of the Lucenec Formation. The Egerian succession 'ti 03), whieh are at present 300 km distant from one another the equivalent Harshegy and Kiseell formations in Hungary. The tenninates with the regressive delta sediments of the 180 m thiek (Nagymarosy 1990; Csontos el al. 1992). ~~I North Bakony Mountains. In this region Eocene deposition in oldest Oligocene sediments are freshwater and fluviaJ deposits of Siovak Opatovee Member and the lignite-bearing, braekish, In the Early Miocene (Eggenburgian). the Fil'akovo-Peterva- an archipelago landseape commenced during the tatest Lutetian Ihe Skalniea Member (Kiseellian age) deposited in the Rimava marshy-fluvial Becske Formation. sara Basin was fonned. Its extent was less then that of the Buda somewhat later than in the South Bakony Mountains. Basal and Lucenec sub-basins. These are overlain by the littoral Basin and it lacked the southern eonnection to the open sea but clasties and redeposited bauxite are covered by the Dorog Coal J deposits of the Hostisovee Member eonsisting of clays, silts and Fil'akovo-Petervasara Basin. During the Eggenburgian, the opened towards the basins of the Outer and Inner Carpathians Formation (e. 50 m) eomprising paralic marls with diverse sandstones with thin coal seams. Ongoing transgression led to short-lived Fil'akovo-Petervasara Basin evolved. The Fil'akovo (Sztanö 1994; Halisova el al. 1996). At the end of the braekish and marine maHusc fauna. The coal is eonfonnably the formation of the spongelbioclastie and intraelast limestones Formation concordantly overlies the Lucenc Fonnation in the Eggenburgian, extensive felsie volcanism, related to astheno- overlain by neritie marls and by the epibathyal Padrag Mari (c. of the Batka Limestone Member deposited along the slopes of Cerova vrchovina Mountains. Its Hungarian equivalent is the spherie manlle uplift assoeiated with the uplift of the area (aetive 200 m). Above a hiatus, the Upper Oligoeene non-marine Csatka barner islands. The subsequent isolation of the Central Para- Petervasara Formation. The 500 m thiek formation was deposiled rifting), occurred, together with a coeval marine regression. Formation follows (e. 800 m); this part of the sueeession is tethys is manifested by the euxinie faeies of the Tard Clay in shelf environments, often showing a strong tidal inftuence Initial backare rifting resulted in the deposition of Ihe Bukovina similar to that of the South Bakony Mountains. Terrestrial and Formation cropping out in thc Budapest area. The development (Sztanö 1994). The Siovak Cakanovee Member and the upper Formation which consists of continental deposits with rhyodacite freshwater deposits alternate; thin eoal seams oecur in the basal of new depositional eentres in the Oligocene was accompanied part of the Hungarian Szeeseny Formation (Csasur 1997) tuffs (ZagyvapaIfalva Formation (Csasur 1997), rhyodaeite tuffs parts and fluviatile gravels and claystones are charaeteristic in by a transgression during the Kiseellian as marked by the clays represenl the offshore faeies. Outing the late Eggenburgian the in Gyulakeszi, Hungary). Ihe upper part. of the Kiseell Formation (800 m) in Hungary and the upper Ci. 200 m thiek, mainly fluvial deposits of the Bukovinka (Slovakia) 1070 M, W, RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE "11 1071 I' and Zagyvapalfa formations (Hungary) were deposited. These phically, they form the and the Great 11'. comprise sandstones, clays and rhyodacite tuffs (in Hungary Hungarian Plain. The PBS is surrounded by several Neogene Lillle Hungarian Great Hungarian Limestone I,' ~ I Sopran Gyulakeszi tufl) with abundant remnants of warm subtropical to 0) mts ~r!~ basins (e.g. Ibe Vienna and Styrian basins in Ibe west, the Plain Plain tropical flora. The Hungarian Zagyvapilfa formation contains Ibe Banovce, Nitra and Transcarpathian basins in the north, the ;1.11 Bi W Sandy limestone famous footprint sandstone at Ipolytamoc with very weil pre- Transylvanian Basin in the east, and the Morava, Sava and Tuzla ~ Tapolca Fm. serired traces of mammals and birds, and an enonnous fossil basins in the south). All of these basins formed in the Early- .Q Marl trunk of Pinus sp. (Kordos 1985; Hably 1985). Middle Miocene and contain several thousand metres of sedi- a:: :1 ment. Generally, a gradual shift in basin formation can be c: Shale (clay,siltstone) I. Novohrad-Nograd Basin. During the middle Early Miocene observed from the NW to the SE (see Csontos et al. 1992). ~'" (Oltnangian), the Novohrad-Nogrid Basin began to form. In Geologically, Ibe major basins described below are the most fl. Anoxie black shale Siovakia the lacustrine SalgotaIjan Formation is up to 250 m important. thick. In its lower part it consists of 30-80 m of locally cross- Coal measure bedded sands and clays with three characteristic coal seams (Potor Member). The overlying Plachtince Member comprises The LUtle Hungarian Plain Basin c: Evaporite I .CJ! clays with rare coals and tuffs. Carbonate clays include foramini- The Little Hungarian Plain Basin (LHPB) (Figs. 17.16 & 17.18) c: 0 fern and nannoflora of zones NN3 and NN4 indicating marine c: I extends to the north of the Transdanubian Range and soulb of c: Clayey marl ingressions during Ibe Ottnangian. The Salgotarjan Formation the Köszeg, Sopron, Little Carpathian and Inovec mountains. In a.'" gradually passes into the Karpatian Modry Kamen Formation, of its initial, early Middle Miocene, stage of formation, Ibe LHPB Sandy conglomerate which the Medokys Member represents the basal part of the was not connected to the Vienna and Zala basins. During the succession. Tt consists cf c. 60 m of fine-grained laminated Middle Miocene, it becarne connected with the Zala Basin but '"E c: Clayey gravel sandstones aod siltstones, locally with convolute bedding (Vass remained separated from the Vienna Basin by the Mihalyi Ridge ~ro+=-'" I (J)'Ul & Belaeek 1997) and tempestites with mixed marine and (Tanacs & Rilisch 1990). The Tatricurn in Siovakia (Fusan et al. ITE Sandymarl endemic-brackish fauna. The overlying Krtis Member (40 m) 1987), Ibe Bakony Unit in Hungary and the Alpine nappe C represents littoral sediments. Deposition culminated with tbe systems form Ibe basement of the LHPB. This basement is ~ ~ Siltstone 300 m thick Seeiance Member containing a rieh bathyal marine structured by tectonic highs (e.g. the Mosonszentjanos and 0 Conglomerale fauna. lts equivalents in north Hungary include the Egyhazas- Mihalyi highs) and deep sub-basins (e.g. the Csapod, Pasztori ~I .~ c: terrigenous I marine I gerge and the Fot formations and the Garab Schlier Formation EI and Szigetköz sub-basins). '0•• (Csaszar 1997). At the end of the Early Miocene a major Sandstone Subsidence of the LHPB began during the late Early Miocene. CO'" EJ:a terrigenaus I marine regression occurred in the entire Novohrad-Nograd Basin leading Initial deposits include terrestrial and freshwater clays, breccias I Terrestrial(variegated) clay to erosion. and conglomerates (up to 400 m) deposited along the central axis ~ (Red beds) A suhsequent transgression in the early Middle Miocene I: of the basin, in a 25 to 30 km wide belt. Tbe first Middle (Badenian) led to the deposition of the Pribelce Member (Vass et ••c.C: Miocene marine sediments (Badenian) are the sandstones and M Diatomite al. 1979), which is an equivalent of the Hungarian Baden Clay limestones deposited at the basin margins. PeJites with sandstone ~:m Formation (Csaszar 1997). This transgression was accompanied - li intercalations appear in the more basinal parts. These deposits C: ~ 8auxite by intense volcanic activity, represented by andesite volcani~ are up to 300 m thick and include the Baden Clay Formation and '" c: clastics in the Krupinska planina Mountains. The Hrusovo the Rakos Limestone. Vo1canic tuffs are frequent in the marine 8.S, k':'\/0~J Andesite pyroclastics r Member comprises "tuffaceous deposits with marine fauna and sequences and thick stratovo1canic successions occur to the NE nannoftora of the Early Badenian. During the Middle Miocene r;- ci> in Slovakia. By the Badenian the eutire LHPB bad been flooded Cl Rhyolitepyroclastics the Novohrad-Nogrid Basin became continenta!. After a phase of ~.J'." W kt+\i~ rl\~I\~A8asalt effusives f by the sea. Only a few NE-SW trending ridges formed islands. t..• emersion and denudation during tbe Middle and Late Miocene, The thickest Badenian units are located in the NE of the basin. l/v~v~vJAndesite effusives rA~;G~18asalt pyroclastics I, some subsidence is recorded in the latest Miocene or Pliocene Tbe Badenian-Sarmatian transition appears to be continuous in (Pontian). Fluvial and lacustrine deposits of the Poltar Formation the deepest part of the LHPB. The Sarmatian successions, up to (gravels, sands and kaolin days) were deposited in the Lucenec, 450 m thick, consist of clayey marIs, claystones, sandstones and ~fl.l'i~... Fig.17.18. Lithostratigraphy of the Sopron Mountains in Hungary, the Little Hungarian Plain and the . Rimava, Roznava and Tuma sub-basins. Coeval basaltic volcan. tuffitic sandstones (Tinnye and Kozar Formations). Upper Mio- .-i; I, ism (Podreeiany Formation) led to the formarion of maars wilb l' cene (Pannonian) sllccessions of tbe Peremarton supergroup (up laminated lacustrine deposits rich in organie matter (e.g. algi- to 1200 m thick) overlie the Sarmatian. The lower part of this '.,',.l;I-•..

I nates at Pincina; diatomic clays at lelSovec) (Vass et al. 1998). ~, !' supergroup is mainly clayey (e.g. Endröd Mari = Belezna Cal- Dacian to lowermost Quatemary volcanism is indicated by the careous Mari, Lenti Mari, Nagylengyel Mari) while the Vjfalu uplifting mountains. The HCR comprises Ibe Nagygörbo and the conglomerates, calcareous gravels, sandy limestones and tuffac- basaltic Cerova Formation which includes various volcanic ii (= Tofej) Sandstone and AIgyö (= Driva) Formation occur in !1J~ Varpalota basins, and thc Budapest area. eous clays (KOkay 1973; lambor 1980). An Upper Badenian unil I! structures (cones, lava fiows, lava plateaus, maars). As a the upper part. The associated Late Pannonian transgression of The Nagygörbö Basin developed during the Early Miocene up to 350 m thick consists of brackish to freshwater clays, coal I consequence of the uplift of the Cerova vrchovina Mountains and ~' Lake Pannon led to flooding of the entire area (Tanacs & Ralisch .,...... •...... along the NW margin of the Bakony Mountains (lambor 1980; seams, diatomites and alginites and unconformably overlies this due to the selective erosion ofthe softer deposits ofthe Fil'akovo 1990). The thickest units (c. 2100 m) of the LHPB were ~ Hamor & limbor in Steininger et al. 1985). The Ottnangian succession. The Sarmatian is characterized by tuffaceous sand- Formation, the basaltic ftows, originally filling palaeovalleys, deposited during the latest Miocene and Pliocene. These include f deposition commenced with terrestrial clays and conglomerates, stones and claystones. The upper part of the depositional now form the relief (relief inversion). ji the Dunantul Supergroup which is composed of the Vjfalu including the Lower Rhyolite Tuff (130 m). This member is succession of the Varpalota Basin is composed of 60 m of 1 Sandstone, the Rabaköz and the Hansag Red-bed formations overlain by Karpatian c1ayey marls, siltstones and sandstones Pannonian clayey marls, 120 m of Pontian sandstones, siltstones Continental development. South of the Mountains more iJ (lambor 1989). (150 m) yielding marine fossils in the upper part. Tbe Badenian and freshwater limestones. '1 ., than 500 m of clastics of the Eocene Szentlörinc Formation The Hungarian Central Range (HCR) represents a complex sandy marls, limestones, sandstones and conglomerates are up to In the Budapest area the Neogene succession begins with .I'1 represent an isolated Palaeogene continental depositional envir- of small sub-basins extending in age from the Ottnangian to the 420 m thick, unconformably followed by 40 m of Sarmatian 100 m of Eggenburgian marine conglomeratic sands (Budafok '1 onment in the Szigetvar area (Csaszar et al. 1990). Middle Badenian. During the Late Badenian it formed a slowly, conglomerates and limestones. The Pannonian is represented by 1! Sand). This is the littoral equivalent of the Szecseny and 1 but continuously, rising SW-NE striking ridge. The uplift is still 120 m of siltstones and gravels, while the Pontian and Pliocene !~l Petervasara formations in northem Hungary. The conglorneratic Pannonian Basins System (A.NJ ongoing. This ridge includes the Bakony, vertes, Gerecse, Buda, ri.. cornprise 200 m of sands, clays and lignites. sands are overlain by Ottnangian and Karpatian gravels, calcar- lll! Cserhit, Bükk and Aggtelek-Rudabanya mountains. Between the In the Varpalota Basin (North Bakony) 50 m of terrestrial eous conglomerates and tuffitic siltstones of the Fot Formation The Pannonian Basins System (PBS) (Fig. 17.16) is a complex uplifting blocks, small sub-basins developed, while the later clays (possibly Eggenburgian?) are overlain by the Oltnangian- (90 m). In the Middle Badenian non-marine beds and tuffs were of several (sub-)basins that formed during the Neogene. Geogra- i ~:i Neogene sedimentation was confined to the margins of the Karpatian Bantapuszta Formation (250 m), a marine complex of deposited, and were subsequently overlain by corallinacean Iime- 1:1: .~ (i:iI lh I I!I , I"L J 1072 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1073 stones and days in the Late Badenian. The Sannatian SoskUt neritie lithofaeies may be substituted by the Szilagy Mari ean be considered as a major low-angle fault (Rumpier & Limestone lies eonformably on the Badenian. The total thiekness (Turrile/la-Corbu/a beds) of more basinal eharaeter. The Sarma- tian units (2500 m) are lithologieally very similar but have eoal Horvath 1988). Seismie evidence indieates that the Budafa area, of the Middle Mioeene is 200 m in this region. Pannonian elays tian eomprises 20-80 m of littoral limestones. Beeause of uplift seams and clays in the uppermost part. where the Drava and Zala basins join, underwent very late and Pontian sands (up to 300 m) uneonformably overlie the during the Late Mioeene and Plioeene, Neogene sedimentation compression resulting in folding of the uppermost Mioeene/ Middle Mioeene deposits (eompiled from Jambor el al. 1966). eeased during the Sannatian in the West Mecsek Mountains. Plioeene strata (Körössy 1988), although the Quaternary units Great Hungarian Plain The Somogy-Mecsek-Kiskunhalas Basln (SMKB) eonsists of 3. The development in the East Meesek Mountains differs are undeformed. These folded structures ean be eonsidered as the a senes of sub-basins extending from south Transdanubiato the eonsiderably in terms of the distribution and thieknesses of the The Great Hungarian Plain (GHP) whieh forms part of the PBS west-east axial prolongation of the flal Sava folds whieh extend Danube- Tisza interfluve. The sub-basins of the SMKB have a formations (Forgo ef al. 1966; Hamor 1970). The terrestriall covers parts of Hungary, Romania and the former Yugoslavia. from inta Hungary. The maximum subsidence of the SE-NW strike, and are bounded by two large fault systems: the fluviatile Szaszvar Formation (380 m) represents the initial The area of maximum subsidence in the GHP is situated in the area took plaee in the Pannonian and Pontian. The thickness of Mecsekalja Lineament in the south aod the Kapos Lineament in period of sedimentation. It eonsists of elays, conglomerates, ;f,:' valleys ofthe Danube and the Tisza (Fig. 17.16). Basement relief the Pontian (probably including Plioeene parts) is up to 2500 m the north. The SMKB extends /Tom to the southern and sedimentary fill of the GHP are very heterogeneaus (Nagy- sandstones and coal seams in its upper part. The overlying in the Dniva Basin. part of the Great Hungarian Plain (Tanaes & Raliseh 1990). An Karpatian fish-shale (370 m) includes eonglomerates, thin marine marosy 1981; Fig. 17.!8). The area ean be subdivided into The Zala Basin is subdivided into a northern and a southern important feature of the sedimentation in this region is the early sillstones and an interealation of the Tar ('Middle') Rhyolite Tuff extremely deep sub-basins (up to 7000 m), with a more or less sub-basin. The northern Zala sub-basin is eharaeterized by the onset of subsidenee (latest Eggenburgian to earliest Ottnangian) in its upper part. The Badenian is represented by the eorallina- eomplete Middle Miocene to Plioeene sedimentary sequence, Transdanubian Range. Here, the Karpatian deposits are often in contrast to the areas of Great Hungarian Plain aod the Little eean I1mestones of the Pecsszabolcs Formation. This is overlain and intrabasinal ridges and highs, with an ineomplete sedimen- missing, and the Badenian, Sannatian, Pannonian and PORtian I Hungarian PlaiD. by the paralie eoal seams of the Hidas Formation. The Late tary reeord (up to 2000 m and usually laeking the Middle deposits are relatively thin and taper out towards the north and The evolution of the SMKB ean be related to three transgres- Mioeene). The sub-basins of the GHP include the Jaszsag Sub- Badenian transgression deposited the Szilagy Mari in the basinal east. Coarse~grained conglomerates and breccias fonn the Lower sions. Subsidenee began in the Early Otlnangian but affeeted basin (in the NW centra! zone), the Nyirseg Sub-basin (in the parts and the Rakos Limestone in nearshore environments. The Mioeene (presumably Karpatian) unit. The upper part of this only the western part of the zone (i.e. the Somogy and the West lotal thiekness of the Badenian is 280 m. Tbe eonformably NE), the Dereeske Sub-basin (in the east central zone), and the unit consists of paody sorted conglomeratic sandstones and Mecsek region). Terrestrial aod fluvial sedimentation was mainly overlying Sarmatian limestones are 150 m thick. Mako and Bekes grabens (in the south). A further sub-basin non-marine pebbly siltstones (215 m total thiekness). Badenian to the west and north of the Meesek Mountains. No subsidenee loeated in the western part of the GHP (Kiskunhalas Sub-basin) I 4. The Kiskunhalas Basin is loeated in the southern part of the deposits comprising 619 m of c1ays, silts and corallinaeean- took plaee in the Kiskunhalas area during the Otlnangian and is teetonieally related to the South Transdanubian Meesek Zone. Danube-Tisza interfluve. Its depth may be >5000 m. The oldest bearing sandstones of the Tekeres Schlier and the Szilagy Early Karpatian. Tbe nexl phase began in the Late Karpatian. Neogene sediments belong 10 the Kiskunhalas Formation, and Formation follow. The Sarmatian Kozard Formation (344 m) The character of the sedimentation changed from terrestrial Palaeogeography and teetonic setting I comprise eoarse-grained c1asties, w~ich eorrespond to the Szasz- eonformably overlies the Badenian. It eonsists of clayey marls through brackish to marine. Tbis transgression also invaded the The evolution of the OHP can be summarized as a history of var Formation in the Meesek Mountains. These beds, up to and sandstones. The 1049 m thiek Late Mioeene (Pannonian) Kiskunhalas area. Maximum sediment accumulation was to the gradual subsidence beginning in the tatest Early Miocene and I 800 m thiek, are of Early Karpatian age in the deeper sub-basins Peremarton Su~ergroup comprises clayey marls in the lower north (Meesek) and in the Kiskunbalas Sub-basin. During the continuing through the Middle Miocene into the Pliocene or even or younger (Early Badenian?) in the shallower ones. Tbe marine part and the Vjfalu Sandstone and Algyö Formation in the third phase, the transgression covered the area from the SW. Quatemary times. The rapidsubsidenee may have been related to I: Middle Badenian eonformably overlies these non-marine beds. lt upper part. The Pontian (1471 m) eonsists of alternations of During the Pannonian and Pontian the Mecsek area was uplifted the erustal atlenuation of the area (Horvath el al. 1986), resulting is represented by eonglomerates, breccias and the offshore sandy-c1ayey marls and sandstones, with clays, conglomerates and formed an island in Lake Pannon. The area north and south in the formation of pull-apart basins loeated in strike-slip fault Szilagy Mari (c. 600 m). No Sarmatian deposits are known from and coal seams in its upper part. The deeper southern Zaia sub- of the Meesek area subsided markedly during the Late Mioeene zones (e.g. the Balaton and the Meesekalja lineaments). The sub- 1I this area. The transgressive pelitic and sandy PannonianPeremar- basin fonned above basement, which eonsists of older crystal- (1500 to 2000 m thiek units). In the southern part of the basins in the north subsided rapidly during the Middle Mioeene ( ton Supergroup follows (850 m). Effusive lava beds of the line eomplexes and Mesozoic units, but is generally paody Kiskunhalas Sub-basin (Felgyö and Kömpöe areas) intense and the Early Pannonian while in the south the main phase of ii Kiskörös-Kecel basalt are intercalated ioto the Lower Pannonian known. Basin development was geoerally comparable with that subsidence continued ioto the Pliocene. The sedimentary subsidence took plaee during Late Pannonian, Pontian and pelitie beds. The Pontian and Pliocene regressive sueession (e. of the northern sub-basin. In the deepest part (Budafa areal, development in the SMKB is herein subdivided into four areas as Plioeene times (Tanaes & Raliseh 1990). The oldest Neogene 1800 m thiek) is represented by the mainly sandy Dunantul sedimentation began during the Karpatian with the deposition of deseribed below. subsidence occurred in a zone extending from the Mecsek i Supergroup. Clays oeeur in the upper part of the Plioeene. conglomerates. Tbe overlying marine Badenian is very thick I. In the West Somogy area of the SMKB the sueeession Mountains (Transdanubia)to the Kiskörös areawhere subsidenee The Mid-Transdanubian Zone is a deep Neogene basin (>2900 m) eomprising clayey marls, rare sandstone intereala- begins with the 1100 m thick Szaszvar Formation, aseries of loeated between the Balaton and Kapos lineaments in Hungary. began in the middle Early Mioeene (Otlnangian). Subsidenee in tions and alSO m thick stratovolcanic complex in its lower part. I: terrestrial/fluviatile eonglomerates, sandstones, clays, clayey The deepest part of the basin may be up to 5000 m. The oldest the rest of the OHP commenced in the latest Early Mioeene or The Sannatian, if preserved, comprises sandstones and bitumi- marls and days. lt is overlain by the marine sandstones and Middle Mioeene. mernber of the Neogene compnses a few hundred metres of nous, c1ayey marls with fish scares. As in the northem sub- clayey marls of the Budafa Formation of Karpatian to Early conglomerates with frequent red-bed intercalations. Its age may Marine transgression reaehed the GHP in Badenian times. 1I basin, the Upper Miocene and Lower Pliocene are represented Badenian age (970 m). Vp-seetion follows the 490 m thiek be pre-Badenian or Early Badenian. It is overlain by thin marine During the Badenian and Sarmatian the GHP formed an 'I by the Peremarton Supergroup (1155 m) and the Dunantul I Tekeres Schlier, aseries of clayey marls and siltstones. A hiatus archipelago of large islands, shallow and deep-marine basins. Badenian deposits and a thick Badenian volcanie eomplex. The Supergroup (825 m). separates the lower part of the Lower Badenian and the overlying 1j During the Sann,atianand Early Pannonianeven the topographie i' younger part of the Neogene was eored by the Mezöesokonya-4 In the Drava Basin the thiekness of the Neogene in the 690 m thiek Middle and Late Badenian rocks, represented by the borehole whieh reeorded 2000 m of Neogene rocks, but did not highs (e.g. the Battonya-PusztafOldvar and Algyö highs) were I' ',,<,- Croatian segment is up to 7000 m. The basement consists of I: Rakos Limestone and Turrite/la-Corbu/a-bearing marls (Szilagy drill the entire thiekness of the Badenian voleanie eomplex. This :;. submerged. During the Early Pannonian the GHP atlained its Palaeozoic and Mesozoie erystalline and sedimentary units. The ~ Formation). The next hiatus spans the Sarmatianand large parts was unconformably overlain by 450 m ofthe PannonianPeremar- ,Ji maximum depth. This event is documented first by the presence Neogene sueeession, as presented here, is based on Velic & [I of the Pannonian. The transgressive Ujfalu Sandstone represents of the pelagie Endroo- T6tkomlos Mari, an important potential ton Supergroup and by 1200 m of the Pontian and Plioeene 'j~1 Sokac (in Steininger el a/. 1985). Deposition eommeneed during I only the upper part of the Pannonian. These beds are followed by DunanlUl Supergroup. souree rock, and later by the turbidite-richSzolnok Formation. the Ottnangian and Early Karpatian, represented by 2000 m of ~ the Zagyva Formation. The total thiekness of the Pannonian is At the end of the Pannonian, basin subsidenee slowed down and l conglomerates, sandstones, limestones and clayey marls. During only 330 m. The overlying Pontian eomprises 250 m of sands gradual infilling of the basin began. Deltas prograded from the I the latest Karpatian, the marine charaeter of the basin became and clays (Somlo Formation) and 650 m of the Tihany Forma- Zala and Drava basins NNW to the SSw. While the northern part of the basin had dominant, but fuHymarine eonditions were typical only from the tion. already filled up and the paludal Bükkalja eoal seams were The Zala Basin is loeated in SW Hungary (Fig. 17.16) and is Badenian, when the marine transgression reaehed the Drava 2. In the West Meesek Mountains (eompiled from Forgo el al. depositeBanat and Morava sub-basins located to the south in former Hungary and northem Croatia. These two basins are conneeted In the 400 m thick Sarmatian units there are altemations of The regressional upper part eontains coal seams and elays. The Yugoslavia and in Romania. both geographieally and also in tenns of their depositional marls, laminated bituminous marls, rare sandstones and diato- Gyulakeszi ('Lower') Rhyolite Tuff is interealated into the lower- history. The main differenee is the strike of the basins. While the mites. Towards the top of the Sarmatian, the regressive trend most part of this formation. The second, Karpatian-Lower axis of the Zala Basin is SW-NE, the Drava Basin is NW-SE Sedimentary and stratigraphie development resuJtedin an erosional uneonformity between the Sarmatianand Tbe pre-Badenian formations of the GHP are tentatively assigned Badenian suecession eomprises limnie shales (Koml6 Member), (Körössy 1988, 1989; Tanacs & Ratisch 1990). There are also the Pannonian. Thus, the top part of the Sarmatian is missing. 10 the Lower Mineene (Otlnangian and Karpatian). Tbe oldest of the braekish and marine Budafa Formation, and the shallow differences in the sediment thicknesses between the basins, with The Pannonian units (up to 1000 m thick) eomprise marls, c1ayey the pre-Badenian formations is the terrestrial-IimnicMadaras marine Tekeres Schlier. The Middle-Late Badenian is repre- the Neogene succession being somewhat thicker in the Drava marls and subordinately sandstones, whieh were deposited in Formation (up to 100 m thick), whieh eonsists of eonglomerates sented by the 130 m thiek Rakos Limestone. This littorallshallow Basin. The Zala Basin formed parallel to the Raba Fault, whieh freshwater to brackish water environments. The overlying Pon- and thin tuff beds. Tbe overlying Kiskunhalas Formation (80- 1074 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1075

o Krosno-Moldavide flysch units ~ Neogene volcanic complexes 900 m) comprises sandy siltstones with conglomerates in limnic- Szolnok 'Flysch' Basin (A.N.) terrestrial facies. The first Middle Mioeene lithostratigraphie unit lIllllI Magura-Dragovo-Petrova units carpathian • Pieniny Klippen belt is the Tar ('Middle') Rhyolite Tuff and related voleanie eom- The Szolnok Basin (= Szolnok Flysch Belt) is a 130 km long ~ Inner-Carpathian flysch POLAND ~ m Inner-Carpathian pre-Palaeogene units plexes (e.g. Nyirseg Voleanie Complex). The first marine event and 20 km (rareiy 40 km) wide, SW-NE striking basin that Hungarian Palaeogene basin (HPB) '/ 0,. occurred in the Badenian and comprises the littorallshallow extends beneath the Great Hungarian Plain from the town of o $/ neriticAbony Limestone with conglomerate intercalations, thc Szolnok (Hungary) into the Maramures area of Romania (Fig. [;l;l Szolnok and Inner-Dinaride flysch <11] Mako Formation (marls and siltstones) and the Ebes Limestone. 17.20) (Dudich & Bombita 1983). Tbe basin strikes parallel to o Mecsek Palaeogene basin (MPB) C1~ In the Sarmatian both the brackish-water Hajduszoboszio Sand- an elevated erystalline ridge between TUrkeve and Körösszegap- • Transylvanian Pg. basin (TPB) <14' • stone and the Dombegyhaza Limestone were deposited in littoral ati. It can be traeed toward the east to Carei and Satu Mare in '1] to neritic settings. Romania and disappears beneath the Gutii Mountains. It is Thc Pannonian and Pontian facies belts shifted in time and known from several boreholes, espeeially from Hungary, but also UKRAINE spaee due to the gradual infiUing of the GHP (Pogacsas er al. from eastem Romania. North of the ridge the basement drops 1990). Thus, separation of the Pannonian and Pontian units is and is overlain by the deep-marine deposits (flysch) of the difficult and thc formations outlined below cannet be precisely Szolnok Basin (Kömssy 1959) and this contaet may be tectonic. dated (Jambor 1989; Juhasz 1991; Fig. 17.19). The oldest series of formations belangs to thc transgressive Maros Group and Palaeogeography and tectonic setting include evidence ofbasaltic volcanism in sorne places (e.g. Kecel The Szolonok Basin is located on the NE margin of the Tisza Formation). The basal Bekes Conglomerate Qecues mainly in the microeontinent. Together with the Mesozoic Tisza Nappes they Mako and Bekes grabens. The conglomeratie beds are overlain form a tectonic unit and represent the basement of the Neogene by the Endröd Mari and the Totkomlos Calcareous Mari Pannonian Basin. Körössy (1959, 1977) and Szepeshazy (1973) Member, which were deposited in a deep offshore environment. emphasized the strongly tectonized eharacter of the deposits of Submarine fans (Dorozsma Mari Member) also oceur. These the Szolnok Basin, with dips of between 70° and 90°. Palaeonto- were derived from steep slopes and occur only in the Mako and logical investigations indicate that deposition was not continuous, Dereeske sub-basins. Tbe Va83rhely Mari Member is a more but occurred over discrete time intervals with long hiatuses pelitic variant of the Dorozsma MarI. The lava flows and tuffs of between them. Tbe preservation and recent distribution of the the Kecel Formation are interbedded with the sediments of the Szolnok Basin deposits is strongly controlled by Early Miocene Dorozsma MarI. compressional tectonies and subsequent Miocene denudation. The deposition of the overlying Jaszkunsag Group coincided Tectonic imbrication and erosion is also suspected, whicb would with maximum deepening and the beginning of basin infill. The explain the lack, or scarcity, of Palaeocene and Cretaceous units. lower part of the group is represented by the offshore marls of Thus, the Szolnok Basin has an exotic position within the the Nagykörü Member (Endröd Formation) which is overlain by Carpathian are, having no direct connection with any of the or interfingered with the turbidite-rich Szolnok Formation. Carpathian or Dinaric units. In terms of its palaeogeographic 200 km Pontian sedimentation commenced with the deposition of the position, the Szolnok Basin may represent either (I) the tectoni- Csongrad Group eomprising the Algyö and Törtel formations. cally displaced continuation of one of the Outer Carpathian units, The AIgyö Formation (alternating elayey marls and sandstones) or (2) the continuation of the Inner Carpathian units (i.e. the represents the delta slope of rivers filling the GHP. Delta-front Transcarpathian 1000 m & B31di-Beke 1993; Szepesh3zy 1973; Majzon 1966). The basin developed on basement consisting of metamorphic, plain environment and interfingers with the Bükkalja Lignite. thick unit is eovered by up to 3000 m of Neogene and The Middle and Upper Eoeene part of the suecession com- ophiolitic and sedimentary units assembled during the Middle The Pliocene succession ends with the elays of tbe lacustrine- Quatemary sediments. The precise thickness of the turbidite prises shales, thin sandstones, polymictie conglomeratie sand- Cretaceous (Ciupagea er al. 1970; Sändulescu 1984). paludal NagyalfOld Formation. dominated deposits is unknown, since boreboles did not reach stones, eonglomerates and breccias. Rare nummulitid- and basement. The lithologieal composition of the Szolnok Basin coralline algae-bearing limestones (with ehaotie structure, prob- Palaeogeography and tectonic setting succession is incompletely known, but it is non-continuous and ably redeposited) were observed. The Eocene calcareous nanno- The history of the TSB basinfiU was strongly influenced by the ean be subdivided into discrete time slices. Studies of core #i~ plankton assemblages indicate pelagie conditions and are evolution of the Carpathians. Its sedimentary record is subdi- fundamentally different from the coeval nearshore assemblages vided ioto four teetonostratigraphic megasequences: Upper Cre- Facies materials (Baldi-Beke er al. 1981; Nagymarosy & Baldi-Beke -'~ Pannonian s. I. formations type 1993) have shown that only a few Cretaceous and Palaeogene of the neighbouring epicontinental Transdanubian Palaeogene taceous, Palaeogene, Lower Miocene, and Middle-Upper basin (BaIdi-Beke 1984; Nagymarosy & BaIdi-Beke 1993), Mioeene (Krezsek & Bally 2006). Nagyalföld Variegaled Cray swamp and nannoplankton zones can be recognized. ~~ Formation lacustrine The Szolnok Basin deposits overlie clastic deposits with proving the absence of a elose palaeogeographie relation. The Upper Cretaceous clastic sequence was deposited in a ,!e Zagyva Formation alluvial alkaline basaltie complexes of Early Cretaceous age. Deposition ~ The presence of Early Oligocene sediments is uncertain. The basin generated by the collapse of the Mid-Cretaceous Orogen }~~ o commenced during the Late Cretaceous and is represented by Oligocene part of the sequence comprises clayey marls (similar (Sanders 1999; Willingshofer er al. 200 I). The succession is up "'" Ujfalu Formation delta.fronl calcareous shales, marls, c1ayey and calcareous marls of the to the Kiscell Clay) with sandstone intercaiations. Lepidocyclina- to 1000 m thick and consists of coarse and fine-grained siliciclas- ~ A1gyö Formation delta-slope lzsak MarI. In the West Carpathians, the Upper Campanian to ~ hearing conglomerates are also recorded. The Oligocene nanno- ties and limestones deposited in continental and marine (both Lower Maastrichtian Puchov Formation represents an equivalent plankton assemblages are less pelagic and show more nearshore shallow and deep) settings. Deposition of the Palaeogene sedi- ~ prodeltawlth ;~"' '" Szolnok Formation gravity-transported for these beds. Turbiditic sandstones with graded conglomerates, ,1." features than the Eocene ones, suggesting that the depositional ments was coeval with a eompressional post-rifting phase ~ c1astlcs and rarely with breccias, are interbedded into the generaUy shaly :;i;1 environment gradually changed from pelagic deep-water to a (Krezsek 2005). The sedimentation rate was low but constant and transgressional unit. Based on the palaeoecology of foraminifers, a pelagic and shallower, nearshore one. the altemating marine and continental cycles are separated by and deep basin '""'" bathyal depositional environment is suggested for the Puchov two third-order sequence boundaries related to minor inversion I ~\ion deposits with local of the Palaeogene basin. During the Early Miocene, the flexural volcanlc activity Formation (Majzon 1966; Szepeshazy 1973). In some units, non- Transylvanian Basin (S.F.) calcareous and non-fossiliferous shales may indicate deposition sub-basin generated by the thrusting of the Pienides was devel- Fig.17.19. Lithostratigraphy and facies types ofthe Pannonian in below or elose to the CCD. The top part of the Cretaceous and The Transylvanian Basin (TSB) is surrounded by the Eastem and oped almost exelusively in the northem part of the TSB (up to Hungary. almost the entire Palaeocene are missing from the core material. Southern Carpathians and the Apuseni Mountains, and represents 1000 m of sediments). Several unconfonnities related to synsedi- 1076 M. W RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1077

mentary tectonic activity have been recorded in the shallow- to (e.g. Moigrad Formation). The Upper Rupelian is strongly Chronostratigraphy Sedimentary environments . B deep-marine sediments. transgressive, including dysoxic environments (bituminous shales ~:ii Central and Iithostratigraphic units Major tectonic ehaoges from the beginning of the Middle of the I1eaoda Formation). Standard Paratetliys Miocene (Badenian) transformed the TSB into a backare basin The Chattian is mainly siliciclastic with an overall prograda- ~r (Sanduleseu 1984), eharaeterized by a dominantly eompressional tional pattern and widespread continental deposition, probably P'ILQC;Ill.[I~... 5.332 ... c regime, and a high rate of subsidence between the Late Badenian generated by a eustatic sca-level fall and climate change. While 'm and the Early Pannonian. Early Badenian hemipelagie to shal- most of the southem part of the basin was exposed, and '" Late Badenian to Pannonian 10w-marine sedimentation (Iess than 100 m) was followed by an continental deposits were dominant in the Giläu and Mese~ area, (jj 1;;;1 .. 7.246 .•• NW uplifl and erosion important phase of Middle Badeniao evaparite deposition marine inner shelf (Bnza! Formation) and offshore to slope 15: .~ .. 9.0 ..• (300 m). Subsequent silieielastie deposition (up to 3000 m) (Vima Formation) deposits were dominant in the Preluca area. ::> :5 oeeurred in deep-marine (Late Badeniao), outer-ramp (Early The base of the Lower Mineene megasequenee (MS3) is t:: Sarmatian), shelf aod delta (Late Sarmatian to Pannoniao) coincident with deposition of the marine Vima Fonnation which ~1 .. 11.608 •• settings (Krezsek & Filipeseu 2005). Most of the Upper Mioeene was continuous aeross the Oligoeene-Miocene boundary. Subse- basin fill was eroded due to the post-Pannonian uplift and quent retrogradation was coeval with the transgressive event erosion. which was generated by the onset of eompressional teetonics and c (Jj which created 0 fiexural basin (Györfi el al. 1999). Microfannas ~ ::iii Sedimentary and stratigraphie development with Mediterranean affinities (Popescu el al. 1995) invaded the The Poloeogene megasequenee (Fig. 17.21 MSI & MS2) is basin, aod the overlying Eggenburgian liUoral sands of the Co",! Q) w =ü I~~ .• 13.0. divided by two uneonformities (Hosu 1999) into three sedimen- Formation preserve a typical assemblage of bivalves with Oopec- tary phases, eorresponding to the Daoian(?)-Early Priabonian, len gigas (Moisescu & Popescu 1980). Early Miocene maximnm ü~I~~ the Late Priabonian-Early Rupeliao and the Late Rupelian~ ftooding is assoeiated with the deposition of the Eggenburgian o Chattian (see also Filipeseu 200Ia). C10se to the KlPg boundary, Cheehi~ Formation, an offshore unit preserving diverse mierofau- ~ tectonic cornpression led to a major change in the depositionaJ nal assemblages with Globigerinoides Iri/obus (Popescu 1975). c' Badenian environments, initiating erosion and a change to alluvial fan and Following the deposition of the Chechi! Formation, the basin was III E fiuvial sedimentation (Jibou Formation; Hosu 1999). Fossil filled during the remaining Early Mineene with deep-marine e»: c vertebrales have been described from the lacustrine deposits in tnrbidites and eoarse-grained fan deltas belonging to the Hida III the vieinity of the Thaoetian- Ypresian boundary (Gheerbrant el Formation. al. 1999), while deep-marine deposits with Danian foraminifera Tbe base of the Middle to Upper Mioeene megasequenee ~1:ii ...t<;~rp. ... '70.6.' ... Formation), followed by a carbonate platform (Cluj Limestone) The marine fiooding event at the beginning of the Late o .•.. Campanian I/) with Crassostrea /ransilvanica and Nummuli/es jabianii. Maxi- Badenian (Popescu 1972; Dumitricä el al. 1975) was probably w Ü ::iii mum ftooding is indicated by offshore bryozoan marls (Brebi both globally aod regionally (increased subsidence rates due ~ .... 83.5 •... Formation) which also include the Priabonian-Rupelian bound- tectonic shortening in the Eastem Carpathians: Sändulescn 1988) w Santonian ary (Pycnodonle giganlica biohorizon). Progressive shallowing is controlled. Transgression resulted in the deposition of hemipela- c:: -85.8-- ü recorded in the overlying Hoia Limestone (skeletal packstones) gic sediments, subsequently overlain by the highsland prograding Basement (metamorphics, ophiolites and Permian to Coniacian sediments) and the Mera Formation (siliciclastic and calcareous). submarine faos of the Pietroasa Formation (Filipescu 2004). By Tectonic events at the end of the Early Rupelian led to a the end of tbc Late Badenian, inereased regional eompression Fig. 17.21. Lithostratigraphy of the Transylvanian Basin (based on Krezsek & BaBy 2006). progressive shift to fluvial and siliciclastic ramp environments resulted in a relative sea-Ievel fall and lowstand deposition. Due 1078 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1079

1.' 2.' 21" to the partieular tectonic setting, the total thickness of the Upper strike-slip boundary; this is a strongly tectonized terrain e. 22" Badenian ranges from a few metres (in the west) to > 1500 m (in 600 km long and 1-20 km wide. Tbe Outer Carpathians are the SE). formed by stacked nappes and thrust sheets, which show differ- '. :..::-':/':'. ':.:::'.:.:.<:::'>::'. ':\.:'::>. ':\:.:.:':.'.:'.::-".:.':.'.:',.:':.>:. The subsequent transgressive deposits near the Badenian- ent lithostratigraphic and structural development. From south to Sannatian boundary (planktonic foraminifera and Anomalinoides north they include: the Magura, Fore-Magura-Dulda Group, and '. ': . biozones) were followed by prograding submarine fans (Sarmatian the Silesian, Sub-Silesian and Skole units. In the Outer Car- :': ~:'.' Iris Formation). The subsequent sea-Ievel fall resulted in increased pathians the main decollement surfaces are located at different salinity in the basin (Varidentel/a reussi Biozone: Popescu 1995), stratigraphie levels. All of the Outer Carpathian nappes are f1aUy and extensive erosion in the northem part of the basin. Another overtbrust onto the Miocene deposits of the Carpathian Foredeep "':'::'.:.'~~':".-:.~., transgressive event (E/phidium reginum Biozone) was associated (Oszczypko 1998; Oszczypko & Toma. 1985). However, along with deltaic progradation (Dogie/ina sarmatica Biozone) (Krezsek the frontal Carpathian tbrust a narrow zone of folded Miocene & Filipescu 2005). By Late Sarmatian times, the onset of uplift deposits developed. In Poland these are represented mainly by \:::.'~.:>.'..~:i:.:::~Lii: :~::::~. a10ng the basin margins (Apuseni Mountains) resulted in the the Zglobice, and partially by the Stebnik units. The detachment '. deposition of deltas, fan deltas, coarse submarine fans (Feleac levels of the folded Miocene units are usually connected with Formation), and a major unconformity. Sarmatian deposits range Lower and Middle Miocene evaporites. in thickness between 300 m and >1000 m (in the basin centre). The overlying shallow-ramp and deep-marine siliciclastic Palaeogeography "~,~., deposits are associated with a new transgression at the end of the The Outer Carpathian Basin occupied the northern margin of Sarmatian (Porosononion aragviensis Biozone). This extended Neo-Tethys (Oszczypko 2004, 2006). Geomagnetics revealed that into the earliest part of the Pannonian (Lopadea Formation); the boundary between the North European Plate and the Central outer.ramp condensed sedimentation predominated. Fan deltas, West Carpathian Block was probably located 60-100 km south ramp and deep lacustrine sediments are typieal of the subsequent of the present-day position of the Carpathian margin (Oszczypko prograding systems (Krezsek 2005). The brief re-establishment & Sl~czka 1985; iytko 1997; Oszczypko 2006). The Outer of connections with the outer Carpathian region cau be inferred Carpathian sedimentary area can be regarded as the remnant of from a brackish marine ingression (Ammonia acme), generated an oceanic basin transformed into a foreland basin (Oszczypko by an extrabasinal relative sea-Ievel rise. Fan deltas, proximal 1999). Tbis basin developed between the colliding European crystalline core of Gryb6wunil lacustrine fans, incised channels and alluvial fan systems were continent and various intra-oceanic ares. The important driving theTatraMts. the most characteristic features of the middle part of the Lower forces behind teetonie subsidence in the basin were syn~ and High Tatra and Oukla unil Early Miocene flysch Pannonian. The subsequent transgressive and highstand condi- post~rift thermal proeesses as weil as the emplacement of the sub- Tatra units Miocene 01 the Carpathian tions are documented only in the eastern part of the TSB, and o Foredeep nappe loads related to subduction processes (Poprawa et al. Podhale flysch Fore-Magura uni!, Sambir - Rozniativ unit comprise an overall coarsening-upward succession (Vingard 2002). Similar to other orogenie belts, the Outer Carpathians m North European Platform Miocene deposits upon Formation). The thickness of the Pannonian deposits ranges from were progressively folded towards the continental margin. Ac- Pieniny Klippen Bell Silesian unit, the Carpathians 300 m (SW) to 500 m (SE). The Pliocene to Holocene evolution cording to the reconstructions of Roure el al. (1993), Roca et al. "' Andesites Magura nappe Zgtobice Unit of the TSB was characterized by uplift, erosion (Sanders 1999) (1995) and Behrman er al. (2000), the Early Oligocene Outer a- Malcov Fm. Sub-Silesian unil and structural complications produced by salt tectonics (Krezsek Carpathian Basin was at least 380 km wide. & Bally 2006). Fig. 17.22. Geological sketch map of the Polish Carpathians and their foreland basin. Abbreviations of facies-tectonic subunits of the Magura Nappe: 8u, Palaeomagnetism Bystrica Subunit; Ku, Krunica Subunit; Ru, Raca Subunit; Su, Siary Subunit. Volcanism According to Marton et al. (1995b) the Western Carpathians and Mid- to Late Miocene Carpathian deformation was accompanied its hinterland are characterized by a counterclockwise rotation of by intense magmatic activity in the volcanic are covering most of 80'. The first rotation of 50' took place during the Late -Early Cretaceous basin opening; Late Cretaceous- ka et al. 2000; Golonka 2004), resulting in the unification of the eastern margin of the TSB. Volcanic products sealed parts of Ottnangian to Early Karpatian and the second one (of 30') Palaeocene inversion; subsidence during Palaeocene to Middle facies, incIuding the position of the CCD level, as weil as low the Pannonian sedimentary record. There are several well-known occurred during the Badenian. Eocene times; and Late Eocene-Early Miocene synorogenic sedimentation rates. This general trend dominated the Early and volcanic tuff lithohorizons in the Badenian-Pannonian sedimen~ closing of the basins. In the Outer Carpathian area the KlPg Middle Eocene in the Skole, Sub-Silesian, Silesian and Dukla tary record of the TSB (Märza & Meszaros 1991), which are Sedimentary and stratigraphie developmelIl boundary is located within a continuous turbidite sequence. basins, as weil as in the northern part of the Magura Basin. The related to Neogene calc-alkaline, subduction-related magmatic The Outer Carpathians are composed of mainly Upper Jurassie The Palaeocene represents a time of major changes in deepest parts of these basins were occupied by hemipelagic, non- activity of the Carpathians and Apuseni Mountains (Pecskay et to Lower Miocene deep-marine deposits ('flysch') (Fig. 17.23). sedimentary conditions in the Quter Carpathian basins, ranging calcareous shales. During the Middle Eocene these shales passed al. 1995). The sedimentary successions of the main tectonic units differ in from uplift of the intrabasinal source areas to general subsidence up into shales with intercalations of thin-bedded sandstones terms of facies development and thickness. The thickest sedi- and a sea-Ievel rise. These changes are marked by the deposition (Hieroglyphic Beds). Outer Curputhiuns in Polund (N.O.) mentary cover belangs to the Silesian unit, which varies from .~ of thin- to medium-bedded turbidites, traditionally referred to as In the Magura 8asin, Palaeocene deposits are overlain by shales 3000 m in the west to >5000 m in the east. The thickness of the the 'Inoceramian Beds' (Bieda et al. 1963), and recorded from (up to 150 m), which pass upwards into the thin-bedded turbidites The Polish Outer Carpathians (POC) are part of a mountainous other tectonic units is markedly thinner and varies between ~1i the Magura, Dulda and Skole successions. The 300-500 m thick of the 200-600 m thick Beloveza Formation (Oszczypko 1991). ;;;~: arc that stretches for > 1300 km from Vienna to the lron Gate of 3000-3800 m in the Skole Unit, c. 1000 m in the Sub-Silesian units are characterized by calcareous, micaceous sandstones The upper part of the Lower/Middle Eocene succession comprises the Danube River at the Serbian-Romania boundary (near Unit, 2300-2500 m in the Dukla Unit, and 2500-3500 m in the ~ intercalated with day shales. During this time the evolution of the thick-bedded turbidites of the Magura Formation, which is Orsova) (Figs 17.16 & 17.22). In the west, the Carpathians are Magura Nappe (Poprawa et al. 2002). In terms of facies the Silesian Basin was still influenced by the Silesian Ridge, 1000-2000 m thick (Birkenmajer & Oszczypko 1989). Eocene linked to the Eastern Alps and in the east they pass into the distribution, thickness of deposits, and palaeocurrent directions from which non-calcareous, thick-bedded turbidites and con- deposition in the Magura Basin was controlled by the activity of an Balkan chain. The POC are c. 315 km long and 60-90 km wide, (only in the Magura areal, the Silesian and Skole basins can be glomerates (Istebna Beds) were shed into the basin. The upper accretionary wedge which developed on the southem margin ofthe and are located in southern Poland. considered as independent sedimentary areas. The Magura and part of the Istebna Beds comprises up to 200 m of shales. The basin during the Late Palaeocene collision between the Inner Silesian basins were separated by the Silesian Ridge, while the Lower Eocene is characterized by the occurrence ofthick-bedded Western Carpathian block and the Pieniny Klippen Belt. During the Tectonic setting Sub-Silesian area formed a submarine high dividing the Skole turbidites and conglomerates (up to 500 m), which form elon- Eocene the migrating load of the accretionary wedge led to firrther Traditionally, the Western Carpathians are subdivided into two and Silesian basins during the Late Cretaceous to Eocene gated lenses (Ci~Zkowice Sandstones). The northern periphery of subsidence and a shift in the depocentres to the north. As a result, a distinct ranges (Ksi~i;kiewicz 1977; see also Froitzheirn et al. (Ksi~kiewicz 1962). the Silesian Basin was dominated by marls with exotic pebbles long and narrow submarine fan developed. The northern, deepest 2008). The Inner Carpathians are considered to be the older Tbe sedimentary succession of the poe comprises four deposi- (sub-SiIesian succession). part of the basin, often below the CCD, was dominated by basinal range, while the Quter Carpathians represent the younger range. tional megasequences, which reffeet the main stages of basin During the Eocene, a broad connection between the Quter turbidites and hemipelagites. The sedimentation rate varied from Between them, the Pieniny Klippen Belt represents a Cenozoic development (Poprawa et al. 2002; Oszczypko 2004): Middle Carpathian basins and the world oceans was established (Golon- 6-18 mlMa on the to 103-160 mlMa on the outer 1080 M. w. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE

fan, and 180-350 mlMa in the area affeeted by the middle fan-lobe North Alpine Foreland Basin and northwards into the systems (Oszezypko 2004). The fan was supplied from the SE, Carpathian Basin. The basin is c. 210 km long and c. probably from lhe Inner Carpathian/lnner Daeidearea. wide, rl'g During the Priabonian and Rupelian, uplift in the Outer 'cß ~äJ Carpathian Basin (Poprawa et al. 2002; Oszezypko 2004) was Tectonic setting aeeompanied by the transfonnation of the Outer Carpathian The CCF is a peripheral foreland basin that developed due to remnant oceanic basin ioto a foreland basin. Ihis led to the subsurfaee loading of Ihe Alpine-Carpathian orogenie belt on the rl"" I~ replaeement of deep-water shales and basinal turbidites by passive margin of the Bohemian Massif. The CCF exhibits ~E {~ Qi~ pelagie Globigerina Marls, followed by Oligoeene bituminous striking lateral variations in terms of basin width, depth, and the ~~ ~~~l Menilite shales deposited in the newly restrieted basin. Tbis type stratigraphy of the sedimentary infill. There are also variations in ~ E 0 <,I) Ql of deposition dominated all of the Outer Carpathian basins, :J :6~ .~) pre-Neogene basement composition and tectonic subsidence. The Cl exeept for the main part of the Magura Basin (Van Couvering et Cll ~[)lö.g main area of subsidence shifted from the south, in the Late :2 ~.~ al. 1981). During that time, the pelagie Globigerina marls and Oligocene/Lower Miocene to the north in Middle Miocene times. 01.0 Menilite shales of the Magura Fonnalion, as weil as the 0:"Cf) This reflects the change in orientation of the main convergence m~ turbidites of the Maleov Fonnation (MiddlelUpper Oligoeene), direction and a generally eastward-directed lateral extrusion of . ~ were deposited in the SE pari of the Magura Basin. The the Carpathian blocks. The reaetivation of NW -SE and NE-SW northemmost part of the Magura Basin, whieh was supplied from ~~ trending basement faults was also important for the basin shape .~ .5 I~i the NW (Silesian Ridge), is eharaeterized by Middle Eoeene Cf) " E~ ~ and for its extent. The southern part of the CCF had a Cf) shales that pass upwards into marls and thin-bedded turbidites complicated evolution due to its position at the junction between I (Zembrzyee Beds, Upper Eoeene), thiek-bedded glaueonitie ~iQ E 0 i the Eastern Alps and the Western Carpathians. ~ ~ sandstones (W~tkowa Sandstone, Lower Oligoeene), and finally OCl ~I~ into glauconitic sandstones and marls (Budz6w Beds, Oligocene) u..Cll >-. >- Sedimentary and stratigraphie development i (Oszezypko-C1owes 200 I). In the marginal parts of the Outer :2 Deposition in Ihe CCF began in Egerian-Early Eggenburgian ~ Carpathian basins, G/obigerina Marls pass into Menilite Shales ~D times (Fig. 17.24). Terrestrial (alluvial and ftuvial, Zerotiee (up to 250 m thiek) with ehert horizons at the base. The Menilite Cll Member) and deltaie sediments oeeur loeally at the base of the 32 i Shales, whieh eontain lenses of thiek-bedded sandstones (Cergo- :J ! succession in the SW of the basin. During the subsequent ,; wa and Kliwa Sandstones), gradually pass upwards into a Q . . transgression from the south, SE and east, these deposits eomplex of thiek-bedded, medium-grained, ealeareous sandstones ~ -g.s progressively passed into marine ones (clastic coast and shallow- ~ (Lower Krosno Beds, up to 800-1000 m). Higher up in the a ]~. m marine environments). The shallow-marine fades (about 40 m succession, thin-bedded, finc-grained sandstones pass into marly i palaeowaler depth) was interdigitated with lagoonal and deltaie ~i~ shales (Upper Krosno Beds, Early Mioeene, up 10 3000 m). •.. .9 e ¥ deposits (Nehyba er al. 1997). The upper part of this Lower o These lithofacies are diachronous across the Silesian, Sub- ~~i Miocene succession comprises deltaic and clastic coast deposits Cll ~ Silesian and Skole basins (Sl~ezka & Kaminski 1998). '00" ;£ (Cejkoviee Sands). The souree area was lhe deeply weathered Following the phase of Late Oligoeene folding, the Magura margin of the Bohemian Massif. A distal rhyolite airfall tephra ~ IEl Nappe was thrust northwards onto the terminal Krosno Basin. ü5 .s horizon oeeurs in the Upper Eggenburgian (Nehyba 1997). 'ö This resulted in the final phase of subsidenee in the Outer Dunajovice and Dyjakovice sandstones and the Dobre Pole ., Carpathian Basin (Late Oligoeene-Early Mioeene). Subsidenee '" Claystone (glauconitic sands and calcareous clays with rich was accompanied by a progressive migration of the depocentre foraminiferal fauna) were deposited under marine conditions in ! axes towards the north and increased depositional rates ranging the SE part of the CCF during Early Mioeene times (Ad3mek ue!sal!S 5 from 350 mlMa in the Rupelian (northern part of Magura basin) ! 2003; Chlupac et al. 2002). Eggenburgian deposits also oeeur in qns to 600 mlMa at the end of the Oligoeene (SE part of Silesian ~ the northern part of CCF in the area of Oslrava. Basal ftuvial Basin). During the"Eggenburgian a piggybaek basin developed on sands and gravels pass upwards into marine claystones, bryozoan i the Magura Nappe (Zawada and Kremna fonnations, at least :'I limestones, sandstones. and conglomerates (Jaklovec Conglomer- Q) ! 550 m thick) and a marine connection with the Vienna Basin via ö '0 ate) (Chlupac er al. 2002). Lower Mioeene basaltie voleanism is -'" ~~ ~ Orava was established (Oszezypko er al. 1999, 2005; Oszezypko known from the Opava region. cn & Oszezypko-Clowes 2002, 2003). A seeond depositional eyde is eonfined 10 Ihe middle Early i Mioeene (Ottnangian) and was related to the onset of thrusting, t Volcanism z ~ ;,<: whieh led to markedly different depositional histories in the z ~ ::: ~ z The final stages of tectonic evolution of the Polish Outer proximal. and distal parts of the CCF. In the distal (western) part, z ~ z z ~ ~ .t .s Carpathians were associated with volcanic activity related to a6elS Ii] ~ >! 0 " I;j ~ " :'I 'ö the deposition was direeted by the interplay of basement relief, z Ci '5 " z z subduetion beneath the front of the Carpathian are. In Ihe (J ~ ~ ~ ~ :'i u ~ 0 sediment supply and eustasy, while Late Eggenburgian thrusting ~ ;li 3 ~ 11 '" !j Kroscienko-Szczawnica area small andesite intrusions are located '" .. le affeeted the deposition in the proximal parts of the basin. The W ~3M01 ~3ddn ~3MOl along the northern margin of the Pieniny Klippen Belt. The time }:j3ddn 3100lV'j t13MOl ~ deposition of a synorogenic clastic wedge, related directly to S8!J8S l:I3ddn I"H3MOl o 3N3:JOIl"j 3N3:JO~ll0 3L)fl of the volcanic activity in this area has been dated as 3N3:J03 3N3:J03lVd ~ flexural subsidence due to the thrust loarling, reflects this change ~ ~ 11.35 :f: 0.45 Ma (Birkenmajer & Peeskay 2000). walsAS .~ 0 3 N I (Nehyba 2004). At the base of Ihe sueeession a typieal basal ., 3N3~03"1"d ".l3~1:> ~ ~ .~ forebulge uneonfonnity oeeurs (Crampton & Allen 1995). To- . , "E i l;arpathian Foredeep in the ezech Republic (S.N., N.D., wards the passive margin, the unconformity is overlain by eJ3 :> o z N o 3 :> 'OS31N ~ d S.H., RR) progressively onlapping sediments above an increasing strati- ~I:::J eV'jUleW!l 1 graphie gap. Changes in the heavy mineral speetra (Nehyba & ~ ~ ~ g g ~I ~. ~ '!I Sl ~ g ~ b {2J Tbe Carpathian Foredeep in the area of the Czeeh Republie Burianek 2004) refteet the new situation. Braekish to ftuvial ;:i (CCF) is limited to the NW by the passive margin of the sands and days (Vitoniee Clays), and sands and gravels of the ~ Variscan Bohemian Massif and its Mcsozoic platform cover and Rzehakia Beds, eomprise Ihe Ottnangian deposits in the distal •• by the overriding nappes of the Western Carpathians in the SE. parts of the basin. These deposits (with the endemie bivalve The CCF eontinues southwards into the Austrian part of the '" Rzehakia socialis) were recognized in the Miroslav and Frydek- 1082 M. w. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1083 .,I/) I Massif; marshes were established on the continental rnargin have a tbiekness of about 200 m (RüZieka 1989) in this area s-Cll ,.,I/) Carpathian Foredeep (Czech Rep.) (Dohikova & Slamkova 2003). In the northern part of the CCF, (= Lower and Upper Fonnation). E the upper Lower Mioeene (Karpatian) deposits are represented ::;:'" 11I CDf!5 GI GI GI iicS by the Stryszawa Formation comprising terrestrial basal con. .S I/l 0;: Cl C"lU Carpathian Foredeep in Po/and (N.O.) Cll ,go South & Middle North glomerates, sandstones and claystones, and lacustrine/lagoonal E ->- GI a I " Cll ll. siltstones that pass into marine deposits (claystones and silt~ Tbe c. 350 km long Polish Carpathian Foredeep Basin (PCFB) is F tJ) tJ) tJ) I - ., stones, and subordinate gravels and sandstones). Clays, silts, I~ a:: part of a large sedimentary basin that stretehes from the Danube sandstones and eonglomerates with gypsum form the uppermost in Vienna (Austria) to tbe Southern Carpathians in Romania a: part of the sueeession (Adamek el al. 2003). (Fig. 17.22). Towards the west it is replaeed by the North Alpine w Teetonic aetivity along the aetive margin affeeted the deposits Foreland Basin. The width of the PCFB varies from 30-40 km in 0.. TORTONIAN 0.. Pannonian of the CCE Sediments in the foreland of the Carpathian nappes the west to 90 km in the Rzeszow area and 50 km at the Polish- :) were shingled and staeked in the form of duplexes. Sandstones, Ukrainian border. It can be subdivided into an 'inner' and the eonglomerates and clays (gravity current deposits) in front of the 'outer' part. Tbe boundary between them runs along the Zdanice Nappe in the middle part of the basin belong to the Carpathian Tbrust. Sarmatian Kromefii Member. SERRAVALLIAN During the early Middle Mioeene the CCF geometry was Palaeogeography I reorganized, beeause the NNW- and NW-directed eompression The Early to Middle Mioeene PCFB developed as a peripheral ~dayS __ ..o:::;' sands of the Carpathian orogenie wedge ehanged to a NNE- and NE- foreland basin and is related to the advaneing Carpathian Front U I I w direeted compression during the Late Karpatian and Early (Oszezypko 1998; Oszezypko et ul. 2006, and referenees there- Cl-' Badenian. In the soutb, deposits are loeated in the eenlral parts in). During late Early Mioeene times the Western Outer Cl I :E of the basin at some distanee from the passive and aetive basin Carpathians overrode the European platfonn. The load of the v~ margins. The areas with the maximum sediment thiekness are Carpathian nappes resulted in Ihe development of a 25-50 km Badenian algal 151-1 IW marly clay situated along the basin axis forming an almost symmetrie basin wide Early Mioeene flexural depression (inner foredeep). This LANGHIAN ~ limestones I~I~ =~=~=~J I £; with a SSW-NNE orientation. Deposits of eoarse-grained basin developed botb on tbe top of the advaneing Carpathian 0 Z Gilbert deltas, eoastal environments, lagoonal deposits and Front and on the platfonn basement. The relatively narrow basal deeper-marine deposits have been reeognized. These are partly brackish or freshwater, moat-like basin was filled with coarse W W c1astics eorrelated with the Grund Fonnation in the North Alpine clastie sediments derived from the emergent front of the Outer Z Kromefii Foreland Basin. The maximum thiekness of the deltaie gravels Carpatbians and from the platfonn. The Lower Mioeene deposits N w and gravelly sands is about 175 m. Deltas are loeated along of the inner foredeep fonned a c1astie wedge along the Northern IC) Karpatian Fonnation Ü both basin margins. Abundant intraclasts (sometimes several Carpathians, comparable with the 'Lower Freshwater Molasse' of 0 -0 metres in diameter) reftect cannibaHzation of tbe older basin the weslern North Alpine Foreland Basin. ::1: Rzehakia I g - - ~ Rzehakia infil!. In the northern part of the basin, the basal eonglomerates Latest EarJy Miocene times were characterized by the develop- 0 I Member Member and sandstones may have been deposited in marine environ- ment of SW-NE and NW-SE trending grabens. Subsidence, W Ottnangian BURDIGALIAN ments (Chlupae et al. 2002). The deeper-marine deposits (c. wbich affected both the inner and outer foredeep, was aecompanied rhyolite 600 m) eomprise mudstones with silts, clays and shell debris. by the Early Badenian transgression (Oszezypko 1998; Oszezypko Z tuffI&11 Z - - - - These are interpreted as outer-shelf deposits or hemipelagites. el al. 2006) whieh flooded both the foredeep and the marginal part ------sandy The presence of otoHths confirm a palaeowater depth of about of the Carpathians. Simultaneously, the shoreline shifted north- I: 201-1 a: 400 m in the eentral part of the basin (Brzobohaty 1997). wards, from 30-40 km to 100 km in the western and eastern parts ~ w ~ = = := := = = = claystones ji ;;: Divakyl Coastal and lagoonal deposits, as weil as occurrences of algal of the basin, respeetively. The palaeobathymetry of the Early 0 _ - ..., ~"'

about 1200-1300 mlMa, and was aeeompanied by a sedimenta- Badenian-Sarmatian sandstones and shales (Gazdzieka 1994), lJl tioo rate of ooly 1000m1Ma. Towards the NE margin of thc whieh display large-seale cJinoforms (Krzywiee 1997). During E Polish Carpathian Foredeep PCFB, the subsidence and sedimentation rate decreased to 100- the early Sarmatian, littoral carbonates and c1astics were depos- t_~ 200 m/Ma. The area of maximum Sarmatian subsidence was the ited. After the Sarmatian the final northward thrust moved the GI:rl GI ~~~ Wielkie Oczy Graben. Thc total subsidence in this zone varied Outer Carpathians onto the PCFB. .S;~ I ra I 1ii ';: ~ ~ ; E European 0 from 1500 m in its NE part to 3000 m in the SE. ~ .t ~ ~ Ci) .~ ~ Western Eastern Platform A reIalively narrow belt of deformed Upper Badenian- a: Sarmatian fnredeep deposits known as the Zglnbiee Unit erops Carpalhians in Western Ukraine (0. Y.A., V.V.A.) out al the front of Ihe Polish Outer Carpathians (Kotlarezyk Four main struetural units are recognized in the Western Ukraine er 1985; Ksi~kiewiez 1977). This unit eonsists of several fault- from west to east (Figs 17.4 & 17.16): the Transearpathian Basin, ~ TORTONIAN and-fold struetures with a maximum width of up to 10 km. To the Carpathians, the Carpathian Foredeep, and Ihe Volhyno- n. :J thc west of Krakow, there is a narrow zone of foIded Miocene PodoJian Plate (i.e. the SW margin of the East European deposits (Ksi~zkiewiez 1977). In the western part of the Platform). The Mukatehevo and Solotvino sub-basins are part of ------Carpathians (Andryehow-K,ty areal several thrust sheets of the the Transcarpathian Basin which is separated from the Romanian ------_._------Sub-Silesian Unit, eovered by lower and upper Badenian de- Transylvanian Basin by the Maramures, Lepus, Rodna and ------posits, are recorded. These sheets are thrust onto the Badenian Preluka mountains. To the SW the basin is bordered by the Great deposits in the outer PCFB. Hungarian Plain. The Mukatchevo and Solotvino suh-basins are o I I w I SERRAVALLIAN divided by the voleanie Vyhorlat-Hutin Zone (Voznesensky Sedimentary and stratigraphie development 1988). The PCFB is asymmetrie and filJed with predominantly elastie o...J o Mioeene sediments (Oszezypko cl a/. 2006) (Fig. 17.25). The Palaeogeography and tectonic setting ~ outer foredeep is filJed with Middle Mioeene (Badenian and The pre-Neogene basement of the Transcarpathian Basin consists 8adenian Sannatian) marine deposits, which range from a few hundred of Palaeozoic to Palaeogene units. In Neogene times, the 15 H I W LANGHIAN _ metres thiek in the northern part to 3500 m at the Carpathian Solotvino Sub-basin underwent maximum subsidence during the Front. The inner foredeep, loeated beneath the Carpathian Badenian and up to 2000 m of sediments were deposited, while o I Z ~~~~~~.~~~~~~.~~==:=:=:=:=:==:=:=:=:=:=:=:= nappes, is composed of Lower to Middle Miocene autochthonous the deposits in the Mukatehevo Sub-basin are >2500 m thiek. deposits. Thc Lower Miocene strata are mainly of terrestrial Generally, the suceessions are comparable with those of the W UJ Platform Sasement origin, whereas the Badenian and Sarmatian sediments are Great Hungarian Plain and the East Slovak Basin. The deposits z marine. Tbe deposits of the Carpathian Foredeep are underlain are usually only slightly deformed. Close to the Chop- Vysehkovo NI", UJ \J t> Karpatian conglomerates by Perroo-Mesozoie terrestrial and shelf sediments and loeally by Antieline, however, beds dip at up to 90° and displacements of c. Palaeogene deposits. The platform basement, with a Neogene 20 km are reeorded in the northern part of the Solotvino o ~ algal vermelid limesIones sediment cover, dips southward beneath the Outer Carpathian depression (Voznesensky 1988). nappes for al least 50 km (Oszezypko & Sl~ezka 1985; The Carpathian Foredeep is situated to the NE of the o I :2 olislostrome Oszezypko 1998). Carpathians Front and is divided into an inner and an outer zone. W BURDIGALIAN Ottnangian sandstones The oldest Miocene deposits were found in a sub-thrust The inner zone consists of the Boryslav-Pokuttya and Sambir position in a few borcholes in the western inner foredeep, and nappes whose development was eaused by the uplift of the Z Z fresh-water limesiones comprise marine mudstones of late Egerian-Eggenburgian age Carpathians. The Boryslav-Pokuttya Nappe overthrusts the Sam- (Gareeka el a/. 1996; Oszezypko & Oszezypko-Clowes 2003). bir Nappe (Kulehytsky 1989). The flexural downbending of the 20 f- I er variegaled c1aystones Higher up in the sequence, slide deposits attain a thickness of up w outer zone eommenced in the Badenian. The subsequent post- variegated claystones to 370 m. The overlying Karpatian deposits comprise coarse- to W ~ Sarmatian folding resulted in complex deformations in the inner ...J medium-grain«l, polyimietie eonglomerates and are followed by zone, but did not affeet the outer zone (Vialov 1986). Tbe :::::::::: ::.::::::::::::. siltstones & mudsiones a eonglomerate-sand-mudstone unit up to 650 m Ihiek. The Sambir and Boryslav-Pokuttya nappes were detaehed from their upper part of the succession may have been deposited in an basement and moved c. 25-30 km. Sedimentary cover attains a o I I I Egerian ~~~~~~:~~~~~~: gypsum&anhydrites alluvial fan setting. In the Cieszyn area, the Lower Miocene thiekness of up to 6000 m. AQUITANIAN :::: :::::: ::.::::::::::::. mans & marly elays foreland deposits are overlapped by a 40-90 m thiek unit of Late ------Karpatian transgressive conglomerates. :. ~~:. ::::~:. ~:.:.:: salts Sedimentary and stratigraphie development ------.- - - - -_. The Badenian sediments rest directly on the platform base- The lowermost deposits of the Transcarpathian Bssin are of ::::::::::::.::::::::::::. rc--oI bioca!caren,.tes ment, exeept for the SE part of the inner foredeep, where they Eggenburgian age and comprise up to 90 m of sandstones, ------~ overlie Lower Miocene deposits. The thickness of the Lower siltstones and sandy clays (Burkalo Formation, zone NN3; ~1J~.~:i.~.-~~:;.-.-~ tuffites Badenian dcposits is variable, ranging from 1000 m in the Andreyeva-Grigorovieh cl al. 2002). Karpatian deposits are western inner foredeep (Skawina Formation) to 30-40 m in other 0.: I 0 I CHATTIAN I ~;1.:SI:'ti 1 .:el~.) t1". lilhoslratigraphic unit represented by the Tereshul eonglomerates (up to 100 m), . ~~~'m'~~~;,o •••• ~. •••• ~.. \.!..I parts (Baranow Formation) (Ney el a/. 1974). Sedimentation of eomprising unsorted boulder-pebble eonglomerates. The con. -.i!1""fi'~~,. II'•.Li!1,. ~L"9. the Skawina Formation (cJays and sands) began during the glomerate components are slightly rounded and consist mainly Fig. 17.25. Regional stratigraphie scheme of the Miocene deposits of the Polish Carpathian Foredeep (after Oszczypko 1998; Andreyeva-Grigorovich et al. Praeorbulina glomerosa Zone in the inner foredeep and during of Jurassic and Cretaceous limestones, sandstones and clays- 2003). Lithostratigraphic units: I, AndrychOw Formation; 2, Zebrzydowice Formation; 3, Sucha Formation-flysch olistoplaquc; 4, Stryszawa Formation; 5, the Orbulina suturalis Zone in the outer foredeep (Garecka et al. tones derived from the Palaeocene (Andreyeva-Grigorovich et 1996). The mid-Badenian evaporitie horizon (Iower part of the Debowiec Conglomerate; 6, Skawina Formation; 7, Sypka Gora conglomerates; 8, Krzyzanowice Formation; 9, Wieliczka Formation; 10, Gliwice beds; a/. 1997). The overlying Middle Mioeene (Badenian) deposits 11, Kedzierzyn beds; 12, Baranow bcds; 13, Chodenice and Grabowiec beds; 14, Krakowiec beds; 15, sulphur-bearing limestones; 16, algaJ-vermetid Teef NN6 zone; see Peryt 1997; Andreyeva-Grigorovieh et a/. 2003) are represented hy the Novoselitsa and Tereblia formations, limestones; 17, Biocalcarenite ofthe Chmielnik Formation. either overlies these deposits or rests direetly upon the platform eomprising rock salt (up to 270 m) whieh formed as a result of basement. This evaporitic horizon eonsists of rock salt, clays- a marked regression (Vialov 1986; Voznesensky 1988). The tones, anhydrite, gypsum and marls. Between Wieliezka and marine Novoselitsa Formation and the lower parts of the marine environments as refleeted by thc deposits of the whieh were mainly deposited in the Mukatchevo Sub-basin in Tarnow, the thiekness of the salts reaehes 70-110 m (Garlieki Tereblia Formation have nannoplankton assemblages of the NN5 Solotvino, Teresva and Baskhev formations. During the Bade- lagoonal and terrestrial environments. Upper Mioeene and 1968) and deereases towards the east to a few dozen metres. The zone, while NN6 zone assemblages occur in the upper part of nian, separation into the Mukatehevo and the Solotvino sub- Pliocene sediments are represented by the Iza, Koshelevo, mid-Badenian evaporites are overlain by thick (up to 1.5 km in the Tereblia Formation (Andreyeva-Grigorovieh et a/. 2002). basins oecurred. Sarmatian units are represented by the clays, Ilnitsa and Chop formations, which are restrieted to the the central part, and up to 2.5 km in the eastern part) Upper The Late Badenian transgression led to the establishment of sands and tuffs of the Dorobrativ, Lukiv and Almash formations, Mukatehevo Sub-basin. These are mainly voleanie and terrige- 1086 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1087 oaus deposits, including important lignite seams (Voznesensky of sandy clays with sandstones rieh in pectinids. The overlying the Southem Alps formed their southem continuation. Southem in the development of the Cenozoic volcanism of the Venetian 1988). Tirass Formation (up to 40 m) is characterized by evaporites Alpine units in NE ltaly inelude: (a) Palaeozoie basement; area (e.g. Doglioni & Bosellini 1987). In the NE Veneto, the Eo- In the Inner Carpatbian Foredeep the Boryslav-Pokuttya and which are overlain by the laminated clays and siltstones of tbe (b) Pennian-Pliocene sedimentary cover, inc1uding continentai, Alpine phase produeed overthmsts and WSW-verging folds Sambir nappes eomprise the Polyanytsa, Vorotysheha, Stebnyk Kosiv Formation (up to 700 m), ineluding an important bed with platform and basinal deposits; (e) voleanie and subvolcanie which completely deformed the Permo-Cenozoie sedimentary and Balyeh formations (Vashehenko & Hnylko 2003) (Fig. 17.8). radiolariaos (20 m) (Vialov 1986). The Lower Sarmatian is deposits, mostly occurring in the Dolomites-Recoaro (Mid- cover. Ca1careous days, siltstones, sandstones, conglomerates and olisto- represented by the Dashava Formation, up to 5000 m Ibiek, Triassie) and Colli Euganei-Monti Lessini areas (Palaeogene), The Neo-Alpine tectonic phase aeted during Ibe Neogene and stromes are eharaeteristie of Ibe Polyanytsa and Vorotysheha comprising c1ays with sandstones and tuffs. and (d) a thiek sueeession of Quaternary alluvial deposits filling reached its acme during Late Mioeene-Plioeene times. Much of formations. The Polyanytsa Formation is absent in the Sambir the Po PlaiD. The Variscan and Alpine orogenie cycles are the uplift of the Venetian mountains, and the fonnation of a Nappe and the Vorotysheha Formation has only a restrieted Volcanism recordcd in this area. The fonner involved pre-Permian thrusting, series of south-verging overthrusts which progressively migrated distribution. The Polyanytso Formation is usually assumed to be The Neogene magmatism of the Transcarpathian is eharacterized polyphased folding and metamorphie imprinting of the basement towards the Venetian plain, are due to this eyele. Although the ofEggenburgian age (Andreyeva-Grigorovieh el al. 1997; VekJieh by intensive volcanic activity. It was associated with the flexural whereas the latter is reeorded by the Dinarie (Palaeogene) SW- Venetian and Trento area constitutes one of the lesser deformed el al. 1993), although there is some evidenee that sedimentation subsidenee of the Transearpathian region along deep faults, vergent thrusts and by the widely distributed deeollement cover, regions of Ibe Soulbern Alps, the geometry of the Neogene eommeneed during the Oligocene (Vashehenko & Hnylko 2003). whieh aeted as eonduits for the upwelling magmas. The thiekest basement nappes and transfer faults ofthe Neo-Alpine (Neogene) deformation is rather eomplex (Doglioni & BoselIini 1987). The boundary between the Polyanytsa and Vorotysheha forma- accumulations of tufTaceous and effusive rocks were deposited south-vergent episodes, prograding toward the Po Plain foreland. In the Veneto region, Neo-Alpine tectonic activity is indicated tions is diachronous and ranges from the Oligocene-Miocene (1) during the Early Badenian in the eentral part of Solotvino The Friuli Platform and the Julian Basin eontinue southwards mainly by south-verging overthmsts. Just south of the Dolomites, boundary up to the Eggenburgian. Sedimentation of the Vorotysh- and the eastern part of the Mukatehevo basins, (2) during the to the Adriatic and Dinaric platforms, and the Bosnian Basin, the overthmsts also involve the erystalline basement (Valsugana eha Formation lasted until the Badenian, but its upper boundary is Badenian and Sarmatian in the Beregovo and Vyshkovo areas, respectively (Cati el al. 1987; Herak 1987). Cati el al. (1987) Lineament, Pieve di Cadore Lineament; e.g. Doglioni 1984). To also diaehronoos (Vashehenko & Hnylko 2003). Sandy-argillae- and (3) during the Plioeene in the Vyhorlat-Hutin Zone. have proposed a scenario with an additional Friuli Basin that the south, in the Venetian Pre-Alps, the sedimentary cover is eous sediments characterize the Ottnangian to Lower Badenian Badenian volcanism was characterized by acid liparite-dacitie subdivided the Friuli Platform into SW (SW of Pordenone) and deformed by fo1ds and overthmsts. The presenee of a basal Stebnyk Formation in the Boryslav-Pokuttya Nappe. In the Sambir and daeitic lavas and their associated tuffs. From the Sarmatian NE (Udine area and south of Udine) sectors. This basin decollement surface, consisting of Upper Permian evaporites, is Nappe the basal part of the Stebnyk Formation is cut by thmsting, to thc Pliocene, the acid vo1canism was replaced by intermediate, supposedly eontinued to the Outer (= Extemal) Dinarides. As a still under debate. Neogene deformation in the SW part of the 11: and passes upwards into the sandy-argillaceous Karpatian, to and later by alkaline, volcanism, Le. andesites, andesite-basalts eonsequenee, the SW and NE Friuli platforms should be Venetian area (Le. Monti Lessini, Monti Beriei, Colli Euganei) is Lower Sarmatian Balych Formation. In the NW of the Sambir and basalts (Voznesensky 1988). eonneeted with the Adriatie (present-day Dalmatian zone) and rare. Folds and overthrusts occur. in the westemmost part of the Nappe, the Balyeh Formation is overlain by the Radych Conglom- Dinarie (present-day High Karst zone) platforms, respeetively. Monti Lessini and in the Monte Baldo; these are SE-verging and erates (Vashehenko & Hnylko 2003). are linked to the Late Miocene Giudicarie compression (Castel- The Outer Carpathian Foredeep was generated on the and Dinarides: overview (D.B.) larin 1981, 1984; Grandesso el al. 2000). Diaehronism in the margin of the East Europaean Platform, where thick marine, Soutkern Alps in ltaly: Venetian Pre-Alps (D.ß" G.ß., The Southern Alps are separated !Tom the Eastern Alps (i.e. deformation of the Southern Alps was noted by Castellarin & brackish and continental Neogene sediments overlie Proterozoic, RM., J.H.N.) Austre-A1pine units) by the Periadriatie Lineament (PAL) (Fig. Vai (1981), who showed that the main shortening event in the Palaeozoie and Mesozoie deposits (Kulehytsky 1989). The Mid- 17.26). In terms of palaeogeography, both units are eonsidered to The Palaeogene of the Southern Alpine area of NW Italy western area of the Southem Alps occurred during the Late die Mioeene (Badenian) sueeession begins with the Bogorod- represcnt the northem extension of the Adriatic Micropiate which encompasses parts of the Trentino-Alto Adige and Veneto Oligocene to Early Miocene, as marked by the coarse-grained ehany Formation (e. 100 m thick) whieh is characterized by also includes the Po Plain and the adjacent . Ouring regions. At the beginning of the Cenozoic, this area. was clastics of the Lower Gonfolite Group, whereby the eastern area marly-tufTaeous sediments (up to 40 m). Its upper part eonsists the Palaeogene, when the Eastern Alps formed an arehipelago, subdivided into two basins whieh are roughly separated by the experienced the elimax of deformation during the Late Miocene present-day north-south alignment of the Brenta River. and Pliocene. From the Chattian to Langhian, the Lessini Block can be r-voQ\1>~ Palaeogeography and tec/onic setting considered as the foreland basin of the Dinaric Range (Massari The western basin, encompassing the Monte Baldo and Monti el al. 19800). An important palaeogeographie and geodynamie ",(I>~~'1>'~ Pan non i a n Lessini, the Monti Berici and Colli Euganei as weil as the change occurred in the Mid-Miocene with the onset of a maj,or Vincentin Pre-Alps, is characterized by widespread Palaeocene, phase of extension in the Pannonian Basin and the Inner Basins Lower-Middle Eocene and Oligocene volcanic activity and by Dinarides (Horvath 1984). The ongoing northward eonvergenee the deposition of shallow-water carbonates. The Eocene succes- of Adria and Europe culminated in .3 major Upper Miocene 0;;,v- s ../ sion comprises senes of shallow-marine platform systems and compressional phase, whose effects were widespread across the oS er"'o ~ IJ y.s t e m related basinal units. Some areas became emergent in the Early Alps and Apennines. Major south-verging thmsting, uplift and "1v~ (J:q~tJ, dsi'~'-'~'~ Oligocene, while others were sites of shallow-marine siliciclastic southward teetanic progradation occurred in the Venetian area (J ~;

margin (Winterer & Bosellini 1981). It was a region of shallow- resedimented ealearenites (P. Mietto, unpub!. data). Further to the Avesa in the Verona hills. Here, a 70 m thick succession of deposition of paralic fades including the famous Ronca. horizon marine carbonate accumulation until the uppennost Early Juras. west, in the western Lessini Shelf, shalIow-marine carbonates bedded marls and marly limestones (= Pietra Gallina; Hottinger (Oe Zanehe & Contemo 1972). During the Bartonian, suhaerial sie. The platfonn was drowned during the Bajocian to Kimmer- predominate, including many of the famous fossiliferous local- 1960) is deposited above hardgrounds on top of the Seaglia volcanic activity led to the formation of the Monte Calvarina and i/i idgian and formed a deeper shelf eharaeterized by the famous ities found in the Monti Lessini (Oe Zanehe & Contemo 1972; 'I' rossa. Monte Faldo, and the original Alpone-Chiampo Graben was 'I; 'Rosso Ammonitico Veronese'. Lower Cretaceous-Lower Eocene Mietto 1975; Besehin el al. 1998). The poorly studied western In the western Lessini Mountains (Fumane area), micritie and replaced by an emergent volcanic ridge on which muddy and sediments ('Maioliea', 'Seaglia rossa') (Fig. 17.27) are of deeper- margin encompasses the central-eastern Lessini Shelf up to the ~V marly limestones with planktonic foraminifera range in age from lignitie sediments were deposited (Yalle dell'Agno; Barbieri el marine origin (Bosellini 1989). Ouring the eomplex eollision San Bonifacio hills. Thanetian to Lutetian (Ungaro 1990; Garavello & Ungaro 1996). al.1991). between Europe and the Adria Plate, the former Trento Plateau In the SE Monti Beriei an important tectonic threshold, These limestones are overlain by e. 50 m of Middle Eoeene The Bolea area has been studied sinee the end of the reaeted rigidly and was hloek-faulted; the submerged Trento probably coincident with the Riviera Berica area, has been nummulitic calcarenites (Formazione di Avesa; Sarti 1980; nineteenth eentury (Oppenheim 1894; Fabiani 1912, 1914, 1915; Platform was segmented into separate blocks, showing variable identified; commencing in middle Eocene times, this boundary Ungaro 2001). In the western Monti Lessini area, near Verona Sehweighauser 1953; Malaroda 1954; Hottinger 1960; Cita & uplift, and was punetuated by several voleanie piles. Shallow- separated the Berici-Lessini area, comprising mainly shallow- and in the southern MOllte Baldo area, the Lower Eocene Bolli 1961). Barhieri & Medizza (1969) summarizedthe geologi- marine carbonate sedimentation was initiated on these topo- marine deposits, from the Euganean Basin characterized by deep sueeession consists of a few metres of muddy calcarenites and eal and stratigraphieal setting. Tbe famous Peseiara fish-heds graphie highs and eventually eoaleseed to form the Lessini Shelf open-water sedimentation (Piceoli el al. 1976). This threshold marls belonging to the Pietra Gallina; these are overlain hy have been known far more than four centuries (Sorbini 1989; (Luciani 1988; Bosellini 1989; Zampieri 2000; Beeearo el al. played a fundamental role in the Oligoeene palaeogeography. nummulitic calcarenites, which were deposited from Ypresian to Papazzoni 2000b). 2001). During the Oligocene a new graben forrned in the Marostica area Bartonian times (Oe Zanche el al. 1977). In the Monti Beriei, the Seaglia rossa is followed hy a few The distribution of Palaeogene sediments in the Southern (Barbieri el al. 1991; Zampieri 1995). In the central Monte Baldo area, Ypresian to Lutetian nummu- metres of turbiditic tuffs, tuffaceous marls and marls, which pass Alpine area of NE ltaly was strongly influeneed by the Alpone- Thin and discontinuous Upper Palaeocene to Lower Eocene litie calcarenites with coralline algae and corals (Forrnazione di upward into marly ealearenites (Pietra di Nanto; Fabiani 1915). Chiampo Graben (Barbieri el al. 1991; Barbieri & Zampieri mar1y limestones are widely distributed in NE llaly, e.g. Monte Besagno, 50~ 70 m thiek) overlie the Upper Cretaeeous-Upper This unit is Lutetian in age and grades upward into larger 1992; Zampieri 1995). Tbis graben was aetive during the Baldo (Lueiani 1989), Lessini Shelf (Garavello & Ungaro 1996), Palaeocene Scaglia rossa, or the lower Ypresian deposits. In the Nummuliles ealearenites, up to 50-90 m thiek, traditionally Palaeogene and extends along a NNW -SSE axis in the eentral- Monti Beriei (Massari & Medizza 1973) and Colli Euganei northem Monte Baldo area, Early to Middle Eoeene sediments named the Calcari nummultiei (e.g. Ungaro & Bosellini 1965; eastem Lessini Shelf. The graben thus divides the Lessini Shelf (Massari el al. 1976), as weil as the southem Altopiano di comprise shallow- and deep-water carbonates. These overlie the Mietto 1988; Bassi el al. 2000). In the SE part of the Monti into two areas which evolved separately, as shown by the Asiago areas (Ungaro & Garavello 1989). During the early to Seaglia rossa (Bosellini & Lueiani 1985), the basinal deposits Berici, Early Eocene pelagic limestones have been ascribed to different stratigraphie successions from earliest Late Palaeocene middle Eocene, sedimentation was differentiated into pelagic and (Seaglia einerea, Caleare di Chiusole) as weil as the slope and the Seaglia rossa (Pieeoli el al. 1976). In the eastem Monti onwards (AntoneIli el al. 1990). The eastem margin of the neritie facies. The lauer are widespread across the entire area platform earhonates (Caleare di Maleesine, Caleare di Torbole), Beriei (Mossano areal, outside the Alpone-Chiampo Graben, the graben encompasses the eastern Lessini Shelf and the western from middle Eocene (Lutetian) times onwards. A representative which represent the initial platform sediments of the area Calcari nummulitid extend up the Bartonian-Priabonian bound- Monti Berid and the succession comprises planktonic marls and area for Ypresian sedimentation is found near the village of (Bosellini el al. 1988; Lueiani 1989). ary (Ungaro 1969; Papazzoni & Sirotti 1995; Bassi el al. 2000). Within the Alpone-Chiampo Grahen, mieritie and elayey lime- In the western Colli Berici, this formation comprises only stones, apparently identical to the underlying Scaglia rossa, have Lutetian rocks (Fabiani 1915); shallow-marine carbonate sedi- been aseribed to the middle Thanetian (Barbieri & Medizza mentation was interrupted by the extrusion of basalt flows which Jg 'e 0 o oe: ~e:'-e: e: .- 1969). Malaroda (1967) grouped all of the sediments from the led to the infilling and emersion of the Alpone-Chiampo Graben o.a> Q).g e:a>0'" e: ~ :c .~~ ~~ ~m :J ~ s . "n; E.Q '(] rn '" Upper Cretaeeous Seaglia rossa (below) to the Lower to Middle at the end of the middle Eoeene (Ungaro & Bosellini 1965). At m m -'""'00 *.~ Cl ~ ~..I.! E e: .3 ",a> 5~ e =a> '" :J'" Eocene Calcari nummulitici (above) into the Caleare di Spilecco. the Bartonian-Priabonian boundary, a general regressive phase w VJ VJ. VJ '" ",'" 0 •• ~ e:$ $ ~~ :20, a>-' m e ~e: e: .ce: ü "E '" e: ::; '" This unit consists of basal massive limestones overlying volcani- has been recognized in the Monti Berici and Monti Lessini areas a> 0 o to o '" ~ d> ::; ~ elasties, followed by larger foraminiferallimestones with brachio- (e.g. Ungaro 1969; Lueiani el al. 2002; Bassi el al. 2000). In the lANGHIAN 1ij::; ::; g::; e: o ~ " ~E 0. pods, crinoids and calcareous algae. These are considered to be Colli Euganei, basinal conditions continued through thc entire oci I w~ · a> Early-Middle I1erdian (= Ypresian) in age by Papazzoni & Less Early Eocene; Palaeocene sediments are absent in the Berici area o () « BURDIGALIAN £; ~ « 20 :J 1l (2000). Ungaro (200 I) aserihed the Caleare di Spileeeo eropping (Massari el al. 1976). In the Colli Euganei, pelagie marls are W ~ ~ g out in the Cavalo-Poiano area to the Palaeocene~Early Eocene. deposited above the Ypresian Seaglia rossa (Massari el al. 1976; Z " AQUlTANtAN " Yoleanie layers (including basaltie flows, hyaloclastites and Lueehi Garavello 1980) and extend up to the basal Oligoeene. W « volcaniclastics) are often intercalated with these carbonates Locally, calcarenites and basaltic pillow lavas occur (De Vecchi o CHATTIAN ~. ~ & () 0 (Barhieri Medizza 1969). The Lower-Middle Eoeene sueees- & Sedea 1995). 0- sion differs markedly from other areas in having two main In the Marostiea area (southem Altopiano di Asiago), the 30 N " « carbonate bodies which, towards the NE, coalesce into a c. 100 m Palaeocene is represented by the Scaglia rossa facies, which is RUPELIAN h ~. e"<,, ••~~ e,.",,,,,,, me""''''',d1- ,.::~ d~~[jg ::d ~%'%~~~~~III~JI~ thiek sueeession (Yalle dell' Agno; Beeearo el al. 200 I). overlain by marly limestones and marls with planktonic forami- o o " ~~~~~ M3.m., '''f'''. e"""""''''.rto Caslelgomberto Fm.diCalvene /////.//_~:3 ~~~ m~~~ ;///: ~~~ In the Bolca area, the middle Eocene nummulite limestones nifera (Garavello & Ungaro 1982). Lower-Middle Eoeene w Orbitoidas ._ Mama di Mama dJ Mama di di MOrtiS3 -Wusliiif" ~ I PRIABONIAN (Marmi dei Chiampo) are interbedded with 100-200 m thiek mieritic, marly limestones with planktonic foraminifera (Scaglia z z ~~ ~ <;jif ~~~Fm .•"ad"'.",=. *' /~~ hyaloclastites. Both the calcarenites and the biogenie carbonates cinerea) pass upwards into Lutetian-Bartonian larger foraminif- w MRTONlAN A". ~ t ~ _.""","11" e,.,,,,,, ""..~ /;/~~/) of the Monte Postale area, as well as the laminated carbonates of eral calcarenites, glauconitic marls and massive calcarenites w w ~ nmestones ~ votcaniles __ ~~~~ the Monte Bolca area, are laterally equivalent with the lower (Calcareniti di Monte Gaggion; Fraseari Ritondale Spano 1969; 'Manni'di Calcari Cl I~ ~ member of the Marrni dei Chiampo. According to Papazzoni Garavello & Ungaro 1982; Ungaro & Garavello 1989). The o () . a> Chlam~ nummuhlici Calcarenitedi ~ (2000a), eoralline and eorallimestones ofthe Monte Postale area Lower-Middle Eoeene deposits of the southern Altopiano di o o LUTETIAN Calcare I Calcan. ,I I',:: ~..9! Calcari MonleGilg9lon W w d'Avesa nummu!JbCl Fm. di ~.~ j nlJmmu~i~ .". ' . "" •• are Early Eocene in age, while the Calcari di Ronca. e Soave, Asiago (Calvene-Pradipaldo areal were deseribed by Garavello Besagno ::=: ':: u Calcandl ~ dl __ variegata .J 'Q ~ '0 RorcleSoave Ouampo __ PtanktonlC Scaglia Marmi di Chiampo and the Pictra Gallina are middle Eoeene in & Ungaro (1982), Trevisani (1994) and Papazzoni & Trevisani cinerea a> ~ l:: Calcan Pielra di Nanto rnarly age. Locally, these data are confinned by calcareous nannoplank- (2000). c( Pie!ra J ~ Cafcare di nummuliticl limestones YPRESIAN ton (Beeearo el al. 2001). Within the thiek voleaniclastie !I Gallina""" Gallina S U MontePoslale __ Mama Scaglia An important transgression is recorded across the entire 0.. deposits, some Iignitic deposits are present, including the famous western Venetian area at thc beginning of the Priabonian. In _, __ C~CalcarediSpiecco~~ ""oe•. 1-1-Scagna Scaglia w THANETlAN Scagfia SCaglia rossa rossa fossil Lagerstätten of the Purga di Bolca area (Sorbini 1989). At Calvene, a biogenie eonglomerate (Conglomerato di Grumale) "" ""', S

overlain by tbc Lower Oligocene Formazione di Calvenc. The 1989; Dal Molin el a/. 2001). In the Late Oligocene, following (Braga 1972; Trevisani 2000). Tbe Neogene sediments of the Vittorio Veneto-Belluno area Priabonian transgression is also evident on thc elevated ridge of weak, local volcanic activity, this area emerged, as documented The Belluno Flysch is a sedimentary body > 1000 m thick, are mainly siliciclastics. Carbonate deposits with thick rhodolith the former Alpone-Chiampo Graben, where the historical holo- by the clays produced by the subaerial alteration of the volcanic located between the Alpago and the Feltre areas, as weil as in the accumulations are represented by the upper Chattian Calcarenite stratotype of the Priabonian is loeated (Passo di Priabona, near sediments present at the top of the Calcareniti di Castelgomberto Venetian fore land basin between Vittorio Veneto and Segusino. di Castelcucco unit in the Vittorio Veneto area, and by the coeval Monte di Malo) (see Mietlo 2000 for overview). The Priabonian (Sovizzo; Bosellini 1964). In the northem Monti Berici (Valmar- In the Alpago and Belluno areas, this unit contains only lower Calcarenite dell'Alpago unit in the Belluno-Alpago area. The succession transgresses altered Middle Eocene basalts and is ana, Col dei Bosco), the Chatlian succession is represented hy Eocene sediments, in the Feltre area it extends into the middle Siltite di Bastia unit is overlain by the Calcarenite di Castelcucco characterized by the basal Conglomerato dei Boro (Fabiani 1915; sandstones and calcareous sandstones rich in larger foraminifera, Eocene, and in the Follina area up to the late Eocene. North of and overlies the Calcarenite dell'Alpago. In Ibe Alpago area the Antonelli el a/. 1990). which are overlain by coralline algal rudstones (Ungaro 1978; Feltre, the middle-upper Eocene succession is characterized by Siltite di Bastia is up to 250 m thick and decreases in thickness In the western Monti Serici this conglomerate is not so evident Bassi el a/. 2007). Chatlian sandstones and coralline algal altemations of biogenic calcarenites, marls and sandstones. The towards Feltee; in the Venetian foreland basin area it is a few and is known as the Conglomerato a Cerithium diabo/i (Fabiani rudstones are also present in the Monti Lessini area and are Mama di Possagno unit and the upper part of the Belluno Flysch metres thick (Ghibaudo el a/. 1996). Between the Feltre and 1915; Ungaro & Bosellini 1965; Mietlo 1988). The Mame di known as the Arenarie e caleari di S. Urbano (Bosellini 1967; are interpreted as slope deposits intemngering with the distal Alpago areas, two sandstone units with glauconite (Arenaria di Priabona has a thickness of c. 90 m in the type area and can Bassi el al. 2007); these are overlain by Lower Miocene marine faeies of Ibe Belluno Flysch (e.g. Costa el al. 1996; Stefani & Orzes and Arenaria di Libano) overlie the Siltite di Bastia, attain 170 m in the Mossano area (eastern Monti Berici; Bassi et marls (Mame argillose dei M. Costi). Grandesso 1991). separated by a sihy unit (Siltite di Casoni). Around BeIluno these a/. 2000). The top of the succession is locally characterized by a In the Monte Baldo area, the Early Oligocene is represented Across the eastern Venetian area, the Eocene deposits are three formations are > 100 m thick. The Arenaria di Orzes has marly horizon rich in bryozoans (e.g. Ungaro 1978; Mame di by shallow-water carbonates (Fonnazione Acquenere), siliciclas- unconformably overlain by the Chatlian Molasse. The unconfor- been interpreted as an estuary shoal deposit, whi!e the Siltite di Brendola in Broglio Loriga 1968). This formation appears to tic carbonates (Caleare di Linfano) and marls (Mame di mity js the result of an important hiatus which becomes older Casoni and the Arenaria di Libano represent prodelta and delta- decrease in thickness towards thc centre of the elevated ridge of Bolognano) (Bosellini el al. 1988; Luciani 1989). Upper Oligo- towards the east (Middle Eocene-Early Oligocene in the Alpago front facies (Massari el al. 1986a; Costa el a/. 1996). the former Alpone-Chiampo Graben; it is absent in the Valle cene sediments crop out in the Monte Brione and Monte MoscaJ and Belluno areas) and younger towards the west and south Tbe Burdigalian is represented by a transgressive-regressive deli' Agno, where the overlying Oligocene Calcarenit; di Castel- areas; this succession is represented by conglomerates and larger (Early Oligocene in the Feitre, Possagoo and Follina areas). The succession related to a eustatic event affecting the outer carbonate gomberto is transgressive over Middle Eocene volcanic units foraminiferal and coralline algal calcarenites (Calcare di Incaffi; (Barbieri el a/. 1980; Mietlo 1992). Southem Alpine Molasse ranges from the Chattian to Recent platform. The Mama di Bolago consists of marls and ranges- in Luciani 1989) and by deep-water mixed siliciclastic-carbonate (Massari et a/. 1986a; Costa el a/. 1996), and represents parts of thickness from 100 m (Feitre) to 200 m (Venetian foreland basin The basaltic units of the Monte Baldo area were subaerially units (Formazione di M. Brione, Oligo-Miocene in age; Luciani the infilling of the Venetian Basin, restricted to the east by the areal. The overlying Arenaria di s. Gregorio (up to 60 m of exposed in the uppermost Bartonian. The overlying Middle to & Silvestrini 1996). Dinaride Mountains, and to the west by the Schio-Vicenza sandstones) represents a rapid transition from outer- to inner- Upper Eoeene succession comprises platform (Caleare di Nago), In the southem Altopiano di Asiago area, the Oligocene units lineament. The Chattian-Messinian sediments form a ciastie pIatform environments with a fluvial influence (Costa et al. 1996). slope (Calcare di Maleesine) and basin (Scaglia cinerea) deposits comprise siliciclastic sediments passing into paralic fades. The body with a maximum thickness of >4000 m at the Venetian The Langhian commenced witb a rapid transgression, which (e.g. Castellarin & Cita 1969; Luciani 1989; Bassi 1998). The Arenarie di Mortisa formation is overlain by thick lower foreland basin-plain boundary. The molasse consists mainly of followed the abrupt deepening of the Venetian Basin to bathyal Caleare di Nago was subaerially exposed at the Eocene- Oligocene siltstones and sandstones, often with conglomerates sandstones, siltstones, marls and conglomerates. These are inner- conditions. The succession begins with the Mama di Monfurno Oligocene boundary (Luciani 1989). (Formazione di Calvene; Papazzoni & Trevisani 2000). The platform carbonate deposits that are occasionally overlain by which comprises a basal layer of fossil-rich glauconitic sand- [n the southem Altopiano di Asiago, the Formazione di succession ends with the Formazione di Salcedo, a rhythmic more distal sediments (Mama di Bolago, Mama di Monfumo, stones overlain by marls containing small bivalves (20-45 m Pradelgiglio was deposited during the Priabonian between the alternation of volcanic deposits and fossiliferous units such as Mama di Tarzo; Massari el al. 1986a). Sedimentation com- thick). The Arenaria di Monte Baldo overlies the Mama di Astico and Brenta rivers (Frascari Ritondale Spano 1970; the Arenarie di Sangonini and the Mame di Chiavon. This area menced with shallow-marine deposits including a tide- and" Monfumo and consists of coarse glauconitic-fossiliferous sand- Trevisani 1994). This formation consists of siliciclastic sediments emerged in the uppermost Early Oligocene (Principi 1926; wave-dominated delta system, and a mixed siliciclastic-carbonate stones, and biocalcarenites alternating with grey marls. This unit which pass upwards into larger foraminiferal calcarenites with Frascari Ritondale Spano & Bassani 1973). faeies (Massari et al. 1986a, b). The Arenaria glauconitica di represents shelf deposits with sand ridges (Massari el a/. 1986a, coralline algae and benthic macrofossils (Papazzoni & Trevisani During the Aquitanian a new transgression led to the re- BeIluno, up to 50 m thick, consists of fossiliferous sandstones b). The Arenaria di M: Baldo crops out in the Venetian foreland 2000). The upper Priabonian Arenarie di Mortisa, overlying the establishment of marine conditions in the western Venetian area. rich in glauconite and represents the transgressive basal layer of basin area (Vittorio Veneto, Crespano). Its thickness ranges from Formazione di Pradelgiglio, consists of bioturbated marls with The Miocene successions are represented by sandstones and the molasse succession. It is heteropie with the Conglomerato di 50 to 300 m, with a maximum near Vittorio Veneto. larger foraminifera, siltstones and sandstones, and forarniniferal calcareous sandstones directly overlying the Marne di Priabona M. Parei and the Calcarenite deli' Alpago (Massari el a/. 1986b). From the Serravallian to the Messinian, several important calcarenites (Trevisani 1993). (Monti Lessini in the Verona Province), Oligocene limestones The Conglomerato di M. Parei (Keim & Stingl 2000), which cbanges occurred in the Venetian basin: the axis of tbe foredeep The Oligocene is missing in the Monti Lessini area of the (Monti Lessini in the Vicenza Province), and submarine voleani- crops out in the Ampezzo area, contains Chattian to Aquitanian shifted and the basin was incorporated into the South Alpine Verona Province (AntoneIli el al. 1990). Tbe presence of clastic sediments (Monti Berici; Ungaro & Bosellini 1965). In fossils in the matrix and unconformably overlies Mesozoic units. fossilized palaeokarstic cavities, filled by yellow soils (terra defonnational system. In the initial stage, accelerated subsidence the Marostica area, the Aquitanian Calcare di Lonedo trans- The Chatlian Calcarenite dell'Alpago (Costa et a/. 1996) com- led to the deposition of epibathyal marls (Mama di Tarzo) gialla di Verona), suggests intense erosion subsequent to emer- gressed onto the Fonnazione di Saleedo, which eomprises coral- prises up to 50 m thick glauconitic calcarenites with larger overlying the Arenaria di M. Baldo, followed by organic-rich sion (Corni 1977). Near Cavalo (North Verona), Oligocene beach line calcarenites (Frascari Ritondale Spano 1969). The foraminifera, rhodoliths and bryozoans. This is restricted to- tbe lower Tortonian mudstones. The subsequent stage was character- sandstones transgress over Lower Eocene deposits (Castellarin & Burdigalian Molasse of Schio overlies the Calcare di Lonedo. In Alpago area (Massari el a/. 1986b). The Calcarenite di Castel- ized by rapid slope progradation (middle Tortonian). Localized Farabegoli 1974). The Oligocene is well represented along the the Vieenza area, the Chattian Arenaria di S. Urbano is overlain cucco (Scudeler Baccelle & Reato 1988; Bassi el a/. 2007) crops conglomerate bodies (Conglomerato di M. Piai) within this eastem Monti Lessini margin and in the Colli Berici (from by the Miocene Mame argillose dei M. Costi, which are only a out in tbe Castelcucco and Vittorio Veneto area and is repre- succession represent mass-fiow deposits probably funnelled along Lumignano to Villaga), where an important shallow-water carbo- few metres thick (Bosellini & Dal Cin 1966; Bassi el al. 2007). sented by larger foraminiferal and coralline algal calcarenites a structural depression (Massari el al. I986a). In the late nate platform, characterized partly by hermatypic corals and alternating with thin marly beds. This unit overlies the Siltite di Tortonian, subsidence slowed down and a stack of vertically patch-reefs developed (Geister & Ungaro 1977; Ungaro 1978; Eastern Venetian part of the Brenta River. Ouring the Bastia and is disconfonnably overlain by the Aquitanian Siltite aggrading fan-delta sequences (Arenaria di Vittorio Veneto) were Frost (981). These shallow-marine carbonates represent the Palaeocene-Early Eocene, pelagic units were deposited in di Casoni (Massari et a/. 1986b). deposited on the shelf created by the previous progradational Calcarenite di Castelgomberto (Bosellini 1967; Bosellini & the Belluno (Scaglia cinerea, Mama della Vena d'Oro) and in the The northem margin of the Lessini Shelf is located in the episode (Massari el al. 1986a). The architecture ofthe Messinian Trevisani 1992) in which volcanodetrital lenses, rich in fossils, western Treviso (Scaglia variegala) areas (Fig. 17.27). In Valsugana area (Borgo Valsugana to Pieve Tesino). The early to alluvial system was largely controlled by tectonics. Palaeocurrent are locally present (e.g. Accorsi Ben;ni 1974). On the opposite the lalter area, as in the Feltre area, sedimentation continued lowermost middle Eocene is represented by deep-water sedi- indicators and the composition of Tortonian-Messinian sand- side of the Monti Beriei, towards the Colli Euganei, the Marne until the Middle Eocene (Scaglia cinerea). During the Late ments (Scaglia einerea) with planktonic foraminifera (Fuganti el stones and conglomerates suggest a source area within the Euganee were deposited in a pelagic basin (Piccoli el a/. 1976). Eocene, a regressive succession evolved with the deposition of a/. 1965). The Late Eocene consists of shallow-marine forami- eastern South Alpine domain. The Messinian Conglomerato dei Tbe temporary emersion of volcanic islands is documented by the Mama di Possagno and the Calcare di Santa Giustina units. niferal and coralline algal calcarenites of the Calcare di Nago Montello represents coarse fan.deltas passing upward into allu- the formation of lignitic deposits, the most famous of which in In the SE Monte Grappa area (Treviso Province), the Possagno unit and deep-water sediments (Mame di Bolognano, Formazione vial deposits (up to 200 m thick). Blue sandy days, early-middle Monteviale and Gazzo di Zovencedo (Monti Berici) contain an seetion (parastratotype of the Priabonian) is the thickest Priabo- di Castello Tesino; Luciani & Trevisan; 1992). The Oligocene is Pliocene in age, deposited above the Cnnglomerato dei Montello extraordinary land mammal fauna (e.g. Dal Piaz 1937; Bagnoli nian succession in the Southem Alps. The section is c. 700 m represented by the Formazione Acquenere (marls and marly crop out ncar Comuda and- represent a neritic setting (Massari cl el al. 1997). thick and consists mainly of clay marls with planktonic and small siltstones with Nummulites), the Calcare di Linfano (Iarger a/. 1993). At the beginning of the Late Oligocene, the Calcareniti di benthic foraminifera (lower-middle Priabonian Mama di Possag- foraminiferal calcarenites: Schiavinolto 1978), the Formazione di Castelgomberto carbonate platform became emergent (Frost no formation; Cita 1975; Grünig & Herb 1980). The Mama di Castello Tesino and the Formazione di M. Brione. The Priabo- Volcanism 1981; Gianolla el al. 1992); this event is documented by extreme Possagno is overlain by the upper Priabonian Calcare di Santa nian to Rupelian deposits are generally characterized by a large Palaeogene magmatism within the Eastern Alps is variable in palaeokarst formation (Bartolomei 1958; Mietlo & Zampieri Giustina unit, consisting of larger foraminiferal calcarenites amount of siliciclastics and a reduced thickness (Trevisani 1997). time and space. This magmatism can be interpreted in tenns of 1092 M. W RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1093

the changing geodynamic framework that is reflected in the Martinis 1962; Auboin 1963; Bignot 1972; Cousin 1981; Cucchi (SBZ3) in age. Alveolinid and nummulitid foraminifers, corals, characterized by interbedded siliciclastic sandstones and marl- different evolution of the relatcd mantle sources (Wilson & el al. 1987). A short synthesis was given by Ventur;ni & Tunis corallinacean algae and sea-urehins appeared during SBZ4 stones. Tbe sedimentological features (probably basin plain Bianchini 1999). Two main tectonomagmatic associations cao be (2002). The Palaeogene scenario, inherited from the Mesozoic, (Pugliese el al. 1995, 2000). Sedimentation continues until the turbidites) and the ichnofacies suggest a deep-marine environ- recognized: orogenie (subduction-related) suites and anorogenic consisted of the Friuli Platform, which bordered the Belluno late Cuisian (SBZ 12) with shallow-marine sedimenls containing ment (Tunis el al. 2002). In agreement with Pavsie & Pekmann (intraplate) suites. Basin to the NW and the Julian Basin towards the NE (Venturini larger foraminifera (Gozzi 2003). These Palaeogene deposits are (1996) and Tunis el al. (2002), the turbidity CUITentflow was Magmatic rocks characterized by orogenie affinities, including & Tunis 2002). Palaeogene deposits of the Friuli-Venezia-Giulia mainly NW-SE directed (Drobne el al. 2000b) and preliminary parallel to the WNW-ESE striking basin axis during the Mid- both mafic and felsic dykes as weil as granitoid intrusions, were part of the Friuli Platform and the Julian Basin. From a larger forarninifera data suggest two main belts in the Trieste Eoeene. occurred mainly between 42 and 25 Ma (with a climax between geographie point of view, the Friuli Platform corresponds to the Karst (Drobne 2003b). The first one (zone 2 of Drobne 2003b) 33 and 29 Ma) along the Insubric-Periadriatic Lineament. Major present-day southem Pre-Alps and Karst, and the Julian Basin ineludes the localities Padriciano, Opicina and Duino. It is Siovenian Tethys basins (K.D., B.O., J.P., R.P.) element composition of the basic rocks indicates a spectrum of can be related to the Julian Pre-Alps. The Friuli Platform and lhe characterized by Danian to early Ypresian (SBZI-9) carbonate magma compositions ranging from calc-alkaline and high-K Julian Basin can be traced southwards to the Adriatic and Dinaric ramp deposits, partly overlain by late Ypresian deep-marine Siovenia is situated at the contact of the Southern and Eastern calc-alkaline to shoshonitic types (Beccaluva el al. 1979, 1983; Platforms, and the Bosnian Basin, respectively (Cati el al. 1987; sediments (Castellarin & Zucchi 1966; Pugliese et al. 1995; Alps with the Pannonian Basin, the Dinarides and the Adriatic von Blanckenburg & Davies 1995; Macera el al. 2002). Tbe Herak 1989). Moreover, Cati el al. (1987) proposed a new Gozzi 2003). The area of Colle of Medea (Udine) mayaiso be Sea (Figs 17.2. 17.26 & 17.29). Palaeogene sediments in SW most primitive mantle compositions appear to be mantle-derived scenario wilh an additional Friuli Basin that subdivided the Friuli part of this belt (Barattolo 1998). The second belt (zone 3 of Siovenia are delimited to the NE by the high plateaus of mells relatively unaffected by shallow-Ievel crustal contamina- Platform into SW (SW of Pordenone) and NE (Udine area and Drobne 2003b) includes the Rosandra valley and is characterized Trnovski gozd, Nanos and Sneznik. as weil as Gorski Kotar in lian. Their leace element distribution displays enrichments in south of Udine) sectors. This new basin would then continue to by Danian to late Cuisian (SBZ 1-12) carbonate ramp deposits Croatia, and to the south by the CIearija hills in the Croatian part L1LE (large ion lithophile elements, e.g. Cs, Rb, K) and the Outer Dinarides. As a eonsequence, the SW and NE Friuli overlain by deep-marine sediments. of Istria. To the west, it passes along a narrow belt aeross the depletion in HFSE (high field strength elements, e.g. Nb, Ta, Ti) platforms may be connected with the Adriatic (present-day Palaeogene terrigenous sedimentation took place in the Julian Trieste-Komen Plateau to the Soca valley, and further along it as typically observed in magmas from active continental margins. Dalmatian Zone) and Dinaric (present-day High Karst Zone) Basin, a narrow, elongate basin, which today is part of the SE towards the north. In a wide are the houndary encloses the hills These geochemical features, along with Sr-Nd isotopic evi. platforms, respectively. Alps (eastern Friuli-western Siovenia). Tbe basin had an internal of Goriska Brda. Further northward the boundary rises on the dence, indicate that magmatism was induced by partial melting margin in the north, which was subject to compression, and an ridges between the Soca and Nadiza rivers. These deposits are of lithospheric mantle domains intensely metasomatized by Tectonic setting external margin in the south, represented by the Friuli Carbonate heavily karstified and contain numerous caves, dolinas as weil as subduction-related fluidslmelts. The significant presence of Tbe tectonic setting of the Palaeogene of the Friuli- Venezia- Platform. The basin was characterized by mixed carbonatel several valleys with outcrops of deep-marine sediments. Palaeo- shoshonites suggests that continental crustal components were Giulia regions eomprises aseries of NW -SE overthrusts, which siliciclastic sedimentation from late Campanian to Early Eocene gene belts associated with the predominant Dinaric direction also involved in subductioD. verge southwards (Castellarin & Vai 2002). Compression led to times. Sediment distribution patterns are eomplex due to a (NW-SE) continue to the east and south to Croatia, and to the To the south, anorogenic volcanic rocks characterize the lhe establishement of a foreland basin which migrated from combination of tectonics, relative sea.level changes, and sub- west to Friuli. In the SE part of Slovenia, Palaeocene beds are Veneto Volcanic Province (VVP). This is Late Palaeocene to Siovenia towards the Veneto (Doglioni & Bosellini 1987). sidence (Tunis & Venturini 1992). During the mnin phase of exposed only as small erosional relics, e.g. between Ribnica and Late Oligocene in age and is represented by aseries of eruptive Drowning of parts of the Friuli Platform proceeded from east to turbidite deposition (Maastrichtian-early Eocene), >4000 m of Novo mesto. eentres orientated NNW -SSE. Magma generation appears to west. This tectonic phase is mainly Early Eocene in age (Carulli sediments were deposited. have been triggered by decompressional effects related to exten- el al. 1982; Poli & Zanferrari 1995) and can be linked to Most of the Maastrichtian units are interpreted as slope-apron Teclonic setting and pa/aeogeography sional deformation which affecled the South Alpine Foreland in compressive activity during the Meso-Alpine collisional phase environments located elose to the margin of the Friuli Platform, Slovenia belongs to faur large tectonic units: the Eastem Alps response to the general north-south compression during the (Castellarin & Vai 2002). Following Oligocene extension, a neo- while the Palaeocene and Eocene units reflect a position elose to and the Southem Alps separated by the Peri-Adriatic Lineament; Alpine Orogeny (Beccaluva el al. 2003, 2005). VVP lavas are Alpine eompressive phase occurred (Chattian-Burdigalian), as the outer side of the basin (Flysch di Calla, Flysch di Masarolis the Pannonian Basin in the east; and the Outer Dinarides mainly basic and eomprise a wide compositional speetrum of demonstrated by the formation of NW-SE orientated thrusts and Flysch di Grivo), followed by basin-plain environments and extending to the south (Premru 1980, 1982, 2005; Placer 1981, mantle-derived melts including (mela) M-nephelinites, basanites, (Castellarin & Vai 2002; Ponton & Venturini 2002). Sub- a deltaic system (Flysch di Cormons). Tbe Flysch di Calla I999a). The Dinarides border the Adriatic Platform along the alkali-basalts and tholelites (De Vecchi & Sedea 1995), as sequently, two further compressive phases occurred during (early-middle Pal.eocene) consists of reddish marls interbedded Dinaric Thrust. This series of overthrusts verges from the north typically observed in low-volcanicity rifts. The relative abun- Langhian- Tortonian and ?Messinian-Pliocene-Quatemary with thin sandstones and is a significant unit in eastern Friuli and towards the SE and includes Trnovski gozd, Nanos with Hrusica, danee of siliea-undersaturated and silica-oversaturated products times, as demonstrated by south-orientated thrusts. western Slovenia (Pirini Radrizzani el al. 1986; Dolenec & Sne.znik, and in Croatia, Gorski Kotar and Velebit (Rakovec varies regionally, with more abundant nephelinites and basanites Pavsic 1995). The Flysch di Masarolis (middle-upper Palaeo- 1956; Poljak 2000; Bigi el al. 1990; Blaskovie 2000). Tbe to the west (Val d'Adige and western Monti Lessini), and Sedimentary and stratigraphie deve/opment cene) is mainly represented by thin siliciclastic turbidites, while Cicarija Zone is presumably a deformed intermediate zone predominantly alkali-basalts, transitional basalts and tholeiites to The Palaeogene carbonate platfonn succession commences with the Flysch di Grivo (Late Palaeocene-Early Eocene) conlains between the Dinaric Thmst and the Istria autochthon (Placer & the east (eastem Monti Lessini and Marostica area). The sodic Palaeocene sediments, which mostly overlie Late Cretaceous several carbonate megabreccias derived from the resedimentation Vrabec 2004). The tectonic relationship between the Dinarides character (Na201K20 > I), and the incompatible element distri- units; Maastrichtian is proven for some localities of the east of shallow-marine carbonates (Friuli Platform) as weil as inter- and the Southern Alps was described by Herak (1985, 1986, bution (characterized by negative anomalies in Cs, Rb, K, and Trieste Karst (Pugliese el al. 1995) and Ibe south and north calated siliciclastic-carbonate turbidites. These extensive carbo- 1987, 1999). He subdivided the region into three tectogenetic positive anomalies in Nb-Ta) of WP volcanics show similarities Gorizia Karst (Tentor el al. 1994). Maastricthian inner lagoonal nate debris aecumulations are explained by catastrophic units, namely Dinaricum, Adriaticum and Epiadriaticum, the first with intraplate magmas. Recent studies on spinel-peridotites sediments comprise the last rudist genera Bournonia and Apri- resedimentation events in the deep-water basin. Some megabeds two of which represent carbonate platforms and the third one an (mantle fragments) entrained as xenoliths in WP basanites and cardia as weil as forarninifers (Caffau el al. 1998). The latest have a strike of more than 70 km and individual thielrnesses of intennediate pelagie zone. This subdivision is widely used nephelinites indicated that: (a) the local Iithospheric mantle was Cretaceous to early Danian succession contains several strati- up to 200-260 m (Vernasso Megabed). Olistoliths can reach a (Blaskovie 2000; Biondie el al. 1997; Carulli el al. 1990; Drobne extensively metasomatized by alkali-silicate melts; and (b) the graphie hiatuses, often associated with emergence and the length of several hundred metres. & Trutin 1997; Mioe 2003; Drobne el al. 2000a, b), but it is still area was characterized by an anomalously hot geothenn (Siena development of peritidal eycles, such as in the eastern Trieste The major megabreccia units were generated by the fault- under discussion. Other studies have suggested a. separation of & Coltorti 1989, 1993; Beccaluva el al. 2001). These factors, Karst (Pugliese el al. 2000). One of the basal peritidal cycles at controlled failure of the Friuli Platform margin, which became the Karst Dinarides. or a single Adriatic Carbonate Platform coupled with the adiabatic decompression that was induced by Padriciano records the KlPg boundary (Pugliese & Drobne 1995; seismically active during the Late Palaeocene-Early Eocene. (AdCP) instead of the Dinaric Platform (Tisljar el al. 2002; extension, triggered magma-genesis and, thus, the observed Pugliese el al. 1995, 2000), which is also present elsewhere in The Flysch di Cormons (Early Eocene-Mid Eocene) is charac- Vlahovie el al. 2002; Dragicevie & Velie 2002). During the volcanism (Beccaluva et al. 2005). Sr-Nd-Pb analyses of the the Siovenian Karst area (Drobne el al. 1988a; Ogorelec el al. terized by basin-plain turbidites. Sea-Ievel changes controlIed Cenozoie, most parts of the Adriatic and Dinaric platforms were volcanics, integrated with studies of the entrained mantle 1995, 2001). The boundary is documented by palaeontological basinal sedimentation from the latest Ypresian to the earliest emerged, and only small areas of the Adriatic Platform remained xenoliths, indicate that both lithospheric and sublithospheric data (Pugliese el al. 1995, 2000), palaeomagnetism (Marton el Lutetian (Venturini & Tunis 1991). During the early Lutetian, a below sea level. Tbis occurred during the Palaeocene in Slovenia, (possibly plume-related) mantle sourees were involved in their al. 1995a), an iridium anomaly (Hansen el al. 1995), and a rapid progradation of prodelta, delta-front, and deltaic-plain the Trieste region (Pugliese el ai. 1995) and Hereegovina. generation (Macera el al. 2003; Beccaluva el al. 2005). l3 negative shift in ö C (Ogorelec el al. 1995). deposits occurred in response to tectonic uplift. The prodelta Sedimentation continued, with interruptions, up to the end of the After the KlPg boundary crisis, pioneer biota (small foramini- deposits contain a rieh and diverse macrofauna (corals, molluscs, Middle Eocene. The development of the Palaeagene in SW Southern Alps in ltaly: Friuli Pre-Alps and Karst (N.P., fers, thin shelled ostracods and gastropods) appeared in peritidal echinids, alveolinids, nummulitids, etc.) (Maddaleni & Tunis Slovenia commenced either in the central part of tbe Western G.T.) environments during the early Danian (Shallow Benthic Zone 1993; Hollinger 1960). Tbe corals formed patch-reefs in front of Tethys (after Golonka 2004) or, as proposed by Channell el al. SBZ I of Serra-Kiel el al. 1998). Characean algae indicate the advancing deltaic system. Together with the Siovensko (1979), as an African promonlory along a submarine belt. This " The Palaeogene deposits of the Friuli- Venezia-Giulia region have freshwater influence. The peritidal cyeles are overlain by inner Primorje, the Trieste area belongs to the Trieste-Koper Syncline. structural unit, known as the Apulian Plate or Adriatic (Micro)- been extensively studied (e.g. Stache 1889; Dainelli 1915; lagoonal limestones, which are Danian (SBZ I) to Thanetian According to Pavsie & Pekmann (1996), the Trieste Flysch is Plate consisted of large carbonate platforms: in the west the 1094 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1095

(Il 00 J2 ! E"c rl 'C Q)"üi :;::l~ Q) g I :1 E o c ~ ; I .~ ••Cl 1ii~ '" (Il 5 ~ e ~ "0 I I:!! :>. .l! gJ...J e 5~ ~ .g III .e -5 g I ~ ~ w rJ) rJ) rJ) ~ ~ o «~ g~::f B£ -gl-g cj . GELASIAN :2 ffi~-B.g.~~~~ ~:~ >l1lolll->I1lQ) ""ie 0:>' PIACENZIA w ~-= ZANCLEAN • m ///////////// ~~'i~i~!!.~I o-g13~Eo~~ ~! MESSINIAN wZ~(J)ai"a)~Q)I1l~'li)ai"I' z ffi I1lCcc"'cc:::s:::sc N :t ~ggg gg~~~, . w :> TORTONIAN .2 g~~ ~ ~ ';;~ ~ I ,:3 10 .1'=::'::: w Cl ~~~~~~~~~L-~ o z w SERRAVALLIAN W ~ 'l U g tJ 15 o LANGHIAN o " / z w :;; ~.I ii> z 0:' BURDIGALIAN z~ 20 I!;; w • ~_. 21f?:>"-l' o ~ Mame argillose calcari di ~ AQUITANIAN ~~;~~/d~ dei M. Costi . S. Urbano Siltite di Caseini llbano '" ~ ~ 25 o Cl 0: Arenariee~al~re;- '~~ calcaridl Lonedo ~~ :::::i &1 CHATTIAN o :> S. Urbano Fm. di Salcedo d:r:~D~n~7~:~~~ «I Fig. 17.28. Lithostratigraphy of selected localities in the western and eastem Venetian areas.

Apennines with Apulia, in the east the Adriatic-Dinaric Carbo- larger foraminifers in the Upper Miliolid Beds (DelvaUe & Buser •.. nate Platfonn (or Adriatie Carbonate Platfonn), alternating with 1990), or Operculinid Limestone for nummulitid accumulations deep-marine basins (e.g. BeUuno, Friuli basin; Cati et af. 1987). at the base of the Alveolinid-Nummulitid Limestone (Pavlovee 1963). -rJ) Palaeomagnetism Based on underlying sediments (deep-marine c1astics or At the Dolenja Vas seetion, whieh crosses the KlPg boundary, shaUower- to deeper-marine carbonate platfonn) and the distribu- ::I reversed polarity has been observed in the Polarity Chron C29R, tion of larger foraminifera, Drobne (2000, 2003b) defined four with a rotation angle of 28° in a clockwise direction (Dolenec et biosedimentary zones for the area of SW Slovenia and Istria af. 1995; Marlon in Drobne et af. 1996a, b). Investigations rrom (Fig. 17.30). They were supp0rled by various studies (e.g.

~ ). J:! ~ Htll West of Gori,ka Brda, submarine slides and megaturbidites ment was the continued deposition of the Alveolinid-Numulitid 1l: ~g~ ffi ~ !Xl ~ ;f~,: were described (Tunis & Venturini 1984; Skabeme 1989). Near Limestones during the Ilerdian and Cuisian as weil as a transition ~ ~ Nova Gorica, a 1500 m deep borehole records adepression filled into deeper-marine sediments, with glauconite-bearing strata, at " with deep-marine sediments (Marinko 1992). In Ihe Gorica area, the Cuisian-Lutetian boundary (NP 14). Alveolinids predomi- ~ ~ conglomerates with a souree area to thc NW and SW (i.c. nate, especially those of Alveolina histriea (Le. Alv. rakoveci). in ~ E~ Friuli ~ Q.~ Q) ~ ~ :::l platform) were deposited in several phases from Maastrichtian to addition to nummulitids (Drobne 1977; Drobne & Pavlovec o ::; H.ll Middle Eocene times (cf. Venturini & Tunis 1992). 1991; Drobne & Cosovi" 1998; Drobne & Tmtin 1997). ~ Deep-marine sediments of thc Vipava Valley syncline and its Biosedimentary Zone 4 (BSZ 4; includes carbonate platform ~ . ( ~ 'C!: -g ~J SE extension may overlie Scaglia beds. They are either coo- and deep-marine sediments located along the oldest vertical 41 ~ 1: ~ cordant at tbe platform-basin transition, or fellow after a hiatus faults on the SW slopes of C:;carija to Savudrija ridge, 10 ;::e (fJ :.,'1. _ '" '" (Engel 1970). Locally, megaturbidite beds with nummulitic Podpi"an, and between Krk and Cres islands). The deep-marine r,. 0 ~ ~ breccias predominate (Engel 1974; MiküZ & Pavlovec 2002), sediments of Ciearija and Siovenian Istria can be subdivided into »( ~ N and larger foraminifers of Middle Cuisian age (SBZII) can two complexes of different ages. both of which were part of thc :' ::;) ~~ I: Bl occur in upper beds (De Zanche et al. 1967; Drobne & Bacar Adriaticum. The older one includes the NP14 zone and passes ~"l: g I: ~ 0, 2003). In the Vipava Valley, the Middle/Late Palaeocene (NP7, from Alveolinid-Nummulitid Limestone into deep-marine sedi- ~~ ~ .~!~ .1 Lijak) to Middle Eocene development is weil established (Krase- ments with glauconite beds or with macrofossils (SBZI2?; :- "l: ~ jj € 8E ~ ninikov et al. 1968; Buser & Pavsic 1976, 1978; Pavsic 1994; Mikuz & Pavlovec 2004). At GraeiSce, crabs, nummulites and :: ~ ~ ~ Riznar 1997). At Postojna, deep-marine sediments with conglom- nannoplankton revealed an Early Lutetian (NPI5) age (Pavlovec !O~ :5 erates containing nummulites indicate aMiddie Cuisian trans. & Pavsic 1987). The coastal belt comprises four sedimentary ~ gression (Pavlovec 1981). complexes, passing from limestones with alveolinids and num- Ir : ?/OO <2 "l: g~ ~ Separated from thc Gonea area and Vipava Valley, several mulitids (Early to Middle Lutetian, NPl5-NPI6 boundary) into lj I isolated exposures of deep-marine sediments occur in southem basinal sediments. Sedimentation continued until the NP 16 zone e~/fJ~9./d ...• j ~~ ~ Siovenia. They are mostly erosional remnants (Premru 1982; (Pavsic & Peckmann 1996). e./~fJesOl:l ~'< 1" Pavsic 1994, 1995). Alveolinid-Nummulitid Limestones were deposited from the ~ ,I" CO <9' Biosedimentary Zone 2 (BSZ 2; includes platform and deep- Middle Cuisian to the Middle Lutetian (SBZll-SBZI4). They a:: .. ~ marine sediments from the southem edge of Vipava Valley, overlie deeply eroded rudist limestones, bauxite, coal and bitumi~ ~_--~---.------Brkini with border areas, and southwards to the northem slopes nous beds and represent restricted shallow-water environments. At "l: !Ui i of Ciearija). The deep-marine basins of Brkini and Trieste- the transition to the Lutetian, foraminiferal associations were part .(,) Komen Plateau are part of the Adriaticum. The Brkini Flysch of a larger Central Proto-Tethyan fauna, including species typical tG3t (Cuisian age: Khan et af. 1975; Drobne & Pavsie 1991; Pavlovec for SBZl3 and SBZI4 (Serra-Kiel et al. 1998). At the transition :sf et al. 1991; Pav,ic & Premec-Fueek 2000) was deposited in an from the Middle to the Late Lutetian (NPI5-NPI6), a subsiding >(,) ."~ elongated syncline with gently uplifted limbs of Palaeocene and deep-marine basin developed (Drobne 1977; Cosovi" & Drobne &~i Eocene limestones. At the NE margin, there is a gradual 1998; Krivic 1982, 1988; Marinko et al. 1994). ~ 0 ~ transition from limestones to deep-marine sedimentation (Drobne <2 1977; Pavlovec et al. 1991; Knez 1992). At the SW side, this Significant stratigraphie boundaries ~I ~ f!} j change is more rapid and partly tectonically induced. Deep- In the Slovenian Karst region, the KlPg boundary is present at marine sediments of the Trieste-Komen plateau (Kras area) are several localities (Drobne et al. 1988a, b, 1989, 1995, 1996a; ~I ~

Palinkas et al. (1996) and Hansen & Toft (1996). In the deep- Slovenian Palaeogene Basin and the Hungarian Palaeogene Basin marine basins the KlPg boundary is known from several (Csontos et al. 1992; Jelen et al. 1992, 1998; Fodor et al. 1998). .~'" g :~u localions where it is developed as ooze deposits (scaglia) or E ~g~ Subsequent eonlinenta! extension (rifting) in a backarc setting ~ c~'"E N~ within the Podsabotin Formation. The hiatus spans the lowermost resulted in the formalion of rapidly subsiding grabens/sub-basins ~ iä~_c2 ~ Palaeogene (Sribar 1965, 1967; Pavsie 1977, 1981, 1994; Perch- from Karpatian unti! Middle Badenian times. Synrift subsidenee ~ i~ ~- j 1 J <=h-~~~-- E .£ Z .~ ~ Nielsen & Pavsie 1979). eeased near the Middle-Late Badenian boundary. This was ~~2g~ ~.~.~i ~I~~i ~~Ii:'a::l=::J ~ g ö _ ~ ~ 0.;::: Iii' situated within the transitional beds between SBZ4 and SBZ5 Badenian nonnal faults. In the Pliocene, the climax of compres- ","' ~s (Fig. 17.28). It is charaeterized by Laeazina blumenthaU, Thoma- sional activity caused intense folding, accompanied by basin ~ ~ gf~ Ei ;; sella labyrinthiea and also by a change from Opereulina to inversion, and strike-slip faulting, accompanied by the formation ~."- 18 ;~e~ä Alveolinid~Nummulitid limestones. A 0 0 excursion was fauod of small pull-apart and transtensional basins. .- ~ ~ "" Q in younger beds of SBZ6. It reveals a decrease from -2%0 to ~~-~~~ -8%0 (PDB), and corresponds with the Palaeocene-Eocene Sedimen/ary and stratigraphie development lL >V> ~~~-~~ thermal maximum (Pujalte et al. 2003). Jelen et al. (1992) defined four tectonostratigraphie units that ~ <'2 ~ ;g ~;, .::.0....:1 L Sioven/an Paratethys bas/ns (B.J., H.R., D.S., M.Po., over a wide area north of the PAL (Northern Karavanke f- ~.~~~~ RK.) mountain range, Pohorje Mountains, Pannonian plain of NE f- ~ s ~~ [~ 1: '1 Slovenia) and eontinues in the Styria (Austria) and in Ihe Zala 1 The Paratethyan deposits of Slovenia (Figs 17.29 & 17.31) are .~;S~~ @ 5 area and Little Hungarian plain. (2) Unit A2 exlends in a very preserved in the Alpine and Dinaric foothills in the cenlral and 8 ~g'~t3 c- narrow belt between the PAL and the Donat Tectonie Zone =s< g.-.ö6 . ft:' SE part of the eountry, in Ihe rolling hills and plains in the east -l:;l"'"- t, and NE, as weil as in same Alpine valleys in the north and NW (Southem Karavanke mountain range and the Haloze Hills !:";;':2~E'3 V :! ~.~:i E.s , of thc country. From the margin of the Pannonian Basins System towards the Cakovee area in Croatia). (3) Unit BI extends in a g in the east, several long, narrow depressions, filled by Cenozoic narrow belt from the Julian Alps in the west and eastwards '5 ,~ li.2 .9~ between the Donat Tectonic Zone and the Sava-Celje Tectonic 15 ~ '6h~ ~ e deposits up to 2 km thiek, exlend towards the Alpine and the v;~~ß'O'~ Dinaric mountain chains in the west. Tbe westernmost Parateth- Zone ioto the Varazdin area in Croatia. (4) Unit 82 occupies a ~ ,5 ~ E ~ .5 oN wide area of central and SE Slovenia between the Sava-Celje N '" ~ 0 ~ ~ - yan deposits are found in the valleys of the Julian Alps. The g- ~>ftj Tectonic Zone and the ZZL and continues eastward to Croatia. co ~ N 1:- I' Dinaric chain separates the Mediterranean from the Paratethyan ~ ~(I)O~].H deposits. ::> E N liZ ~ ~ Palaeogene Tethys. The oldest Cenozoie deposits developed f- f- Jj :~-: ~N prior to the creation of the Paratethys Sea in the area under ~g.o'~~'o Tecton;c setting and palaeogeography consideration are described above. Other pre-Paratethys remnants N '«Vi extension and flooding during the middle Late Eoeene. Block Cretaceous Gosau beds are unconformably overlain by coal- 8 ~ ~ '2 ~~... ._ 0.0 0 -.g ;:0.: faulting is evidenced by scarp breccias, isolated small carbonate bearing platy and laminated marly limestones grading inlo shales ;:; ~ = ~.!< a .¥ After Egerian times, the process of post-collisional tectonic sequenees of the Guttaring Group of the Eastern Alps. -'! ..s u .~ ~ .ä ..s eseape (Ratschbacher et al. 1991) eontrolled Ihe development of .% w 'ö ~ ~ ::;-S .~ -~ou-< the area. The lateral extrusion process of the Aleapa crostal Polaeogene Paratelhys. Following the suturing of Apulia and ~J.:: z~ :g~~o.&ä ,., wo~ J"tc NOd NN"td S N"tIN3a"t9 }\ 993 N "t I ~ 3 9 3 N "t 111 3 J Sl)l N "t I N0 CI: block from the Eastern Alpine orogenie belt along the Periadria- the Austro-Alpine units, the area under consideration underwent ~.sd~g~ i'j N 9d N"tZ S3WNVINOl~0l ~l:l3S 9N"tl 1"t9Ic~nB Vlln "t N"tI!l.\fHJ N"t1l3dn~ B"tIl:ld:1- i tic Lineament (PAL) fault syslem and the NW part of the Dinarie subaerial weathering, and some bauxites were deposited. Subse- .~ --3N3JOlld 3H3JOIW 13N3J09110 3H3 ~~ ~~~~~ orogenie belt (Haas & Kovaes 200 I; Jelen et al. 200 I) along the quently, depositional basin developments began in Unit A2 g ~ ~ o M ~ ~ .~ 0. ~ ~ :~1 öl >! ~ ~ :!l M M ~ ~ Zagreb-Zemplin Lineament (ZZL) deformed and offset the within the nannoplankton zone NP19-20 (Jelen et al. 2000). g presumably uniform Palaeogene basin into the present -day :,;~ ~ "t1~Cl(,,):.=n,~~,~ These deposits erop oul sporadieally between the area north of ')~ 1100 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1101

Jeseniee and the Siovenian-Croatian horder (Mikuz 1979; The freshwater succession is topped by a c. 20 m thick succes. Mura-Zala Basin (Fodor et al. 2002), whieh was part of the Badenian extensional collapse (near the Middle-Late Badenian Drobne er al. 1985; Simunie et al. in Jelen et al. 2000; Jelen & sion of ealeareous silicielastics and limestones with a rieh Styrian extensional wedge of Ratschbacher et al. (1991) and of boundary) and the Late Badenian flooding of Hardenbol et al. Rifelj 2002). For Ihe Soeka area, the eo-existenee of a platform shallow-water fauna (Herlec 1985; Pavlovee 1999). the Raba extensiona! eorridor of Tari (1994). lt includes the (1998) resulted in the maximum extension of the Badenian sea. and a basin cao be assumed. Ta thc north, the sedimentary Radgona- Vas, the Mureek (Cmurek), the Siovenj Gradec, the Its westemmost remnant was found al Kamnik (Premru 1983). environments changed rapidly up-section, from freshwater to Egerian to Eggenburgian Paralethys. Within unils Bland B2, Maribor, the Eastem Mura-Örseg and the Haloze-Ljulomer- The collapse produced confined basins, calciruditic submarine margjnal-marine, to outer-shelf, and finally to bathyal environ- a complex tectonic load-flexural basin, with an inner thrust sheet Budafa grabenslsub-basins as weil as the Pohorje and Ihe Murska fans, turbidiles and laminaled muds, with blooms of benthie ments. Tbe freshwater, eoal-hearing strata and brackish calcar- within the present-day Sava-Celje Tectonic Zone, was formed Sobola extensional blocks. foraminifera tolerant to oxygen depletion. eous mudstones termed Ihe Soeka beds are well-known for during the Early Egerian. On the surfaee, these deposits extend During the first phase of extension in the Karpatian, bentbie Most of the Senovo and Krsko basins comprise Late Badenian their rieh flora (Unger 1850). They are overlain by ealeareous continuously from the Ljubljana Basin to the Siovenia-Croatia and planktonie foraminifers indicate deep:.marine, restrieted rnainly shallow-subtidal limestones and some calcareous mud- mudstones deposited on the shelf and slope. Nummulitid- border 10 the east and SE and eontinue to Croatia. The Celje environments. Proxy equations of van der Zwaan et al. (1990) stones. From the Krsko Basin, Mikuz (1982, 2000) deserihed a discocyclinid limestones were deposited on the platform to the foredeep basin, in front of the thrust sheet, reached an upper suggest that a water deplh of 840 m (:1:20%) was reaehed very rieh gastropod fauna. Tbe sueeession eould be daled by diatoms south, (leien et al. 2000). During tectonic eseape, the basins bathyal depth within less than one million years. The basal filling quiekly in the grabens. Tbey were filled by a mud/sand-rieh and silieoflagellales (Horvat 2003). were inverted and incorporated into tbc Southem Karavanke shows that ftexure began while the Smrekovec volcanism was system of gravity flows, and by dacite/andesite volcanielastics, In the Mura-Zala Basin, the combination of the second, strong shear zone between the PAL and the Donat Tectonic Zone (Fodor still active. The succession grades into marsh, brackish, shallow- with a sedimentation rate of 1000-2000 mlMa. Sediments were extensional pulse and a major eustatic flood resulted in water et al. 1998). and deep-marine environments. The transition to marine mud, derived from a fluviodeltaic system of muddy flooding rivers and depths of 880 m (:1:20%) during the laIe Early Badenian. The During the latest Priabonian (earliest NP21 or latest NP19-20 (several hundred metres thiek) of the underfilling stage look alluvial fans. These processes coincided with the formation of a lowstand wedge is overlain by transgressive coralline algal lime- zone; Baldi-Beke in Jelen & Rifelj 2002), the extensional basin- plaee near the Kiseellian-Egerian boundary (P21-P22 bound- signifieantly high relief in the Eastem Alps and the aetivity of a stones with Orbulina suturalis and Preorbulina circularis, fol. forming processes reached unit B 1. Unit BI deposits crop out in aryl (Rögl in Jelen & Rifelj 2002). These muds are similar 10 the number of strike-slip and normal faults (Kuhlemann et al. 2002). lowed by deep-water calcareous muds and rare turbidites. A various locations betwecn tbe Julian Alps in Siovenia and the Kiseell Clay in Hungary, and are oeeasionally interrupted by We assume that towards the end of this first phase, the extension sudden change to sand-rich turbidites elose to the final occur- Ravna gora in Croatia (leien & Rifelj 2002). The sueeession of submarine fans. A second volcaniclastic sequence within the established a connection between the Paratethys and the Medi- rence of Preorbulina circularis may have been related to the thc Smrekovec Basin, with a depocentre in thc Luce area, begins mudsIones was dated as laIe Early Egerian age (Iate NP25) terranean. This happened during the falling stage syslems trael eustatie sea-Ievel fall at the Lan2-Serl boundary of Hardenbol with algal-miliolid, nummulitid and diseocyelinid limestones. (Baldi-Beke in Jelen & Rifelj 2002). belween the Bur4 and Bur5/Lanl sequenee boundaries of Hard- et al. (1998); this was followed by an extensional eollapse These were suffocated by the oxygen minimum zone. Carbonate- Tbe Lasko back-bulge basin contains economically important enbol et al. (1998) as indieated by the eontemporaneous leap in creating confined basins. depleted mud was deposited on the outer shelf and upper slope coal deposits that have been intensively studied since the middle abundance of the benthic and planktonic foraminifera and the A sea-Ievel fall al the Badenian-Sarmatian boundary, whieh is during the Eocene-Oligocene transition. Frequent deep-marine of the nineteenth eenlury (Eltingshausen 1872, 1877, 1885; first appearance of species immigrating from the Mediterranean eorrelated with the Ser3 sequenee boundary of Hardenbol et al. carbonate gravity ftows interrupted the low suboxic slope calear- Bittner 1884; Papp 1955, 1975; Kuseer 1967; Mihajlovie & (leien & Rifelj 2003). The Karpalian marine sediments are (1998) and the MSi-3 isotopie event (Abreu & Haddad 1998), eous mud deposition. The latter ehanged, within the Oligocene Jungwirth 1988; Plaeer, 1999b). Voleaniclastie intercalations in limited to the Styrian extensional wedge and to the marginal eaused further facies differentiation. On the Kozjansko Block, part of NP21 zone, to suboxic basin-plain deposition with rare eoal were dated to 25:1: I Ma (Odin et al. 1994) and are basins/feeding eanyons south of the Donat Tectonic Zone. The shelf areas were temporarily subaerially exposed and subse- distal ealearenitie lurbidites. lts topmost part belongs to NP22. therefore correlatable with the second volcaniclastic sequence. Karpatian age of the brackish water, fluvial and mire deposits quently flooded hy the Early Sarmatian eustalie sea-Ievel rise The deepest sediments are the non~calcareous siltstones of the A basin north of the inner thrust sheet (i.e. in unit BI) also west of the wedge has been assumed on the basis of the observed (Riznar et al. 2002; Horval 2003; Rifelj et al. in press). Various early NP23, in whieh deep-water agglutinated foraminifera underwent tectonic load subsidence. Lenses of corallinacean interdigitation (Mioc & Znidarcic 1989). muds and laminated to bedded calearenites contain diatoms, faunas dominate (leien & Rifelj 2002). limestones in the shallower part of the inner thrust sheet, and The Karpatian-Badenian boundary in Slovenia corresponds silieoflageliates, molluses and plant remains (Horval 2003, and South of the Lute depocentre, in the Gornji Grad area, delta4 submarine gravel fans in the deeper part, were deposited on the wilh the Styrian uneonformity (Mioc & ZnidarCie 1989) and Ihus referenees therein). In shallow basins, discrete occurrences of plain deposition occurred before late NP22, when a transgression Smrekovec volcanics. Further to the north, there is a transition wilh the Bur5/Lan 1 sequenee boundary. Reeent studies (Rögl & Badenian/Sarmatian limestones of various thicknesses, and rich eommeneed (Baldi-Beke in Jelen & Rifelj 2002). The Gomji from volcaniclastic to siliciclastic sedimentation. Ouring the Rifelj, unpublished dala) suggesl, however, a position beneath in coralline algae, conformably overlie Badenian mudstones. Grad Beds (= Oberburg Beds) eomprise braekish silieiclasties underfilled stage, the norlhern basin was filled by about 600 m of the Styrian unconformity, corresponding with the increasing Limestones and mudstones are overlain by laminated caleareous and marine limestones rich in coralline algae, bryozoa, corals, Early Egerian sediments similar to the Egerian Szecseny Schlier abundance of foraminifera and Mediterranean invaders. This shales or calcareous mudstones and ealcarenites. Sandstones, larger foraminifera and molluses (e.g. Hauer & Morlot 1848; in the Hungarian Palaeogene Basin. finding is in accordance with the observation that the cooling eonglomerates, days and corallinacean limestone, containing Reuss 1864; Barta-Calmus 1973; Nebelsiek et al. 2000). They Channel formation occurred prior to the deposition of the events Mi-2 and MLi-1 are younger than Ihe proposed age of the braekish molluses (Bittner 1884), and in the deepest basins are overlain by shelf-muds and bathyal turbiditie muds (Seherba- second volcanielastic sequence. They indicate a change in the Burdigalian - Langhian boundary at the first occurrence of turbiditic sandstones, cover the calcareous mudstones and calear. cher 2000; Sehmiedl et al. 2002, and referenees therein). East of flexural basin development. Subsequently, the sedimentation rate Praearbu/ina sicana (Abreu & Haddad 1998). The Styrian enites. During the Sarmatian, episodes of marine/brackish condi- thc depocentre, in the Mozirje area, the transgression began in increased relative to the rate of subsidence and an overfilled unconformity in this area is a product of tectonic activity and a tions alternate with brackish/freshwater conditions (Horvat 2003; early NP23 (Baldi-Beke in Jelen & Rifelj 2002). Massive basin developed. The interplay of subsidence, sea-Ievel f1uctua- eustatic sea-level fall. Rifelj et al. in press). The westemmost Sarmatian deposits are calcareous mudstones, in placcs rieh in molluses, as weil as tions and sediment supply resulted in the accumulation of The Early Badenian was a time of significant paleogeographic known from Kamnik (Premru 1983), where ealeareous mud- laterally adjaeent nummulite limestones, are overlain by a black >300 m of sediments. These deposits are best preserved to the changes caused by a second, streng extensional pulse and the stones with braekish-water molluses (Kühnel 1933) and diatoms laminated mud containing fish and plant remains (6sh slates of east of Celje and Lasko. The delta-front shelf tilted towards the Langhian eustatie sea-Ievel rise of Hardenbol et al. (1998). (Horvat 2003) are overlain by poorly eonsolidated silieielasties. Teller 1896). In the shallower oxygenated grabens, a mud similar north and alternations of sand and mud accurnulated rapidly. At Between the Donat Tectonic Zone and the ZZL, the Kozjansko In the shallow parts of the Mura-Zala sub-basins, lowstand to Ihe Kiseell Clay of Hungary was deposited. In the deep sub- the shelf break, glaueonilie sand aeeumulated. Cross-bedding erustal block underwent normal faulting and presenl-day east- coarse elastics are overlain by sporadic corallinacean limestones, sill grabens, deposition of black laminated muds, interrupted by and coal oecur at the top of the stacking. west trending faults were reactivated as scissors faults. Ouring mudstones and siltstones with molluscs and plant remains. In the carbonate gravity flows, continued. The locality is historically The Adria push and the cloekwise rotation of the Tisza Unit, the concurrent range zone of Orbulina suturalis and Preorbulina upper part of the succession, poorly consolidated sandstones and known for its endemie fauna (Rolle 1858), whieh is now eonsid- led to inversion, dextral strike-slip faulting and displacement in circularis, flooding created accommodation space along the eonglomerates predominate (Mioc & Znidarcic 1989). Fan ered important for the biostratigraphie correlation of the central the Eocene and Oligocene basins. The premise for this displace- boundary-normal faults in the easlem part of the Kozjansko deposits and distal turbidites are the dominant sediment types in and eastem Paratethys (Baldi 1984). In the depoeenlre, non- ment is that the NW strike of the Sava- Vardar ophiolite zone Block and westward along the deep graben, following the eentral the deeper parts of the sub-basins. During the Late Sarmatian, calcareous silts were interbedded with volcanielastics derived ehanges to a NE slrike along the Zagreb-Zemplin Lineament scissor transfer fault. The subsidence rate was very high and the the Neogene sedimentary sequenee was loeally deeply eroded from the Smrekovee volcanism which occurred within the ear- and erops out again in NE Hungary (Bükk Mounlains) along water depth may have reaehed 500 m. The late Early Badenian due to tectonic upHft and a major eustatic sea~level fall at the liest NP23. The Smrekovec volcanielastic deposits originate with the Szepvölgy Limestone, the Buda Mari, the Tard Clay, the transgression was aecompanied by the formation of organic Ser4fforl boundary ofHardenbol et al. (1998). mostly from gravity flows and reach an estimated thickness of Recsk voleanics and Egerian deposits, all similar to deposits in buildups composed of corallinacean algae, bryozoans and corals. 800-1000 m (Mioc 1983; Mioc et al. 1986). the Siovenian Palaeogene Basin (leien et al. 1998,2001; Haas & Rhodoliths with diameters of up to 15 em oeeur (Anieie & Pannonian sensu stricto to Pontian Paratethys. The Late The Rupelian foraminifera fauna (Herlee 1985; Drobne et al. Kovaes 2001). Ogorelee 1995). The short-Iived earbonale platforms were soon Sarmalian uplilt and erosion was followed by the Early Pannonian 1985; Pavlovee 1999), and its position within the Julian Alps teetonieally lilted and deslroyed (Kazmer et al. 2005), followed subsidenee and flooding. On Ihe flanks of the Mura-Zala sub- nappe structure, suggested that unit BI continues in the sporadic Karpatian to Sarmatian Paratethys. A phase of east-west to by the deposition of bathyal mud and ealeareouslsilieiclastie basins, Pannonian mudstones interspersed with sandstones onlap Cenozoic deposits in the Julian Alps nappe. These deposits, with NE-SW directed backare extension (rifting) created aecommo- lurbidiles. eroded Sannatian and Badenian rocks and the metamorphic a total thickness of more than 600 m, consist mainly of altemat- dation space in unit Al and a NNE-SSW oriented extension Continuous extension, which masked the eustatic signal, was basement of the Murska Sobota extensional block. Turbidite ing various silicic1astics, freshwater limestones and coal lenses. created space in unit A2. This resulted in the formation of the followed by the late Middle Badenian transgression. Tbe Late deposition continued in deeper parts of the basins. On the 1102 M. W. RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1103 Kozjansko Bloek, Early Pannonian deposits rransgrade over Dinarides-Carpathian orogenie bell. This eommeneed with the gene and Neogene. The Palaeogene basin development was Sarmatian, Badenian. or pre.Cenozoic rocks (Poljak 2004; Anicic subduetion of the European Plate below Afriea and eontinued compression, extension was also active during the Pleistocene 1991). Sediments of the Kozjansko Block are well studied in the mainly controlled by compressional events, which resulted in (Jamieie & Novosel 1999). In the Pleistoeene, the uplift of the with. the collision. post-syneollisional transpression, separation closure of the Western Tethys and uplift of the Dinarides, while Krsko Basin (Poljak 2004; Skerlj 1985; Stevanovie & Skerlj 1985, and easlward eseape of the Pannonian fragment, and finally basin Dinarides to Recent elevations caused erosion of the Neogene extension, interrupted by minor compressional events, controlled 1990) and the succession can be correlated with the seismie extension. Cale-alkaline volcanism apparentIy eommenced in the sediments and reduced the dimensions of the freshwater basins. sedimentation in the Neogene. The area of north Croatia and sequenees of Sacchi (2001) as folIows. Aggradational calcareous Eoeene and reaehed its e1imax during the Late Oligoeene and the Frequent earthquakes along the eastem Adriatic coast suggest north Bosnia was characterized by changing marine connections, muds containing Congeria czjzeki and progradational sands con- earliest Mioeene. It eeased during the Badenian. The youngest that compressional tectonics is still active today (Prelogovic & taining C. praerhomboidea are equivalent to the PAN-2 (Fig. typieal for the Central Paratethys. voleanic rocks are alkaline basalts that extruded after the main Kranjee 1983; Papes 1985; Herak 1986; Blaskovie 1999; Dragi- 17.31) seismic sequence of Sacchi (200 I). The overlying aggrada- The formation of the Palaeogene basin in the area of north eevie el al. 1999). extension of the Pannonian Basin during the Upper Plioeene- Croatia and north Bosnia was related to Jurassic/Cretaceous tienal sandy calcareous muds with C. rhomboidea and thc Romanian. following progradational calcareous muddy sands with a coal subduetion along the north Tethyan margin. This initlated the Sedimentary and stratigraphie deveJopment The Oligoeene to Early Mioeene magmatic period along the deposit on the top is equivaJent to the PAN-3 seismic sequence. gradual closure and shortening of the Dinaridie Tethys and the easternmost seetor of the PAL was very intense. It yielded Palaengene. In the north Dinarides (Le. north Bosnia), Palaeo- Tbe youngest deposits are calcareous muds containing brackish. development of a magmatic arc. In the trench associated with gene sediments form part of a Late Karavanke and Pohorje tonalite and granodiorite intrusions Senonian~Palaeogene water ostracods and are equivalent to tbe PAN-4 seismic sequence. this magmatic are, Late Cretaceous-Palaeogene deep-marine sedimentary sequenee. The KlPg boundary is frequently eharae- (Altherr ef al. 1995; Pamie & Palinkas 2000) and voleanie rocks Tbc C. czjzeki aggradational unit corresponds with the Pannonian sequences accumulated. Compression at the end of the Eocene of the Smrekovec suite whieh eneompass the Smrekovee volcanie terized by 'a significant biostratigraphie diseontinuity (Polsak sensu striclo (sensu Stevanovie 1951, 1990). The C. praerhomboi- was aceompained by uplift of the Dinarides (Pamie el al. 1998, 1985). The uppermost Cretaeeous-Palaeogene sedimentary se- complex and the oeeurrenees of pyroclastic and voleaniclastic dea progradational and the C. rhomboidea aggradational units 2000a). This eaused the formation of loeal alluvial environments rocks extending from NW Siovenia (Peraeiea) via Sava Folds to quence consists mainly of turbidites deposited in a narrow basin correlate with the Transdanubian (sensu Sacchi 2001). The second in eastern Croatia (Halamie el al. 1993). (Jelaska 1978). The deep-marine sedimentation, starting in the the Celje, Lasko and Mura basins (Hinterleehner-Ravnik & progradational unit plus PAN-4 are correlatable to the Pontian The Neogene basins of north Croatia and north Bosnia were Pleniear 1967; Kralj 1996, 1999). Voleanie rocks of the Smreko- Maastrichtian, consists of individual graded sequences. It is sensu slriclo (sensu Sacchi 2001). Other remnants along the part of the south Pannonian Basins System (PBS), and were dominated by sandstones and shales during the Maastrichtian and vec suite range in eomposition from basaltic andesite to rhyolite, formed due to the eollision of the European (Tisia-Moesia) and Siovenia-Croatia border are Pannonian marls and marly clays and mainly exhibit a medium-K affinity. Palaeocene, while calcareous shal'es and sandstones, sandy lime- interspersed with sands and sandstones (Anieie 1991). the African plates (Horvath & Royden 1981; Horvath 1995; Three main volcanic lithofacies groups were recognized: stones and limestones prevail during the Early and Middle In the Mura-Zala Basin, the delta began to prograde into the Kovae ef ai. 1998). Following separation of the Western Tethys coherent, autoelastie and volcanielastie types (Kralj 1996). Eocene. These deep-marine sediments are eonformably overlain basin during the Sarmatian, and in the Krsko Basin during the into the Paratethys and Mediterranean during the Late Eocene, by late Middle Eocene limestones. This succession reftects the Coherent rocks are developed as lavas, shallow intrusive bodies early Transdanubian. By the end of the Pontian, the delta plain the northern part of the uplifted Dinarides beeame emergen!. or volcanic vent fillings. Marginal parts of lavas and shallow Palaeogene tennination of subduction and- the convergence of extended over bath basins. Transdanubian sediments attain a During the Oligocene transpressional phase, a Periadriatic dextral stable Africa and Eurasia in the area of the northern Dinarides intrusive bodies are commonly autobrecciated with a tendency to thiekness of 350 m in the KrSko Basin and 500 m in the Mura- strike-slip fault, controlling the formation of the SW margin of grade into hyaloclastite breccias and peperitic breccias. Peperites (Ielaska 1978; PolSak 1985; Pamie el al. 1998). Tectonic uplift the PBS along relicts of the previous subduction zone, was Zala Basin; the thiekness of Pontian sediments in the two basins are less common. and erosion of the Dinarides took plaee at the end of the Late is 1100 m and 1700 m, respeclively. It is not clear, whether this generated. The passive, lithosphere-generated rifting processes Eocene and Early Oligocene. Volcaniclastic deposits are the most widespread lithofacies was the result of post-rift subsidence or post-rift aetivity coupled led to the formation of elongated half-grabens during the synrift The Palaeogene sediments occur in scattered outcrops and in group. Submarine pyroclastic flow deposits of dacitic to rhyolitic with the inereasing intraplate stress caused hy the Adria miero- phase. This began during the Ottnangian and lasted untll the the subsurface of NW and central Croatia. Palaeocene sediments composition can be > 100 m thick, and consist of pumice and plate CCW rotation (Marton el al. 2003b). This movement began Middle Badenian. At the end of the Karpatian, uplift commenced voleanic glass shard-rich tuffs (Kralj 1999). Seeondary voleani- include marine clastics and limestones such as algal and coral at c. 9 Ma, whieh is the time of the opening of the Tyrrhenian as a consequence of the rotation of fault blocks around a clastic deposits are abundant in the Smrekovec volcanic complex limestones (Ielaska el al. 1970; Sikie el al. 1979; Pikija 1987). At Sea (Ielen & Rifelj 2005a, b). horizontal axis. Thc uplift was contemporaneous with sinistral the beginning of the Eocene, sedimentation of the Cretaceous- and comprise volcaniclastic debris flows and turbidity flows. NE-SW strike-slip faulting, which was transverse to oblique to They form internally stratifieli, fining-upward sequenees. Palaeogene deep-marine succession was interrupted, and initial Pliocene. Intense folding and the development of pop-up strue- the master WNW-ESE elongated struetures causing CCW emergence occurred in NW Croatia. The emergence phase lasted Late Pliocene alkaline basaltic volcanism occurred in the tures supplied material to alluvial fans and ftuvial systems; e.g. rotation and the destruetion of the elongate half-graben struc- until the Middle Eocene, when terrestrial elast accurnulations northwestemmost margin of the Mura Basin in the Late Pliocene the Haloze part of the Ljutomer-Haloze-Budafa sub-basin was tures. This loeally redueed the effects of uplift (Iamieie 1983; were ftooded by a marine transgression (Simunie el al. 2000). (Romanian). This volcanism is related to the extension of the Pavelie el al. 1998, 2003; Marton el al. 1999b, 2002b; Pavelie positively inverted and about 2000 m of sediments were eroded Pannonian fragment and upwelling of the asthenosphere (Embey- Several Eocene sediment types occur in NW Croatia: Early (Sachsenhofer el al. 2001; Fodor el al. 2002; Marton el al. 2001). Eocene limestone bre.ccias, calcarenites, shales and conglomerates Isztin & Kurat 1996). Alkali basaltic voleanism oecurred in a 2002a). Coeval strike-slip faulting ereated small pull-apart and The post-rift phase lasted from the Middle Badenian to pass upward into reddish-brown gravels, sands and tuffitic clays, fluvial environment characterized by rapid sedimentation (Kralj transtensional basins (Vrabec 1994, 1999) filled by lake sedi- Recent, and was characterized by thermal subsidence, which was and Early Eocene bauxites; Middle Eocene coarse-grained clastic 1995). Initial magmatic eruptions created a cinder cone with ments. interrupted by two compressional phases generated by intraplate limestone breccias and Iimestone-dolomite breccias; shallow- minor lava ftows. Occasionally. the style of eruptions became The Velenje Basin includes some of the best studied lake stress. The onset of the first period of intraplate stress took plaee marine Middle to Late Eocene limestones (coral biolithites, algal- essentially hydrovolcanic, producing pyroclastic surge deposits, at the end of the Sarmatian and may have initiated the uplift of sediments in the region. Tbe basin was presumably fonned during and in the final stage, large lahar deposits. Alkali basaltic foraminiferal biomicrites and biomicrudites) (Simunic et aJ. the Middle Pliocene as a transtensional basin with a half-graben blocks, resulting in base-level fall and partial basin inversion. 2000). volcanism can be correlated with the final stage of volcanic geometry (Brezigar el al. 1987; Vrabee 1999). Plioeene sediments Tbe second intraplate stress phase affected the basin during the activity in the neighbouring Styrian Basin (Poulditis 1981; Poschi Marine sediments are also known from the Oligocene of NW Pliocene, causing overall compression and structural inversion of this basin include basal silts with boulders, marsh and mire 1991), Little Hungarian Plain and the Bakony-Balaton highland Croatia. They are characterized by marls with sand intercalations lignite, shallow lake marls and clays as weil as massive and across the North Croatian Basin and north Bosnia. In these areas (Simunie 1992). At Mount Poz.ska (east Croatia), Oligocene (Martin & Nemeth 2004). Palaeogene voleanism of the Smreko- it was characterized by the fonnation of several compressional laminated elays with pebbly sands. At the depoeentre, near the vee Basin was reeenUy studied by Hanftand el al. (2004). coarse-grained clastics were deposited in an alluvial environ- Sostanj Fault, these sediments are about 1000 m thiek. struetures, subsidence, the uplift of basement blocks, CCW ment, thus reflecting the existence of continental conditions A change from the Taxodium to Fagus palynoftora in the rotations, and erosion (Marton el al. 1999b, 2002b; Pavelie 200 I; (Halamie el al. 1993). laminated clays represents the Middle-Late Plioeene boundary. Dinarides in norlh Croatia and Bosnia (D.P., M.B.) Tomljenovie & Csontos 2001; Pavelie ef al. 2003; Saftie el al. The Pliocene-Pleistocene boundary is transitional within the 2003). Neogene of north Croatia and north Bosnia. Neogene rocks The area of Croatia can be divided into three major units (Fig. transitional shallow lake/terrestrial silts and sands. Shallow-water Tectonic activity was the main external control on sedimenta- 17.26). (I) The Pannonian and Peri-Pannonian area eomprises cover a large area of north Croatia and north Bosnia (Fig. 17.32). lake deposits are rich in molluscs, mammals and plants (Brezigar tion in the Neogene intramontane basins of the Dinarides and it the lowland and hilly parts of east and NW Croatia. (2) The hilly Tbe thiekness of Neogene deposits is highly variable and is more ef al. 1987). Lamination is interpreted as being related to can be assumed that both compressional and extenslonal events that 6500 m in the Drava depression. Egerian-Eggenburgian and mountainous Dinarides separate the Pannonian Croatia from planktonie stratification in a eutrophie lake. The geology influenced basin evolution. The Dinaridie intramontane basins the eoastal region. (3) The Adriatic Area ineludes a narrow brackish-water to marine sedimentation was restricted to the and petrology of the 160 m thiek uniform lignite seam was were formed after the uplift of the Dinarides due to compression. coastal belt separated from the hinterland by high mountains. Hrvatsko Zagorje Basin, i.e. to the area of the PAL (Simunie el al. Most of the Dinarides became ernergent during the Palaeogene studied by Brezigar (1987) and Markie & Sachsenhofer (1997). This is predominantly a karst area. 1990; Pavelie ef al. 200 I). Marine deposition continued into and normal faulting may have eaused the formation of small Ottnangian times. VoJcanism tectonic depressions during the Oligocene and Neogene. Tectoru- Tectonic setting South and SE of the Hrvatsko Zagorje Basin (i.e. south Cenozoic volcanic activity in NE Slovenia is closely related to cally-eontrolled subsidence facilitated high sedimentation rates, Pannonian Basins System), alluvial and lacustrine .sedimentation The geological evolution of the areas of central and northem the tectonic evolution of the Pannonian Basin within the Alpine- although Pleistoeene tectonies may have generated differential commenced in the eacliest synrift phase (Paveli6 & Kovaci6 Croatia and Bosnia and Herzegovina differed during the Palaeo- uplift of the Dinarides (Soklie 1970; Herak 1986). In addition to 1999; Pavelie 200 I; Saftie ef ai. 2003). The occurrence of 1104 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1105 NORTH CROATIAN BASIN HRVATSKO ZAGORJE BASIN Jrfastodon angustidens indicates a non-marine development dur- except for the SE part, which was probably ftooded from the 00. o. _u ••• NORTHERN BOSNIA REGION ing the Early Miocene of the Tuzl. Basin (Soklie & Malez • 0 ••• 0 "'0 Adriatic Sea. The thicknesses of the Neogene deposits in these "0 " ••• , 00 1969). During the Late Ottnangian, a hydrological!y open lake basins vary from a few hundred to 1900 m in the Livno-Duvno ~:::::: ..::.:.:. 5 •••• ~ ••••• o~ 0 0 h E 00 •••••••••• h --0_.--0 covered the whole area. Lacustrine sedimentation was accompa- Bastn and more t~an 2400 m in the Sarajevo-Zenica Basin. ~w ~ ••••• <:>0 ••••• ~~~1~~.::?-...:._:.-:.+ -0-0. ~I00 •••••••••• ~~ ~~ nied by explosive rhyolitic voleanism (Mutie 1980; Vrabac 1999; However, the stratigraphy of these freshwater deposits is still ;~ '" - -- -- ~g 00-0...._ ..... --~.. _o_o.a Pavelic 200 I). Marine environments commenced during the problematic (Pavelie 2002) . ~~:':'.::?-1i ~~ --00_0 ...... c::::oC::::Oo •• 00 Karpatian (Pavelie 2001; BajraktareviC & Pavelie 2003; Saftie el The oldest Neogene sediments belong to the upper part of the 'ba ••••:: •.:.=- 1"::::::::::::.°, ...... , al. 2003). They are characterized by calcareous siltstones with Oligo-Miocene series. Siliciclastics include conglomerates, sand- ...... __ • __ • a ••••••1 ...... - - :: :::::: :::.:~ . . intercalations of c1astics. The Karpatian sediments in the Tuzla stones, marls and clays. Characaean limestones and eoal beds are ...•• ••••••.... O. " __ ...... 0" ••••••• _ ...... _- sub-basin contain rock-salt and pyroclastic layers (Vrabac el al. sometimes found. Similar conditions occurred in the Early ...... - ...... ------_---- 2003). Miocene, and were followed by sporadie volcanic activity. Fresh- •• 0------.... ~,~:.::-i~ Duc to a relative sea-Ievel fal! at the end of the Karpatian, water endemic bivalves (Congeria) had their main phase of some blocks were exposed, which local!y resulted in the evolution at this time (Kochansky-Devide & Sliskovie 1978). Q.I; ~ -0-.-'-'•••••••• --.-.-- complete erosion of Early Miocene deposits and the exposure of Middle Miocene deposits are similar to those of the Early 0" •••• '0' • __ ...... o' •••••••• _ ~ ...... basement rocks. The eroded siliciclastics were transported into Miocene. Marls, limestones, sandstones, days and conglomerates ...... -- el 0" ••••••• _ ~~ ------....------high-energy, shal!ow-marine environments (Pavelie al. 1998; J. predominate. Pyroclastics oeeur in some areas. Thick marly ~. --_....-•...... • •...... •-- Velie et al. 2000), and also into the relatively deeper sea (Pavelie limestone units with oecasional coal seams are Middle and Late ~ k'------.....-.- --•...... •...... ------et al. 1998). A deepening event during the Early Badenian Miocene in age. The Upper Miocene and Pliocene deposits are ~~ i~ caused the deposition of marls and gravelly calcarenites in the ~ I characterized by marls, clays, siltstones, sandstones, conglomer- i~ iI:::::::::::::::~~~:~ _------offshore areas (Pavelie et al. 1998). During the Late Badenian, ates, limestones and coal seams. Pliocene sediments are known i------1 the transgression ftooded the peaks of the exposed blocks, which from a few localities, such as aseries with lignite in the Livno- ~ ••••••• o. _ ~------had formed isolated islands during the Early Badenian. Marine Duvno Basin and the Sarajevo-Zenica Basin. The youngest ...... --- - ....-...- ... I••••••••••••• sedimentation commenced with the deposition of gravels, which Pliocene to Pleistocene sediments are found in the intramontane are overlain by coral!ine algal beds. Further deepeniog resulted basin in the NW Dinarides (Jurisie-PolSak et al. 1997). in the deposition of marls. In the Early Sarmatian, the salinity of '100.--- 0 B ~:-_:-:..::-::-:..: the sea decreased, and the environment became mesohaline. The Volcanism p isolation of the basin caused a sea-Ievel fall during the latest Palaeogene magmatic rocks in north Croatia and north Bosnia --- •••• 00 Badenian, which resulted in the resedimentation of older Bade- were generated by the collision of the NE parts of the Apulian nian faunas (Pavelie 2001; Saftie el al. 2003). A subsequent Plate and the SW margin of the . The final stage

~ ,_., 0- transgression resulted in widening of the basin. Laminated marls of this subduction is recorded by the sedimentary, magmatic and ...... ------~ e - ••• - ...... ------=. - .... (similar to varves) and massive marls dominated in this period, metamorphic units of the Prosara and Motajica mountains in ~ ~ ~:..~~-_::-::':::.: and the episodic input of sands took place by sediment gravity north Bosnia, which are interpreted as remnants of a subduction- flows. The exc'ellent preservation of the lamination may reffect related magmatic are (Parnie 1977, 1993; Lanphere & Pamie ------_ .•._~-.•..•..•. ~ anoxie conditions (Pavelie 200 I). 1992). [n north Bosnia, granitoids occur both on the surface and -*_~_~~_o:::.~": The ecological conditions changed during the Early Panno- ___ --00. the subsurfaee. They oecur as veins and small- to medium-sized ::~~T~0~f~f20~ff nian. The environments became brackish (oligohaline) and synkinematic plutons in medium-pressure metamorphie rocks. LLLL :_:_:_9.~ I locally freshwater, which caused the development of endemie Isotopic ages of Mesoalpine granitoids, which are associated molluscs and ostracods. Early Pannonian deposits overlie Sarma- with andesites and dacites, range from 48 to 30 Ma. In the ~ ~ I;:: -L -~ö;:;o tian sediments almost conformably and include lacustrine pJaty ~ e L L 0 c:>O basement of the Neogene of the north Croatian Basin, rhyolites ~I:~:-o-.:::=____ v _ ~~LLoo"", and thin-bedded, littoral limestones. Resedimented Badenian of the ophiolite complex yielded ages of 67-47 Ma (Parnie ~ ~I;-:-:~;-;-;-:-:~;-;-: ;i L L •••••• •••• ---_1\- fossils are abundant in the middle Pannonian deposits, reffecting 1993; Tari & Pamie 1998). ____ "'~~"'.o ------•• 0 1- .••• OD ------•• 00 a short-Iived latest Sarmatian period of emergence and erosion. Neogene volcanism is generally related to extensional pro~ A subsequent lake-level rise affected the dominance of marls eesses, except for the oidest volcanic units. Volcanie rocks ffi ~ ....•. _------with occasional siliciclastic inffux. Ouring the Pontian, gradual oecue mostly in the area of the Hrvatsko Zagorje Basin, and in shallowing is reftected by the increased terrigenous sedimenta- I~~I;.,,:.:::; : v<. :: ~a 'I:: :::: ::.::~ the northem part of the North Croatian Basin. Le. in the Drava •••••••••• 00 ~ ••••••••• < 1\" tion within a prodelta environment. Sedimentation tenninated depression. These rocks are divided into several volcanic ~ ••'.0°00 ~~ ~i during the Pontian with sandy delta progradation and the formations: the Egerian-Eggenburgian dacite-andesite forma- 000000 ~Po •••••• (tatite) formation, the Badenian andesite-basalt formation with i /> P~bo't:>. Late Miocene deposits are overJain by Pliocene siliciclastic subordinate dacites and rhyolites, and the post-Badenian basalt~ ~.c:~':..::.~: Pz,~Pg OlIGD-"o1IOCENt Ö-.-6 ~;;;,-."0 ...... sediments accumulated in small freshwater lakes, swamps and alkali basalt formation (Parnie 1997; Pavclie 2001) . -- < •••.•• .) •••.•• --- •....1.",,>----- rivers. Pleistocene deposits are comparable to those of the The rocks of the Egerian-Eggenburgian dacite-andesite for- Pliocene, except for the remarkable amounts of aeolianites (1. mation are known only from the Hrvatsko Zagorje Basin and w~ LEGEND ...... -- gHmestone Velie & Durn 1993; J. Velie & Saftie 1999; Saftie el al. 2003). from neighbouring Slovenia. They may be associated with ...... - i~ ...... ----- brackish.water and marine sands, sandstones, marls, breccias and '" .----- A~ .... ~ volcanicrocks Qm," Neogene intra montane basins of the Dinarides. In the Dinar- conglomerates (Simunie & Pamie 1993). The main phase of Tß ~~~~...'2~:'.._-_- ides, sedimentation of Neogene freshwater sediments began Alpine deformation (Le. the Pyrenean phase), which was ~. VA>'" --- day ~~ I,:;o] ized by frequent lateral and vertical facies variations as a result volcanic activity. Lacustrine sedimentation was aecompanied by .- ••0 ••••••• E:;l coal ~ coarse.gralned dastics of independent local basin developments. Throughout Bosnia explosive volcanism, resulting in the deposition of tuffs and and Herzegovina as weil as eentral and south Croatia, earliest tuffites, reftecting the commencement of rifting (Mutie 1980; Flg.17.32. Geological columns ofthe southem Pannonian Basins System. Miocene sedimentation was restricted to freshwater basins, Seavnicar el al. 1983; Pavelie 2001). ;!,;. ilO6 M. w. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE 1107

SARAJEVO-ZENICA BASIN

LEGEND ::?-:q:<;> ••••• -. N 00°00° l~v;1wodastlcs 1c:..05'~~::------

W I:::::::::::: ~"'" e ------_-_-. I~:~~I,- ~ ~ :: -::.~.~.:: : ::! L1VNO BASIN .+' D- ...... 1----1 '""' ...... ---- ". : .:1 flne-gra!neddastl<:s ...... ------I~0cilcoorseogralneddastics ...... ------000000------:I;~~~~i8 00000=1 ------.~ ------.,:E ~~~:~.~.~ ...... W il ------. ------000000 °0°000 : 3 ~ 000000 Oooooc MOSTAR BASIN ------I°0=000 ...... 'f ...... ------• V ..J. , ~ BANOVICI BASIN • ~:~:~~Cioi::6=: . < ob 00000<::1 ------~' ------...... ~i ------~ . ------~ ------.~ . ------~ ------1 . ------:~ ~, ------, g , H ------'d --- - :~ L ------~~~-=-~=-~=-...... ?_~_C?_~_~I J ------I ~ ""

Fig. 17.33. Geological columns of the Dinarides intramontane freshwater basins. -.....:.

The Karpatian volcanics are known only from east Croatia. In the southem Dinarides, dacite-andesite' tuff beds found in They comprise a volcanic body of 5 km' on Mount Krndija made the Sinj Basin are interpreted as being derived from volcanic /0- up of traehyandesites and tuffs interlayered with marine c1astic sources in Bosnia (Susnjara & Scavnicar 1974). sediments. These volcanies may have originated from the partial melting of upper mantle rocks enriched in MgO (Golub & Marie Ouler Dinarides: eastern Adriatic coast (V.C., T.M., K.D., \ 1968; Pamie el a/. 1992/1993: Pamie 1997). '\ D The Early Badenian is eharacterized by a elimax in voleanic A.M.) BlgEVO activity. The rocks of the Badenian andesite-basalt fonnation, The eastem Adriatic coast includes two units: the autoehthonous with subordinate daeites and rhyolites, are the most widespread part (Adriatic carbonate platform) and the overthrust nappe •. volcanics in the North Croatian Basin (Lugovie el a/. 1990; system (Dinaric tbrust front), which is situated between the Pamie 1992). Peperites and pillow lava also occur (Belak el al. Dinaric Mountains and the Apennines, and includes convergent 2000). The thickness of the volcanics varies and is more than major structural units. Four particular domains can be distin- 1000 m in some parts of the Drava depression. They are also guished (Figs 17.24 & 17.34): (I) Istria with the Ciearija l1 found in the Hrvatsko Zagorje Basin. The volcanies are fre- Mountains at the NW part of the coast; (2) the northern Adriatic quently intercalated with marine clastics and marls. ln some (the coast with the islands of Krk, Cres, Losinj, Rab, and Pag); Fig. 17.34. Geological sketch map ofthe Croatian Guter Dinarides showing the location ofprincipal Cenozoic zones (modified after Geologie map of places pyroclastics oceur within algal limestones (Belak et a/. (3) Ravni kotari (northem Dalmatia with the island of Dugi Otok Croatia 1:300000, 1995). Zones of the Guter Dinarides: 1, Istrian peninsula and Cicarija Mountains; 2, northem Adriatic coastal region with adjacent 1991). The rocks of this formation probably originated from the and the Kornati archipelago); and (4) central to southem larger islands Krk, Cres, Losinj, Rab and Pag; 3, Ravni kotari region with adjacent Komati islands and Ougi Otok; 4, central to southem Dalmatian partial melting of the heterogeneous lower ernst (Parnie 1997), Dalmatia (the coast and the islands of Hvar, Brac and Korcula). coastal area with adjaccnt islands Hvar, Brac and Bisevo. and are a resull of the final stage of the synrift phase of basin evolution (Pavelie 200 I). Pa/aeogeography The rocks of the post-Badenian basalt-alkali basalt formation [n terms of palaeogeography, the studied region belongs to !wo are known ooly from a few weHs in the Drava depression. K- Ar different tectonic settings: the Adriatic Carbonate Platform continental runoff was low. Larger benthic foraminifers indicate deposits (Premee-Fucek & Zivkovic 2005). Fossil flora (Jung- measurements carried out on basalts yielded isotopic ages of (AdCP) (sensu Herak 1986, 1999; Tari 2002) and the Dinaric oligotrophie, warm-water conditions during Early-Middle Eo- wirth 2003) and coals from the Promina beds (Eoeene-Oligo- 11.6-9.4 Ma (Parnie 1997). The occurrence of these rocks has nappe realm (Herak 1986, 1999: or frontal thrnst of the western cene times, and their development reflects the Eocene to cene) indicate wet vegetation conditions on land. been interpreted as being related 10 a short-Iasting period of thrust belt of Tari 2002). According to the Eoeene palaeogeo- Oligocene 'greenhouse'l'ieehouse' transition (Moro & Cosovic Carbonate platforms, such as the extensive AdCP, are an volcanic reactivation during a post-rift phase of basin evolution graphie reeonstruetion of ButterIin el al. (1993), the AdCP was 2002) The global Middle to Late Eocene eooling trend is shown important element in the Guter Dinarides. Shallow-marine (Pavelie 200 I). situated at the northem fringe of the global desert belt, where by the planktonic foraminiferal associations of the deep-water carbonate deposition commenced in the Late Triassie and lasted 1108 M. W RASSER, M. HARZHAUSER ET AL. PALAEOGENE AND NEOGENE 1109 until the Lutetian transgression (Velie el al. 2003; Drobne 2003b, CCW rotations observed in the Adriatic region were driven by Vlahnvie et al. 2005). Carbonate deposition was terminated by that of the Adriatic foreland. This implies that the studied regions E Central- 'l! GI GI Clcarija Northem Ravni the Eo-Alpine tectonic phase, which caused uplift and emergence were rigidly connected and together participated in post-Eocene .5 '" 01 Southem .~ Kolari of the Dinarides, resulting in the formation of significant bauxite CCW rotation. ~ •.. S Istria Adriatic Dalmatia ~ w UI UI UI accumulations (Istria, Ravni kotari). Post-Eo-Alpine sedimenta- " * tion .commenced diachronously from Ilerdian to Cuisian times Sedimentary and stratigraphie development (Bignot 1972; Drobne 1977; Cosovie el al. 1994; Matieec el al. Generally, the oldest Palaeogene deposits of the area (Fig. 17.35) 25 UJ Cl: Z ~ CHATTIAN 1996; Marianac el al. 1998). UJ Q. are breecias overlain by freshwater or braekish and paralic Ü => The Cenozoic history of the cast Adriatic coast reflects the limestones (Kozina-type limestones, part of the Liburnian For- U 0 transition from a Cretaceous passive-margin setting (Dercourt et mation; Drobne & Pavlovec 1991) with local coal accumulations 30 Ö Cl: - W al. 1993) to a foreland basin evolution (Tari 2002). During the ..J 0~ RUPEUAN (Hamrl. 1959). Fully marine conditions were established during o ~ Early Eocene, a homoclinal carbonate ramp, the AdCp' devel- the llerdian to Lutetian (Drobne 1974, 1977), when foraminiferal - oped. Palaeogene carbonate ramps were subject to short-tenn limestones were deposited on carbonate platforms {Magas & 3S W ~'" PRIABONIAN tectonic controls, including subsidence and sea-Ievel changes. Marineie 1973; Korolija el al. 1977; Kosir 1997; Cosovie & 0 ~ Inner and middle camp deposits (Libumian formations and Drobne 1998; Marjanac el al. 1998; Drobne 2000; Velie el al. Z foraminiferal limestones) are widespread along the coast, while 2003; Cosovie el al. 20040). These are overlain by the so-called BARTONIAN 40 N W outer ramp deposits are rare in the north Adriatic region and Transitional Beds with the basal Marls with crabs and the UJ ~ north Dalmatia. Deep-marine sedimentation commenced after a overlying Globigerina ('Subbolina') marls. These sediments Cl Z g significant drowning of the Eocene carbonate platforms. reffeet the regionally diachronous deepening, which commenced 0 UJ ~ 4S 0 Ü during the Early to Middle Lutetian in Istria (Sikie 1965; Bignot 0 lUTErlAN Tectonic setting 1972; Drobne 1977; Benie 1991; Cosovie & Drobne 1995, 1998; W UJ Z Numerous studies have examined the present-day structural Cosovie et al 2004a) and during the Late Lutetian in Dalmatia architecture, tectonic evolution, and palaeogeography of the east (Pavsic & Premec Fueek 2000). Varying thicknesses were caused 50 « ..J '" Adriatic coastal region (Kossmat 1924; Petkovie 1958; Grubie by orogenie processes (Sikie 1965, 1968, 1969). Clastic Eocene w ~ YPRESIAN 1975; Dimitrijevie 1982; Pamie el al. 1998; Herak 1986, 1999; sediments of this area are traditionally referred to as flysch « 9 Picha 2002; Tari 2002). Although there is general agreement that deposits (e.g. MarinCie 1981; Marjanac el al. 1998). The onset of ss 0. UJ the east Adriatic coast consists of (an) autochthonous platform(s) deep-marine (flysch) sedimentation is diachronous, ranging from U THANETIAN Z ffi overthrust by nappes, the tectonic evolution is controversial. For Cuisian-Middle/Late Lutetian (Zivkovic 2004; Schweitzer et al. UJ Q. Ü ~ instance, Pamie el al. (1998) assumed a uniform Adriatic- SELANDIAN 2005) to Late Lutetian (Benie 1983); Bartonian (Benie 1983), 60 0 Dinaridic carbonate platform, while Herak (1986, 1999) distin- Bartonian-Priabonian boundary (Kraseninikov et al. 1968; Mar- UJ Cl: ..J W guished the Adriatic and Dinaric platforms, and this is supportcd & ineie 1981; Marjanac cl al. 1998) and to Priabonian (Pavsie « ~ DANIAN a. by biostratigraphic data (Drobne 1977, 2003b). Tari (2002) Premec Fueek 2000). Sedimentation lasted until the Priabonian 65 9 distinguished a gently tectonized Adriatic carbonate platform (NPI8; Benie 1991), Bartonian (Benie 1983) and Late OIigo- '. .' (Istria) with an imbricated margin (the so-called imbricated cene-Early Miocene (Puskarie 1987; De Capoa et al. 1995). (J Adria) and the Dinaric nappe pile. Deep.marine sediments are mostly overlain by the Eocene- Ö The Palaeogene development was characterized by several Oligocene eontinental to shallow-marine sediments of the Promi- LATE CRETACEOUS l:l not to scala tectonic events. The first of these caused an unconforrnity na Beds (Sikie 1965; Komatina 1967; Babie & Zupanie 1983), UI W between the Upper Cretaceous and Palaeogene strata (Parnie et which are overlain by the Jelar breccia (Oligocene and younger) :lE al. 1998), and perlod of tectonic movements must have been (Bahun 1974; Herak & Bahun 1979; Vlahovie el al. 1999). responsible for the SW vergence at the east Adriatic coast. During the Miocene, lacustrine sediments were deposited (Juri~ According to Pamie et al (1998), the second period of deforma- Sie-Polsak 1979; JuriSie-PolSak el al. 1993; Susnjara & Sakae tion took place during the latest Eocene to Early Oligocene. 1988). t1EEJl E32 11;3 ~4 85 Picha (2002) related NW-SE trending strike-slip faults to the opening of the post-Messinian Albanian foredeep in the Plio- Istr;a. The geological literature on [stria (part of the AdCP) is Fig. 17.35. Correlation chart of lithostratigraphic units from the Palaeocene to Pliocene in the different zones of the Croatian Outer Oinaridcs. Columns cene-Holocene (the third deformational event), which indicates plentiful, including !wo complex reviews by Bignot (1972) and correspond to the zones ofFigure 17.34. 1, Promina beds; 2, Flysch; 3, Transitional beds; 4, Shallow-marine carbonates (including Kozina-type of limestones, Foraminiferallimestones); 5, Shallow-marine limestones (zone 1 after Signot 1972; Drobne 1977; Drobne et al. 1979; Senie 1991; Drobne & the existence of escape tectonics in the region. Tari (2002) Drobne (1977), and many overviews (Drobne 1979; Drobne el Pavlovec 1991; Cosovie et al. 2004a; Zivkovie 2004; zone 2 according to Magas 1968; Mamuzie 1968; Mamuzie et al. 1969; Signot 1972; Drobnc 1974; suggested that folding .nd thrusting began in the Oligocene, al. 1979; Hagn el al. 1979; Drobne & Pavlovec 1991; Drobne & Benie 1983; Marton el al. 1995a; zone 3 according to Mamuzie et al. 1970; Ivanovie et al. 1973; Benie 1983; Drobne et al. 1991c; zone 4 according to when collision and progressive underthrusting of Adria beneath PavSie 1991; Cosovie 1991, Benie 1991, Marjanac 1991; Velie et Magas & Marineie 1973; Borovie et al. 1976, 1977; Korolija et al. 1977; Benie 1983; Susnjara & Sakae 1988; Oe Capoa et al. 1995; Marjanac et al. the Dinaric carbonate platform created imbricated structures at al. 1995, 2002, 2003; Sparica et al. 2000), The carbonate 1998; Pavsic & Premec Fueek 2000; Jelaska el al. 1003; Cosovic el al. 2004b). the margin of Adria; this process continued during the Miocene depositional regime, which prevailed throughout the Mesozoic, and thereafter. The typical NW -SE striking Dinaric structures lerminated during Ihe Early to Late Cretaceous (Drobne 1977; were refolded as a rcsult of neotectonic deformation (Marineie Matieec et al. 1996). Different Eocene succcssions transgraded ramp (Miliolid limestones), to shallower and deeper shoreface nodular clayey limestones and calcitic marls (Schweitzer et al. 1997), producing west-east orientated structures, wh ich are most over various Cretaceous units, which resulted in a high degree of environments (with conical agglutinated foraminiferal. Alveolina 2005; Tarlao et al. 2005), and the upper parts consist of thick (a prominent in the Central Dalmatian islands. lateral and vertical facies variability. The Liburnian Formation and Nummulites limestones), and to deeper parts of relatively few to several tens of metres), massive Globigerina (Subbotina) was deposited in the deepest parts of the palaeorelief. It is open carbonate ramps (Orthophragminae limestones). Facies marls with oceasional intercalations of thin sandstone beds. Palaeomagnetism charaeterized by alternating freshwater to brackish, lagoonal patterns refleet a general deepening.upward trend. This was the These marls are rich in planktonic foraminifera and glauconite Palaeomagnetic studies were performed on Cuisian to Lutetian Early Eocene deposits up to 80 m thick (llerdian to Cuisian; eonsequence of intense synsedimentary tectonics providing ap- grains. They were deposited in Middle to Late Lutetian deeper- platform carbonates from Isma and ccntral to south Dalmatia Drobne 1977). These are thin-bedded mudstones rich in organic propriate accommodation space and a relatively low sedimenta- marine environments (bathyal hcmipelagic deposits) (Cosovie el (Märton el al. 1995a, 2003b) as weil as on deep-marine matter and/or c1ayey mudstones, sporadically with stromatolites tion rate. Sedimentation commenced during the Middle I1erdian al. 2004a). sediments from Istria. These proved the existence of an Adriatic and coal interealations (Labin Basin). Their fossil content, well- (SBZ7; Serra-Kiel el al. 1998) in the Ciearija region, during the Deep-marine deposits crap out in the Trieste-Pazin Basin, micrnplate and demonstrate counterclockwisc (CCW) rotation known since Stache (1889), includes Charophyta and mnlluscs. Cuisian (SBZ IO-SBZ 12) throughout Istria, and during the Early Labin Basin, Mount Ucka, and partly at Mount Cicarija. These with respect to both the African and European plates in post- The early Eocene to Middle Lutetian foraminiferal limestones Lutetian (SBZ13) in its eastem part (Labin Basin; Bignot 1972). bathyal deposits (600 to 1200 m water depth; Zivkovie & Babie Eocene times. Istria must have rotated by 30° CCW, relative to in Istria (up 10 200 m thick) were deposiled in environments The Transitional Beds range from shallow to deep-marine 2003; Zivkovie 2004) are up to 350 m (Marineie et al. 1996). Africa and stable Eurnpe. The latest Miocene to early Pliocene ranging from the restricted inner parts of the carbonate platforml deposits. The basal Marls with crabs comprise <5 m thick They were deposited in a structurally controlled basin, which r' I1II r IUO M, W, RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE ':1 1,! was probably terminated by the orogenieally indueed rise of the was fed from the NW, NE, south and SE. The palaeotransport deep-marine sediments (Ivanovie et al. 1973). The Ravni kotari environment. Cross-bedded skeletal sands and imbricated largcr middle Dinarides. A good example for the tectonic contral 15the pattern was eomplex, although the central Pazin Basin shows a deep-marine deposits are Late Lutetian (NP16) to Bartonian foraminifers indicate the influence of major storm events. synorogenie Promina Formation (Late Eoeene-Early Oligoeene) predominantly longitudinal transport direction with respect to the (NPI7; Benie 1983). The Bekovae section indicates that deposi- The foraminiferal limestones are overlain by the so-called Transitional Beds, which comprise Marls with crabs and Globi- of Herzegovina, which developed during the Pyrenean Orogeny. basinal axis (Babie & Zupanie 1996). Tbe deposits are charaeter- tion extended from the Bartonian (plankton zone PI3, E12) to The Eocene final deformation of the Dinarides resulted from ized by an alternation of hemipelagic marls and gravity flow the Priabonian (PI6/17, E16: Drobne et al. 1991c) and was gerina (Subbotina) marls. Their thickness ranges from II m underplating of Apulia beneath Tisia (the present-day Pannonian deposits (Magdalenie 1972). The prevailing turbidite succession deposited in a deep-marine basin with mainly transversal palaeo- (central Dalmatian islands) to 15 m (south Dalmatia). The Basin terrains), which began during an Oligocene (32-28 Ma) of hybrid carbonateJsilieiclastic sandstones and marls is ran- current patterns. A elose relationship of sandstone bodies deposition of the Transitional Beds extends from the Late Middle period of transpression. This deformation gave rise to the final domly intercalated with thick carbonate beds of debrite origin, (depositional lobes) with channels indieates a lower-slope or Lutetian to the Late Lutetian and refleets a progressive deepening structure of the Dinarides, To the north of the uplifted Dinarides, i.e. megabeds (Hagn et al. 1979). Tbe succession is characterized base-of-slope environment (Babie & Zupanie 1983). Tbe latter is of the sedimentary environment. strike-slip faulting produced a system of smaller and larger by two distinet stratigraphie units: the lower marl-rieh unit with also indicated by the presence of olistolite-bearing megabeds Several hundred metres of deep-marine sediments were depos- transpressional depressions, mainly orientated NE and ESE. subordinate arenite interbeds, and an upper sandstone-rich unit. with huge shallow-marine limestone elasts. The deep-marine ited above the Transitional Beds. The contact can be transgres- During the Oligocene, shaUow- to deep-water, marine and The deep~marine sediments have a stratigraphie range covering sediments of north Oalmatia are overlain by the Promina Beds sive or transitional (Marineie 1981; Sikie 1965), The brackish to freshwater sedimentation took place in these depres- the Middle to Upper Eocene planktonie foraminiferal zones PlI (sometimes referred to as a 'formation'; Ivanovic et al. 1976) stratigraphie range is probably from the Bartonian (NPI7: Benie sions. Along the northem Dinarides margin, this dextral strike- to PIS (Berggren et al. 1995) or E9 to EIS (Berggren & Pearson which are characterized by progressive shaUowing of the basin. 1983) up to the Upper Miocene (De Capoa et al, 1995). A slip faulting i5 seen in the incipient Sava and Drava transpres- 2005). Babie & Zupanic (1983) located its base in a deep-marine Priabonian age has been proven for the oouth Dalmatian deposits olistostrome, and assumed an Eocene-Oligocene age for the (Pavsi<: & Premec Fueek 2000). In central Dalmatia, the sional faults, which apparently represent the ESE prolongation of the PAL (Pamie et al, 1998). Strike-slip faulting was accompa- Northern Adriatic. Tbe north Adriatie region (AdCP and entire formation. The lower part of the Promina Beds is sediments are divided into Lower, Middle and Upper Flysch nied by Early Oligocene volcanic activity. which took place in Dinaric thrust front) includes the north Adriatic islands (Krk, cbaracterized by an alternation of marls, sandstones, congtomer- zones. The Lower Flysch Zone is about 750 m thick and the northem Oligocene transpressional basins and along the Rab, Pag) and the adjaeent coastal region (Rijeka hinterland and ates, limestones and cherts, with freshwater to brackish-water dominated by megabeds, Tbe Middle Flysch Zone is a c. 200 m northem margin of the Dinarides (e,g. area of Maglaj and Vinodol area). Geological overviews are given in the geological fauna. Sedimentation of the upper Promina Beds is characterized thick olistostrome (Marjanac 1996). Within the 850 m thick Srebrenica). Oligocene strike-slip faulting was very active across maps of llirska Bistrica (Sikic et al. 1972), Delnice (Savie & by significant shallowing, which caused progradation of coarse Upper Flysch Zone, megabeds are restricted to the lower part; the Dinarides area and is evident in the presence of transpres- Domazet 1984), Labin (Sikie et al. 1969), Crikveniea (Susnjar et alluvial sediments. These conglomerates contain marly beds with conglomerates interfingering with turbidites and alternations of sional depressions as precursors of Neogene freshwater basins. al, 1970), Cres (Magas 1968), Rab (Mamuzie et al. 1969), Losinj coal and plant remains. The Jelar breccia is interpreted as the thin-bedded calcarenites and calcirudites and marls occur The largest transpressional faults are the Bosovaea Fault, which (Mamuzie 1968), Silba (Mamuzie et al. 1970) and Gospie (Soka<: youngest Cenozoic sedimentary unit in the area, but there are 00 throughout this uni!. Coeval with the upper parts of the Upper controlIed the origin of the Sarajevo-Zenica depression, and the et al, 1974). direct contacts between the deep-marine units, the Promina Beds Flysch Zone are Miocene laeustrine sediments on the island of Vrbas-Voljevac Fault, which controlIed the origin of some The oldest Palaeogene sediments are the Liburnian deposits, and the Jelar breceia. The age of the laner is uncertain, being Pag and inland in most of the karst poljes (Jurisie-PolSak 1979; smalter Cenozoic depressions. Within the AdCP, the Oligocene foUowed by foraminiferal limestones and marly limestones with possibly Middle Eoeene-EarIy Oligoeene (Herak & Bahun, Kochansky-Devide & SliSkovic 1981; Susnjara & Saka<: 1988; strike-slip faulting produced several larger and smalter karst crabs. The Liburnian deposits, and the freshwater and brackish to 1979), Palaeogene-Neogene (Ivanovie et al. 1973) or Late Jurisic-PolSak et al. 1993), valleys. ;: marine limestones, are of Palaeocene age (Thanetian, SHZ 4 in Lutetian-Bartonian (Saka<: et al. 1993). Palaeogeographieally, Bisevo Island extends far out into the Adriatic Sea and its fossil In the SPB, NE ofthe uplifted Dinarides, geodynamic processes li, Klana environs; Drobne 1974; Drobne & Cosovic 1998) and the Jelar breccia is an element of the Dinaric thrust front. content represents a geological peeuliarity. The Cretaceous- changed fundamentaUy after the Oligocene transpressional defor- Ili show a gradual transition to carbonate platform limestones Cenozoic stratigraphy and fossil content of the island differs from mation, Diapirism of the upper mantle and resulting attenuation of composed of alveolinids, nummulitids, assilinids, opereulinids those of the AdCP; instead the transgressive Oligocene sediments il the lower continental erust are manifest in the extensional and orthophragminids (SBZII-SBZI3; Krk island and environs Centra. and Southern Dalmatia. Palaeogene deposits of this of the island (Drobne et al. 2000a) are similar to those of processes that gave rise to the evolution of thc Pannonian 8asin of Rijeka: Bignot 1972; Drobne 1977; Schaub 1981; Ibrahimpa- region (AdCP and Dinarie tbrust front) primarily occur in Cephalonia, Greece (Accordi et al. 1998). The Cenozoic sucees- (18-17 Ma; Royden 1988). The extensional evolution of the SPB sie & Gusie 2000; Klepa<: 2003). They are overlain by mainly teetonie eontact with Mesozoic units, except for a few localities sion of the island beg ins with a characteristic interval of reddish was mainly predisposed by the original Orava and Sava fault deep-marine sediments, the deposition of which started diachro. (Solin and Trogir hinterland). Previous studies were conducted in to yellowish c1ayey marls, alternatLng with thin layers of nodular system, created during the Oligocene transpression. As a result of nously in Early Eocene (Rijeka hinterland; Bignot 1972), and the framework of regional mapping (Borovie et al. 1976, 1977; limestones. Tbe marls are overlaio by limestones with Nummulites the extension, marine transgression Gecurred, and the first phases Late Lutetian (P12 or Eil, Rab and Krk islands; Benie 1983) Herak et al, 1976; Korolija et al. 1977), stratigraphy and fichteli (SBZ 22, Rupelian-Chattian, sensu Cahuzac & Poignant of the evolution of the Pannonian Basin took place under rift- times, The Lopar (Rab) sandstones are unique in the east tectonics (Blanchet 1972, 1974; Chorowitz 1969, 1975, 1977; 1997). reiated, mainly marine environments. This rift-related Earlyl Adriatic realm, because they represent shallow-marine siliciclas- Sikic 1965) as weil as sedimentology and stratigraphy (Benie Middle Miocene filling of the Pannonian Basin was accompanied tics. The facies patterns document sea-Ievel changes and com- 1983; Drobne et al. 1988b; Puskarie 1987; De Capoa et al, 1995; Dinarides and South Pannonlan Basin in Bosnia and by synsedimentary volcanic activity, which took place during prise sandy marIs, heterolithic packages (sandstone-marl Marjanac 1996; Marjanae et al. 1998, Drobne et al, in press). Herzegovina (S.t., R,Red., H.H.) the Karpathian and Badenian. The first rift-related stage of the alternation), sandstones, calearenites, conglomerates and slumps. The oldest PaIaeogene deposits are known from the Split- evolution of the Pannonian Basin terminated by the end of the The age of this succession is uncertain, beeause specimens Makarska hinterland. Tbese are Danian to Early Thanetian (PI- The area of Bosnia and Herzegovina (Figs 17.2 & 17.26) is Sannatian. This was followed by the second evolutionary stage, resedimented from oider strata prevail among the nannofossils P3) limestones (Chorowicz 1977; Jelaska et al. 2003; Cosovie et mostly mountainous, encompassing the central Dinarides. The when continuous Late Miocenc and Pliocene freshwater sedimen- (Benie 1983). The deep-marine sediments are overlain by the al. 2006) whieh are overlain by Early~Middle Eocene (Ypresian NE parts extend into the Pannonian 8asin, while the south partly tation occurred in the Pannonian Basin. Jelar breccia of unknown age (Oligoeene and younger) and by to Lutetian) c1ast-supported breccias and limestones with larger borders the Adriatic Sea. Isolated Cenozoic sediments crop out the Promina beds. planktonic foraminifers. all across the region. Sedimentary rocks prevail, but eruptive Pa/aeogene the Outer Dinarides Towards the mainland, in the Lika region, Palaeogene outcrops The Kozina-type limestones were deposited in more-or-Iess masses of dacite-andesite rocks occur in east Bosnia. Ouring the 0/ In this zone, the Palaeogene rocks are found around Bihac, in are rare. The largest occurrence of Eocene limestones and deep- brackish, protected lagoons and bays during the Middle Cuisian Palaeogene, shallow-marine carbonates were dominant. They Dinara, and between Livno, Mostar and Trebinje. Palaeocene marine sediments is located at Bunic village (teetonic window (SBZ 11), which were partly alfected by severe subaereal exposure occur in two separate regions: in thc Herzegovina area (Outer sediments are restricted to the syncline core of Cardak Livada, in after Herak 1986). Studies on alveolinids showaMiddie to Late causing karstification. They comprise discorbidal limestones, Dinarides) to the south and in Bosnia to the north. The Inner the Votorog Mountains (Papes 1985), They are up to 400 m Cuisian age (SBZII and SBZI2; Drobne & Trutin 1997). miliolid limestones, stromatolites and breccias. Oiscorbidal lime- Dinarides (Bosnia) are composed of deeply weathered c!astic, thick, contain characteristie Palaeocene foraminifers and algae, Lacustrine sediments of Miocene age are fouod in the north stones and stromatolites predominate in Hvar, while miliolid metasedimentary, metamorphie and igneous rocks. They included and are composed of breccias, marls, conglomerates and thick. Adriatic region (Pag islanel, Krbavsko polje; lurisie-PolSak 1979; limestones are prominent on the Peljesac Peninsula. rnostly Palaeozoie- Triassie rocks and the Dinaride Ophiolite bedded calcirudites, Jurisie-Polsak et al. 1993). Thc Kozina-type limestones were transgressively overlain by Zone, The South Pannonian Basin (SPB) covers the Tuzla area Palaeocene-Eocene carbonates of the 50-300 m thick Libur- low-energy, open-shelf foraminiferal lirnestones. Their age ranges (north Bosnia), while the Pannonian Basin sensu lato covers a nian Formation (= Liburnian Limestone; Cicic 1977) occur in Northern Dalmatia. The area of Ravni kotari in north Dalmatia from Middle to Late Cuisian (SBZ 11-12) in the central large area at the southem margin of the Posavina area. the vicinity of Bihac, between Livno and Mostar, and from (AdCP and Dinaric thrust front) eomprises Mesozoie platform Dalmatian coastal region (Drobne 1985; Hottinger & Drobne Stolac and Capljina up to Trebinje. They are dark grey to black carbonates transgressively overlain by Eocene foraminiferal lime- 1980), from early Middle Lutetian (SBZI4) to early Late Palaeogeography and tee tonic setting eoloured beds. Locally, basal breccia limestones and ca1carenites stones (Middle Cuisian to Middle Lutetian, SBZIO-SBZI4; Lutetian (SBZ 16) in the central Dalmatian islands, and from The evolution of the region is related to the Palaeogene Eo- oceur, while the upper levels are characterized by marly and Drobne et al. 199Ic), Their contact is marked by breccias and Early Lutetian (SBZ 13) to Late LutetianiBartonian (SBZ 17) in Alpine, Pyrenean and Sava orogenie phases, and subsequent platy, compact limestones. They diseordantly overlie Senonian locally by bauxite accumulations (Markovic 2002). They are south Dalmatia. Massive Nummulite-Orthophragmina lime- Neogene neotectonic phases. Marine sedimentation prevailed rudist limestones, separated by a bauxite unit. overlain by Transitional Beds, which are overlain by e. 850 m of stones indicate deposition in a quiet, well-aerated subtidal until the earliest Oligocene in the Inner and Outer Dinarides, and 1112 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE lU3

Early and Middle Eocene sediments appear in Dinara, in the marls, with subordinate conglomerates and limestones. Marly section summarizes the most important papers (Katzer 1918; Pannon;an Basin sensu lato vicinity of Duvno and Lip Mountain, as weil as in the area of sandstones, sandy limestones and limestones prevail at the top of Soklic 1955, 1959, 1964, 1977, 1982, 2001; Stevanovic & Mostar and further towards the east. Sediments in the area of the succession. Tbe macrofauna was studied by Oppenheim Eremija 1960, 1977; Cieic 1977, 2002b; Cieie & Papes 1970; The Pannonian Basin sensu /ato covers a large area in north Duvno and Lip Mountain comprise c. 400 m of thick deep- (1908), Katzer (1918) and CiCic (1964). Cieie & Milojevie 1975; Cieie & Jovanovie 1987; CiCic et af. Bosnia, between the rivers Una in the NW and Drina in the SE. marine sediments with targer planktonic foraminifers (Papes Between the rivers Una and Vrbas, in the crest of Kozara and 1988; Cieic & RedZepovie 2003; Vrabac 1989, 1991, 1999; The Late Miocene 10 Pontian period contains 200-300 m of 1985). At other loealities, 100-600 m thick alveolinid-nummuli- surrounding terrains, the so-called Kozara Flysch occurs. Palyno- Ferhatbegovie 2004). brackish and limnic sediments rich in molluscs. The c. 100 m lid limestones of the same age overlie the Libumian Formation. logical data (Cieie 1977) suggests an age of Early to Middle Hydrocarbon exploration between 1934-50 provided data on thick Pannonian sediments of the Sarmatian Sea comprise Both of these successions are fallod in narrow zones related to Eocene. It is composed of arkose and subarkose sandstones, as the pre-Neogene basement of the Tuzla Basin. This consists of: molluscs and ostracods. Sediments (170 m thick) of the brackish reverse faulting and block overthrusting. weil as quartz-mica siltstones aod rare conglomerates. (1) Upper Cretaceous clastics and carbonates; (2) Maastrichtian- Sarmatian Sea show a characteristie succession: reefal olithic and Middle and Late Eocene sediments of Herzegovina can be The Majevica Mountains comprise a 100 m thick Middle Palaeocene-Lower Eocene deep-marine deposits; (3) Middle sandy limestones, sandy marls, clayish marls with molluscs, separated into two distinct successions: (1) marls, conglomerates, Eocene series of deep-marine sandstooes, marls and limestones, Eocene with foraminifers, molluscs and corals; and (4) Upper foraminifers and ostracods (Soklic 1977, 2001). Further proven sandy stones, days, slates, breccia limestones and limestones; which are overlain by marls that include a mixed marine and Eocene quartz sandstones and marls. Early Miocene sediments ages are Early Miocene-Ottnangian (sandstones and marls), and (2) limestone breccias, marls and sandstones with a thickness freshwater fauna (Cieie 1964), as well as slates and sandstones comprise the Slavinovici limestones, the Red and Mottled suites, Karpatian (marls and sandstones with Globigerinid foraminifers) of 100-600 m and mainly deep-marine. Sediments of the first with limestone beds. The thickness of this succession in north and the SaU Formation. They are Aquitanian and Burdigalian in and Badenian (sandstones and marls with foraminifers, molluscs type are known from lar&e areas on both sides of the Neretva Majevica is up to 200 m. Coal seams in these sediments are of age (i.e. Late Egerian, Eggenburgian, Ottnangian and Karpatian). and reefallimestones; Soklic 2001). river, from PosuSje and Citluk to Dabrica, and in the area of loeal economic importance. The 60 m thick SlavinoviCi Limestone is characterized by Lukavieko. They discordantly overlie the Libumian Formation. During the Middle and Late Eocene, the Majevica and Trebovac desiccation cracks of dry lake-mud and the oecurrence of fresh- Bauxite deposits of significant economical importance occur in mountains comprise aseries of 400-1200 m thick flysch-like water gastropods. It is overlain by the Red suite, composed of Summary the areas of Posusje and Dabrice. Mollusc lumacheJles containing sediments (Cieie 2002b). The lower parts are composed of redeposited tropical soils, derived from the peneplanated Dinar- Geologically, the Cenozoic represents the period when Africa larger foraminifera are also found (Cieie 1977). Sediments of the sandstones and alevrolite, the middle parts comprise siltstones, ides. Silty sediments with secondary conglomerates with chert, and Europe were converging, with seafloor spreading taking second type are typically developed around Posusje, Tribistovo marls, slates and rare limestones. The upper parts are character- peridotite and other silicate pebbles. The overlying Mottled suite, place in the Atlantic only as far north as the Labrador Sea and Konjovac. Tbey discordantly overlie alveolitid-nummulitid ized by thick-bedded marls, slates and sandstones, loeally with genetically related to renewed tectonic activity, was derived from (between Greenland and North America). Additionally, numerous limestones and bauxites, and contain a rich mollusc, coral and conglomerate lenses. Sediments from the Vucjak and Trebovac the same source area. In addition to ophiolite rocks, pebbles of micropiates in the Mediterranean area were compressed as a echinid fauna. The succession is up to 200 m thick and consid- mountains comprise thick-bedded sandstones, siltstones, eon- Tithonian- Valanginian limestones also occur. Volcanic activity direet result of Africa-Europe convergenee, gradually fusing ered as being coeval with the first succession. glomerates and slates with larger foraminifera, pollen and spores in the adjacent Podrinje area caused the occurrence of ash layers. together. This resu!ted in a shift in the palaeogeography of Eocene-Oligocene units comprise conglomerates, calcarenites suggesting a continuous succession from the Late Eocene to the Sediments of the Mottled suite are rich in fossils, particularly Europe from a marine archipelago to more continental environ- and marls. According to their typical development in the Oligocene (Ercegovac & Cieic 1968; Cieie 1977). gastropods. Pelite sediments of the suite are irregularly reddish, ments; this change was also related to the rising Alpidic Promina Mountains (Dalmatia) they are called the Promina Beds greenish and flaky, which is characteristic of muds ftooded by mountain chains. Around the Eocene-Oligocene boundary, Afri- (see above). They lie discordanlly on Late Cretaceous and early Miocene jreshwater basins alluvial fans. In the area of Soline, both the Red and Mottled ca 's movement and subduction beneath the European plate led to Palaeogene sediments and are interpreted as terrestrial. The age A large number of lakes existed during the Miocene. which were suites are about 300 m thick. The c. 600 m thick SaU Formation the final disintegration of the ancient . In addition of the Promina Beds is assumed to be Late Eocene to Early initiated by tectonic movements during the Sava Phase. These was deposited within a marine lagoonal environment and shows to the emerging early Mediterranean Sea another relict of the Oligocene. Tbeir thickness decreases from Livno (1300 m), created depressions, in which swamps and lakes formed due to a distinct cyclicity. The cycles begin with banded marls, followed closure of the Tethys was the vast Eurasian Paratethys Sea. At towards Posusje and Tihaljina (900 m), and to Nevesinje and thechange from an arid to a humid climate. Milojevic (1964) by anhydrite and tinally salt (halite and tenardite). Occasional the beginning of the Cenozoic, mammals replaced reptiles as the Gacko (200-600 m). separated the lacustrine basins of Bosnia and Herzegovina into volcanic ash layers can be up to 14 m thick. The Salt Formation dominant vertebrates. three regions: (I) north Bosnian region (Ugljevik, Mezgraja- is exploited at Tusanj (Tuzla town). Central Europe is composed of two tectonically contrasting Pa/aeogene 0/ the Inner Dinarides Tobut, Priboj, Pmjavor, Ljeiljani, Banovici, Durdevik, Seona and The overlying Karpatian sediments (>300 m thick) were regions, namely a northern Variscan, and a southem Alpine Various types of igneous rocks are known from the Dinarides Jasenica basins); (2) middle Bosnian region (Miljevina-Rogatica, deposited after a marine transgression from the Pannonian Basin Europe. The European Plate, a broad area of epicontinental (Katzer 1926; Varieak 1966; Pamie 1996). In Motajica, granites Sarajevsko-Zenieki, Zepacki, Teslic, Kotor Varos, Banja Luka (Central Paratethys). In the Ravna Tresnja-I well near Tuzla, sedimentation, essentially represented- the stable European con- create the central part of the mountain. Six types of granite can and Kamengrad basin); and (3) Outer Dinarides (Gacko, Mostar, rocks of the Mottled suite comprise coarse-grained marine tinent during the Cenozoic. The area, extending from the Atlantic be recognized: (I) massive, medium-grain-sized normal granite; Livno, Duvno and Cazin basins). conglomerates with intercalations of c1ayey and slightly bitumi- shelves of Norway and the Shetland Is1ands through to eastem (2) fine-grained granite with 'frozen edges'; (3) leucocratic The largest laeustrine basins of Bosnia and Herzegovina were nous marls. Poland and beyond, was separated from the Alpine-Carpathian granite; (4) greisenized; (5) aplicoide; and (6) kaolinized gran- created within the main fault zones, e.g. Sarajevo-Zeniea Basin in Karpatian sediments are conformably overlain by deep-marine chain by the Alpine-Carpathian Foreland Basin (= Molasse ites. Isotopic analyses suggested a Cretaceous-Palaeogene age, Busovaca, Tuzla Basin in Spreca, Kamengrad Basin between the Badenian marls intercalated with fine-grained sandstones. The Basin) and its precursors as apart of the Palaeogene Tethys or although Palaeocene- Eocene metamorphosis of the sediment Grmee aod Sana fault, Mostar Basin in the zone of the Neretva marls contain foraminifers, pteropods and other molluscs, nauti- Oligocene-Miocene Paratethys. The region encompasses the cover suggests an Eocene-Oligocene age. Granite massifs also Fault. Terrestrial sediments filling these basins have thicknesses of lids and echinoids, while Late Badenian coarse-grained sedi- North Sea Basin, the Polish Lowlands, the Volhyno-Podolian form significant parts of the base of the Pannonian Basin e10se to 1000-4500 m. Sedimentation in the larger basins began during ments contain larger, thick-shelled, shallow-marine fossils. The Plate, the Upper Rhine Graben and the Helvetic units. To the the Sava River. the Egerian, but thc exact age is uDclear in many cases. In total thickness of the Badenian sediments is about 500 m (e.g. south lay the Alps, a chain of mountains wh ich formed du ring Carbonate sediments dominate during Palaeocene to Early Ugljevik and other lacustrine basins of north Bosnia, the lacus- deep-well Bukinje). They are covered by up to 300 m of the multiphase Alpine Orogeny (see Froitzheim et af. 2008), and Eocene times. They are known from the broad area of Doboj and trine regime lasted until the Karpatian marine ingression from the Sarmatian brackish-water sediments comprising marls interca- whieh can be traced eastwards into the Carpathians; this latter Tesanj, Derventa as welt as in the areas of Trebovac and Pannonian Sea. In other basins, lacustrine sedimentation contin- lated with sandstones and conglomerates. In contrast to the area is very different from the Alps mainly due to the presence Majevica (Stojeie 1968). The microfauna ofthis 50-200 m thick ued until the Pontian. In addition to eoal seams, these basins Badenian marine fauna, the brackish Sarmatian fauna comprises of broad Neogene basins and extensive acidic to ealc-alkaline succession comprises planktonic, benthic and larger foraminifera. contain marls, limestones, elays and eonglomerates, and indivi- a low species diversity but a large number of individuals. The volcanic activity. During the Palacoccne and Eocene, the Alpine [n NE Majevica, sediments of this age are characterized by a dual units offreshwater limestone can be more than 300 m thiek. Pannonian fossils are eharacteristic of brackish environments. system formed an archipelago. The North Alpine Foreland Basin 700-1500 m thick succession of slates, sandstones, marls and Palaeontological information on the lacustrine sediments is In the Kreka Basin, six cyclothems with coal seams were was part of the Alpine-Carpathian Foredeep, a west-east trend- limestones. Sections from Tavna and north Majevica suggest that sparse, but several biostratigraphie conclusions based mainly on deposited during the Pannonian. The cycles were caused by ing basin located in front of the prograding nappes of the Alpine these sediments are part of a continuous Maastrichtian to mammals can be drawn, (Laskarev 1925; Milojkovic 1929; regressions within the Pontian Sea, which resulted in sandy orogenie wedge. The Southem Alps, to the south of the Palaeogene deep-marine succession. Tbe succession was dated . Malez & Sliskovic 1964 Pamic-Sunarie 1977; Malez & Thenius sequences with increasing compositional maturity up-section. Periadriatic Lineament, represent the northern extension of the I by means of foraminifera and algae (e.g. Radoieic 1992). Over 1985). A palaeontological overview on Bosnia and Herzegovina These processes continued until the final tilling of the basin, after Adriatic Microplate (together with the Eastem Alps, i.e. Austro- large parts of north Bosnia, deep-marine sedimentation continues has been published by Soklie (2001). which freshwater swamps developed. Subsequently, these areas Alpine units). In Palaeogene times, they constituted the southem up into the Middle Eocene. The thickness of these sediments is were covered by swampy forests, which were predisposed to coal continuation of the Eastern Alps archipelago. highly variable, ranging from 550 m (Kozara) to 1100 m (Maje- generation. The accumulation of lignite and cellulose continued The Cenozoic history 'of Central Europe is chronicled in a The Tuz/a Basin vica, Trebovac). until the following marine ingression, which occurred as a result series of Palaeogene and Neogene basins present across the On Majevica and Trebovac, the lower part of these units is The Tuzla Basin is part of the South Pannonian Basin, which is of sudden subsidence or, alternatively, of penetration of thc region. In addition to the more stable North Sea Basin, the charaeterized by an alternating series of sandstones, slates and situated to the north of the Dinarides mountain chain. This baITierseparating the basin from the Pontian Sea. majority of these basins were strongly inftuenced by compressive 1114 M. W. RASSER, M. HARZHAUSER Er AL. PALAEOGENE AND NEOGENE lII5

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