GEOL. CROAT. 52/1 83 - 98 4 Figs. ZAGREB 1999

Tectonic Interrelation of the Dinarides and the Southern Alps

Milan HERAK

Key words: Alps, Dinarides, Tisia, Slovenian Trough, KljuËne rijeËi: Alpe, Dinaridi, Tisia, Slovenski jarek, Sava Nappe, Pannonian Nappe, Mid-Transdanubian Savska navlaka, Panonska navlaka, Srednja transda- Zone, Bosnian Zone, Tectogenesis and geotectonic nubijska zona, Bosanska zona, tektogeneza i tekto- classification. genetska klasifikacija.

Abstract Saæetak The study focuses on northwestern Croatia which, including the Glavna je pozornost posveÊena sjeverozapadnoj Hrvatskoj, koja Æumberak (ÆumberaËka gora), Medvednica (ZagrebaËka Gora), ukljuËuje ÆumberaËku goru, Medvednicu, Kalnik, IvanπËicu i Ravnu Kalnik, IvanπËica, and Ravna Gora mountains, make a cross area of goru - presjeciπte susjednih slovenskih “Savskih bora”, Juænih Alpa, the Slovenian “Sava Folds”, Southern Alps, Mid-Transdanubian Srednje transdanubijske zone, Tisije i Unutarnjih Dinarida. To je Zone, Tisia, and the Inner Dinarides. This is a complex structural sloæeno strukturno podruËje, pa ne moæe biti pribrojeno samo jednoj region and cannot be attributed merely to one of the units. Therefore, jedinici. Zbog toga se predlaæe geotektonska interpretacija koja a geotectonic interpretation is proposed which respects the diversifi- uvaæava diverzifikaciju i viπestruku superpoziciju bazenskih i plat- cation and multiple superposition of basinal and platform elements. formskih elemenata. Ovaj koncept omoguÊuje povezivanje Sloven- This concept allows linkage of the Slovenian Trough with the Bosn- skog jarka s Bosanskom zonom i njezinim jugoistoËnim produæenjem ian Zone and its southeastern prolongation as a major coherent tec- u jednu koherentnu tektonsku megajedinicu na kojoj leæe razliËiti tonic unit overlain by different nappe elements. The possible linkage navlaËni elementi. Takoer se raspravlja o moguÊoj vezi s Budva- with the Budva Zone beneath the carbonate nappe is also discussed. zonom.

1. INTRODUCTION attributed to the “Oriental Land”. SALOPEK (1914), analysing modern tectonic concepts, concluded that The structural relationships of northwestern Croatia autochthonous relationships characterize NW Croatia. and the adjacent regions of Slovenia and Bosnia were CVIJI∆ (1924) accepted the idea of the ancient land (he and remain subject to different treatment. The main called it the Rhodopian Mass) but considered its bound- approaches are as follows: aries as ambiguous. Therefore, he proposed to distin- PETERS (1863) assumed the existence of an anci- guish transitional zones between the “Land” and its sur- ent “Palaeolithic Land” within the Balkan Peninsula, roundings. KOCH (1924) gave preference to the Dinar- comprising the “crystalline cores of Slavonia and Sie- idic elements in the whole area, and included even the benburgen”. This megastructure was not supposed to Slavonian Mountains into the Dinarides. WINKLER have participated in tangential Alpine tectonics. SUESS (1924) believed in north-vergent allochthony in the (1875) attributed northwestern Croatia (including Mt. adjacent area of the Slovenian “Sava Folds”, probably Medvednica) to the Southern Alps, while DIENER under the influence of Suess’s concept of a northward (1903) regarded the area as part of the Eastern Alps. push of the Southern Alps. MOJSISOVICS (1880) accepted the “Land” defined by In recent times, MIO» (1975, 1981) paid special PETERS and introduced the name “Oriental Land”. attention to the “Sava Folds” and to the area of the However, he experienced difficulty in defining its Lower Carniolia (Dolenjska, eastern Slovenia). He defi- boundaries. PILAR (1882) was involved with the geol- ned a unit named the Sava Nappe which overlies the ogy of western Bosnia and concluded that the “flysch”, Outer Dinarides, and is overlain by a south-vergent containing “eruptive rocks” (including ophiolites), con- nappe composed of elements of the Julian and Savinja tinued into Croatia. Later, KI©PATI∆ (1899), studying Alps. The extension of such relationships should be fol- ophiolites, accepted the opinion that Mt. Medvednica lowed towards Mt. Æumberak (comprising the area of was a continuation of northern Bosnia (i.e., of the Inner Samobor). PREMRU et al. (1977), by means of some Dinarides), as did also GORJANOVI∆-KRAMBER- deep boreholes, established a well-marked allochthony GER (1907), with the exception of the part which was in Lower Carniola (Dolenjska) and in the adjacent Mt. Æumberak. They considered the area as a part of the Croatian Academy of Sciences and Arts, A. KovaËiÊa 5/II, HR-10000 Outer Dinarides. The “Litija anticline” was defined as Zagreb, Croatia. the Dolsko overthrust (PREMRU, 1983, and earlier). 84 Geologia Croatica 52/1

The same unit has been subdivided in detail by MLA- formed during the Triassic, while in the Æumberak area KAR (1987). ©IKI∆ et al. (1978, 1979), ©IMUNI∆ this occurred no earlier than the end of the Lower Juras- (1992), ©IMUNI∆ & HE∆IMOVI∆ (1979), etc., intro- sic. In contrast, DIMITRIJEVI∆ (1982) accepted the duced short distance overthrusting with different ver- existence of a homogenous zone extending from the gences to explain the tectonic pattern of Mt. Æumberak Julian Alps, over the “Sava Folds” and “Zagreb Zone” (with the area of Samobor) and Mt. Medvednica as well (i.e., Mid-Transdanubian Zone in the current terminolo- as of Hrvatsko Zagorje. They contributed new data to gy), but he placed a sharp boundary towards the Dinar- previous interpretations. MILADINOVI∆ (1981) argu- ides (inclusive of the Vardar Zone, s . l .). Though aware ed for the existence of an extensive allochthonous unit, of great differences within the area of the so-called called the Pannonian Nappe. The idea was born in 1974 Inner Dinarides, I preferred to attribute the area in ques- (see: MILADINOVI∆, 1981) on the basis of the study tion to a common Inner Dinaric megaunit (S u p r a d i n a r - of many published papers and with insight from the i c u m) with possible interior differentiation (HERAK, geologic mapping data. The maps have been made by 1986, 1991, 1995, 1997). For example, the structures numerous authors who registered several inverse con- consisting of Late Palaeozoic and Triassic rocks were tacts but did not evaluate them in a geotectonic sense. considered as overthrusting parts of the bottom margin MILADINOVI∆ has drawn his tectonic map in 1977 of the Inner Dinarides. More recent explanation of the and elaborated in 1981. The nappe concerns only Upper origin of this nappe requires emendation as discussed Palaeozoic and Triassic rocks, which overlie Creta- later. PAMI∆ (1993) was concerned with Eoalpine and ceous and Jurassic formations. The Nappe should cover Neoalpine magmatic and metamorphic processes in the a broad region stretching from Italy through the Julian northwestern Vardar Zone, the easternmost Periadriatic Alps, South Karavanke and Savinja Alps, to the “Sava Zone and the southwestern Pannonian Basin. He was of Folds”, Mt. Æumberak, Banovina, North Bosnia, Uæice, the opinion that the mountains of Hrvatsko Zagorje Prizren, Pljevlja, “Pelagonian Massif”, etc. Within this “can be interpreted as relics of the Sava and/or Julian - megaunit, several tectonic windows and klippen were Savinja nappes”. He proposed to introduce more Dinar- identified, which include the “Zlatibor” window. Since idic elements when treating southern marginal parts of the most characteristic areas lie outside the Pannonian the Pannonian Basin. The participation of Dinaridic ele- Depression, the name of the assumed nappe has not ments in the Mid-Transdanubian Zone was also ackno- been generally accepted. Likewise, there are some regi- wledged by BERCZI-MAKK et al. (1993). Authors ons that cannot be included into such a simple model of from the Institute of Geology in Zagreb use the term this unit, especially the composite structure called the Mid-Transdanubian Tectonic Zone, which is not delim- “Pelagonian Massif”. As to the Western Dinarides, the ited towards the Inner Dinarides (©IKI∆, 1995), as did idea itself may be generally acceptable. However, the many other authors, e.g. HAAS et al. (1995). However, details require refinement. by some authors sharp tectonic limits towards the The possible connection of the Slovenian Trough Dinarides were assumed (e.g., DIMITRIJEVI∆, 1982). with the Bosnian Zone has been registered in several There are many more papers with controversial con- papers. In Mt. Æumberak, TORNQUIST (1918) deter- cepts, but all of them are within the frame of these ideas mined pelagic sediments of Late Tithonian, Berriasian and, therefore special commentary of them is omitted. and Valanginian age. He considered them as a link bet- By comparison of the proven data in NW Croatia ween analogous Slovenian and Bosnian deposits. and eastern Slovenia, the heterogeneity of the region AUBOUIN et al. (1970), COUSIN (1973), and BABI∆ (called the Mid-Transdanubian Zone) is obvious, with (1973, 1974) were concerned with the same problem, the consequence that Dinaridic and Alpine elements are speaking in favour of such a connection. AUBOUIN et superimposed. However, the tectogenetic processes and al. (1970) assumed the existence of a “Furrow”, in the interior organisation remain under discussion. which specific (“basinal”) formations have been depo- Despite the fact that within northwestern Croatia sited since the Late Triassic. However, they do not numerous new data, concerning lithostratigraphy and explain the type of boundary between this “Furrow” local tectonics, have been collected (©IMUNI∆ & and the oceanic realm of the Inner Dinarides, which is PAMI∆, 1989; HERAK et al., 1990; ©IMUNI∆, 1992; characterized by ophiolites and is visible in their recon- ©IKI∆, 1995; HALAMI∆ & GORI»AN, 1995, etc.), a struction of the major structures where they propose a general comparative treatment concerning Dinaridic- direct overthrust of the ophiolitic complex upon the ele- Alpine geotectonic relations remains elusive. Therefore, ments of the “Furrow”. the major aim of this paper is to rectify that problem. Later, BABI∆ & ZUPANI» (1978) again evaluated the analogies between the Julian Alps and the Dinarides and contributed some additional elements in favour of a 2. MAJOR LITHOSTRATIGRAPHIC direct connection. However, they also called attention SEQUENCES to some difficulties. For instance, between the Tolmin - Selπka Sora area and the Æumberak area, differences Mt. Medvednica (ZagrebaËka Gora) and Mt. Æum- exist in the timing of their aquisition of basinal charac- berak (ÆumberaËka Gora) display the greatest diversity ter. In the Tolmin - Selπka Sora region, the basin may be of lithostratigraphic units. In a relatively small space Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 85

Fig. 1 Diversification of Mesozoic events in the adjacent are- as of the Dinarides and the Southern Alps: U) Upper- most platform dep- osits; S) Supradi- naric oceanic roc- ks; D) Dinaric pla- tform deposits; E) Epiadriatic pelagic deposits and for- mations with pela- gic components.

there are numerous inverse tectonic contacts indicating In this paper, only the most pertinent ones will be taken piling up of various lithocomplexes that require palin- into account. spastic reconstruction of the primary environments. Generally, several primarily consistent lithostrati- Compiled stratigraphic data on Mt. Medvednica graphic successions, characterized by features indicat- (©IKI∆, 1995) include units ranging in age from the ing complementary palaeogeographic and tectonic div- Palaeozoic to the Quaternary. Since the main purpose ersification in space and time (Figs. 1-4), can be distin- of this paper is the reconstruction of palaeotectonic guished in the Alpino-Dinaridic realm, though these are relationships, the discussion of Neogene and Quater- dispersed at the surface. nary deposits is omitted. As there is a high degree of stratigraphic diversifica- 2.1. VARISCAN BASINAL FORMATIONS tion, the origin of different stratigraphic complexes can- not be explained by means of lateral facies within sin- The Palaeozoic, from the Silurian to the Middle gle consistent depositional areas. Usable data have been Carboniferous, displays prevailingly basinal type of published in numerous papers cited by ©IKI∆ (1995). carbonate and clastic sediments. They are exposed in 86 Geologia Croatica 52/1

Fig. 2 Proposal of an emended and generalized map of the Dinaridic - South Alpine joint realm for further considerations; subductional tectonic model, based on selected outcrop-areas with simplified and partially enlarged contours: 1) Neogene and Quaternary cover; 2) Austroalpine; 3) Tisia; 4) Uppermost Nappe (with some tectonic windows); 5) Supradinaricum (s. str.); 6) Dinaricum; 7) Epiadriaticum (pelagic deposits and clastics with pelagic components); 8) Adriaticum; 9) ? Ionian underthrust; K) Mt. Kalnik (see Fig. 3); M) Mt. Medvednica (see Fig. 3); Æ) Mt. Æumberak with the Samobor area (see Fig. 4); Iv) Mt. IvanπËica.

Mt. Medvednica (–UR–ANOVI∆, 1973; SREMAC & sedimentary conditions. However, in Trgovska Gora W MIHAJLOVI∆-PAVLOVI∆, 1983). Some outcrops are of the Una River, SE of Zagreb, only non-metamorphic slightly metamorphosed with relatively well-preserved outcrops of the Devonian and the Carboniferous with graptolites, conodonts, etc. Even in cases when they are conodonts are present (–UR–ANOVI∆, 1973) what included into the younger metamorphic complex, it is indicates that they do not belong to the same tectonic possible to use them as evidence of primary basinal unit. The change from basinal type of sedimentation in Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 87 the Middle Carboniferous is due to the Variscan oroge- and some dolomites (in the upper part of the limestones ny which formed the structural basis for later molasse ammonites are preserved). The general tendency of sediments. However, Variscan megastructures (with so- subsidence is obvious. me older tectonic elements) are preserved only in the The Middle Triassic was a time of relative tectonic adjacent Slavonian Mountains belonging to the Tisia disquiet, especially in the Anisian. Some rifting with (JAMI»I∆, 1983; HERAK et al., 1990). volcanism (mostly several types of basalts) and clastic Palaeozoic fragments (together with Triassic exam- sedimentation occurred. However, generally dolomites ples) are poorly preserved as protoliths of the younger and dolomitized limestones prevail, continuing also into metamorphics (greenschists and associated schist mem- the Ladinian. At several horizons of the Middle Trias- bers). This rock complex with changed mineral compo- sic, small areas of ammonitic limestones have been fou- sition originated during the process of progressive low- nd. The tectonic dynamics in the Middle Triassic was grade metamorphism (BELAK et al., 1995a, b). There- tardy-Variscan (final), forming the basis for the origin fore, it may be treated as a consequence of the Alpine of later carbonate platform areas. tectonic deformations and metamorphism. In the Upper Triassic, stromatolitic dolomites and some limestones with megalodontids predominate. Car- 2.2. VARISCAN MOLASSE DEPOSITS bonate sedimentation lasted until the Palaeogene with some oscillations indicated by shallow water clastics The Late Palaeozoic is represented by Carbonifer- and small gaps (CRNJAKOVI∆, 1981). ous deposits with corals as well as clastics, which con- tain the remains of land plants (Banovina, SE of Zag- 2.4. MESOZOIC DEPOSITS WITH reb). Various plant fragments are also found in Mt. PELAGIC INFLUENCES Medvednica and Mt. Æumberak. The molasse deposists in the region of Samobor are The outcrops of Late Triassic pelagic deposits are most characteristic. They consist of Permian (possibly encircled either by platform or by oceanic facies from also of some Carboniferous) clastics composed of qua- which they can be distinguished: from the platform for- rtz conglomerates, lithoclastic graywackes, siltites, sha- mations by the type of sediments (platy limestones, les, and sporadic dolomites. The terrestrial origin of the radiolarites, etc.), and from the oceanic formations by a clastic components is further proven by the remains of lack of a magmatic-sedimentary complex with ultra- land plants Calamites and Sigillaria (JENKO, 1944). mafics and mafic intrusives. On the NW side they out- Evaporites were deposited in the transition time crop in the Slovenian Trough (GRAD, 1961; COUSIN, between the Permian and the Early Triassic. They are 1973; LAPAJNE & ©RIBAR, 1973; PREMRU, 1975, followed continuously by variegated clastics, what may 1983; BUSER, 1977, 1989; BABI∆ & ZUPANI», be decisive in the interpretation of the Uppermost 1978; BABI∆, 1980/81; JURKOV©EK et al., 1990, Nappe (Fig. 2, U), unifying Palaeozoic and Triassic etc.). Towards the E and SE they are present at many deposits as an integral unit which overlies oceanic for- isolated sites. mations of the Inner Dinarides. In recent times, very important dispersed pelagic Some isolated platform outcrops are “strange” with- outcrops have been described on the northern slope of in Variscan molasse deposits. Possibly they can derive Mt. Medvednica and on Mt. Kalnik (Fig. 3), and then from the subducted (?) Dinaric platform. In an Eocene on Mt. Æumberak (Fig. 4). breccia in Hrvatsko Zagorje (Vinica and Viπnjica W of At the localities of Mt. Kalnik the metabasalts, Varaædin), MILANOVI∆ (1982) found Middle Car- shales and radiolarites outcrop. Primary contacts with boniferous limestone fragments with foraminifera and the surrounding facies are not clearly visible. Locally, calcareous algae. He correlated them with analogous the outcrops are composed of heavily tectonized rocks. deposits in Mt. Velebit, Banovina, etc. In the area The lower part of the succession is composed of calcit- northwest of Samobor (near the Bregana Village), in a ized, porphyritic, ophitic metabasalts. The age of the small isolated carbonate area, calcareous algae (Gymno - radiolarites corresponds to the Carnian-Norian time c o d i u m, A t r a c t y l i o p s i s, etc.) have been determined interval (HALAMI∆ & GORI»AN, 1995). (HERAK & ©KALEC, 1967). In Mt. Medvednica a On the northwest slope of Mt. Medvednica radiolar- boulder has been found which contains remains of ian cherts alternate with silty shales. The sediments are N e o s c h w a g e r i n a ( D E V I D É - N E DE˘ LA & KOCHAN- intensely folded, partially even overturned. Their base SKY-DEVIDÉ, 1990). ©IMUNI∆ (1979) registered is not known due to intensive tectonics, and they are Lower Permian algae in a non-metamorphosed lime- non-conformably overlain by Palaeocene calcitic silt- stone in Mt. Medvednica. stones. However, it is probable that the examined Trias- sic radiolarites are partially overlain by similar silty 2.3. TARDY-VARISCAN DYNAMICS AND siliceous sediments (radiolarian cherts, shales, etc.) of THE ORIGIN OF CARBONATE PLATFORMS uncertain Jurassic age (HALAMI∆ & GORI»AN, 1995, p. 135). The main Lower Triassic components include: sand- In the adjacent area of Mt. Hum, NW of Mt. Med- stones, siltites, marly limestones, oolitic limestones, vednica (valley of Burnjak), limestones with intercala- 88 Geologia Croatica 52/1

Fig. 3 Simplified main tectonic units in the mountains Medvednica and Kalnik; basic data from ©IKI∆ (1995) and ©IMUNI∆ (pers. comm.), reinterpreted: 1) Uppermost Nappe; 2) S u p r a d i n a r i c u m (with possible small Dinaric outcrops) disturbed by strong interior tectonism; 3) pelagic deposits and formations with pelagic influences (interpreted as Epiadriaticum); 4) Neogene and Quaternary cover; 5) place of graph- ical shortening of the terrain.

tions and lenses of chert outcrop (©IKI∆, 1995). Dis- tonic unit as the Triassic which constitutes the overly- continuous fragments of pelagic outcrops, belonging to ing nappe. the transition between the Upper Triassic and the Lias Some other Lower Cretaceous outcrops also indi- are also present, as well as pelagic limestones with radi- cate basinal sedimentation (with pelagic influences). olarians and lagenid foraminifera of Late Lias - Dogger Such is the “Oπtrc formation” in Mt. IvanπËica descri- age. Some isolated outcrops belong to the Jurassic-Neo- bed by ZUPANI» et al. (1981). It overlies the afore comian, others to the Tithonian-Berriasian, with a pos- mentioned Tithonian-Valanginian pelagic deposits. The sible “hard ground” at the contact with Triassic dolomi- formation consists of calcarenites, sandstones, marly tes (BABI∆ & ZUPANI», 1973; BABI∆, 1975; ©IKI∆, shale, and deposits with radiolaria and spicules. The 1995, p. 15). The incompleteness of the columns is calcarenites frequently show silicification and recrystal- ascribed to the condensed sedimentation. In Mt. Ivanπ- lization phenomena. The authors concluded that the Ëica, ZUPANI» et al. (1981), and ©IMUNI∆ (1992) part of the basin within the Mt. IvanπËica area originat- also emphasized that, due to the “hard ground”, Tithon- ed upon the continental crust. Analogous relationships ian-Valanginian deposits non-conformably overlie dif- also occur at Mt. Æumberak (BABI∆, 1974). Moreover, ferent stages of the Triassic. Explanation of such a phe- correlation is assumed with the Vranduk area in Bosnia nomenon in that way would anticipate intensive tecton- belonging to the Bosnian Zone (defined by AUBOUIN ics at the end of the Triassic with the consequence that et al., 1970), which displays essential differences in the lack of sedimentation would last until the Late Tith- sediments beginning with the Late Triassic, and contin- onian. Such a hiatus there has not been substantiated. uing during the Jurassic and Cretaceous. The Zone may Moreover, the origin of ophiolites, accompanied by be followed in Montenegro. In Western Serbia OBRA- younger magmatic-sedimentary rocks in the same area, DOVI∆ & VASI∆ (1996, p. 191) speak of “isolated argues in favour of intensive tectonics during the Juras- bedded series” with radiolarites of different ages within sic and the Early Cretaceous. Besides, the Triassic in various complexes. Analogous deposits outcrop even in question does not necessarily belong to the same tec- Albania, however not as a continuous zone but as local- Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 89

Fig. 4 Simplified tectonic map of the east- ern part of Mt. Æumberak (with the area of Samobor), supplemented by J. BUKOVAC: 1) Uppermost Nappe; 2) S u p r a d i n a r i c u m (with possible small Dinaric outcrops); 3) pelagic deposits and formations with pelagic influences (interpreted as E p i a d r i a t i c u m ); 4) Ne- ogene and Quaternary cover.

ized “strange” bodies within the Mirdita Zone. All this environment”. It is important to mention that on the suggests that these deposits with pelagic elements are northwestern slope of Mt. Medvednica a tectonically tectonically emplaced within heterogeneous areas. delimited, narrow Upper Triassic - Dogger limestone Similar heterogeneity has been found even in other zone, partially dolomitized and recrystallized, is present morphotectonic units like the North Karavanke Alps (©IKI∆, 1995). This means that, due to tectonic forces, (MIO» & ©RIBAR, 1975), and in the Outer Dinarides. two major environments have been brought close to one The latter were discussed by many authors (cited in another. This fact requires additional investigation, as HERAK, 1993). The age of dispersed pelagic deposits pointed out by ©IKI∆ (1995, p. 14). For our purpose, it within the Outer Dinarides range from the Triassic (out- seems acceptable that, in the area where the tectonic crops in the Budva Zone, and in the Slovenian Trough) dynamics later increased, the deepening within the Tri- to the Late Cretaceous, with a predominance of Upper assic-Liassic carbonate platform started not earlier than Jurassic outcrops. At the margin towards the Inner the end of the Lias. Consequently, the above mentio- Dinarides even Palaeogene outcrops occur. They all ned, tectonically delimited pelagic limestones with che- require a common provenance influenced by the same rt of Upper Triassic age (HALAMI∆ & GORI»AN, open sea environment. The lack of both intrusives and 1995; ©IKI∆, 1995) should be “strange” in the areas metamorphic rocks means that the distribution area of where they are outcropping. pelagic components was outside the active orogenic re- The oceanic opening made possible the uplift of alm. Therefore, their recent position can only be expla- ultramafic rocks. The isolated outcrops have been fou- ined by entangled tectonics, discussed later. nd in Mt. Medvednica and in Mt. Kalnik, secondarily emplaced into Cretaceous clastics. They are also pre- 2.5. OCEANIC MEGAENVIRONMENT sent in some deep bore-holes north-eastward of Mt. The origin of a belt with oceanic components started Medvednica (©IMUNI∆ & PAMI∆, 1989; ©IKI∆, within the area most often called the Inner Dinarides. 1995; PAMI∆, 1997). Furthermore, a magmatic-sedi- According to GU©I∆ & BABI∆ (1972, p. 336), the mentary complex originated, composed of clastics and lithology and fossil contents of the fragments in the magmatic rocks: gabbro, diabases, spilites, etc. (CRN- Senonian breccia in Mt. Medvednica “show that the KOVI∆, 1963). Norian-Rhaetian limestones had been deposited in a As to the origin of the adjacent Tisia, there are dif- very shallow sea, whereas the Liassic sediments had ferent opinions discussed in numerous papers (see: originated in a considerably deeper and quiet marine CLOETINGH et al., 1993). Later, SZEDERKENY 90 Geologia Croatica 52/1

(1996) is of the opinion that during the Jurassic (Bath- slow subduction and/or obduction. However, these eve- onian) the Tisia fragments were broken-off the southern nts are not the topic of this paper. margin of the Variscan Europe and after a complicated drifting, accompanied by rotation, came to their present tectonic position. In this case, the general platform area 3. TECTONIC EVOLUTION split into two branches. One is nowadays extended in AND CLASSIFICATION the Mid-Transdanubian Unit, Bükk Unit, etc., the other remained southward of the Tisia. However, general The recent general characteristic of the area under agreement does not yet exist. Anyhow, the oceanic for- discussion is intensive fragmentation of the previously mations were subducted northward under the platform described lithostratigraphic complexes. They have been elements, disintegrated them and, possibly, in a latter disturbed by continental (A) subduction, oceanic (B) phase even obducted upon the Slavonian part of the subduction, then by more or less vertical movements Tisia (in contrast, MATEJ et al., 1997, assume the sub- connected with gravitational displacements, and finally duction of Tisia). During the oceanic dynamics meta- by erosion. According to the presented lithostratigra- morphic rocks (greenschists, etc.) were formed (BEL- phy, the main events should be the following. AK et al., 1995a, b). Analogous rocks have been found Before the Late Triassic, the major events were at places outside of our area, e.g. anchizonal metamor- more or less uniform over the whole area, only display- phism has been described in Hungary in the Mid-Trans- ing interior differentiations, sometimes of a high deg- danubian Unit. BERCZI-MAKK et al. (1993, p. 280) ree, but not specific enough to be used as diagnostic accepts the opinion that it presumably belongs “to a features in recognizing single well defined megatecton- nappe unit of lower position” (i.e., to the S u p r a d i n a r - ic units. icum, s. str., as it will be treated in this paper). At the beginning of the Late Triassic, the new major Tectonic consolidation processes, approximately at differentiation started. According to the afore men- the beginning of the Turonian interrupted the tectonic tioned lithostratigraphic sequences and their position dynamics, responsible for the origin of the magmatic- between two carbonate complexes visible at many pla- sedimentary complex. The deposition was influenced ces, a labile (“miodynamic”) continental trough origi- not only from the open sea, but also from the near-shore nated, being connected with the open sea. It enabled the and land surfaces due to oscillation of basin bottom open sea to influence the platform areas. The first depth with changes of depositional environments, fol- deposits in this trough were Late Triassic pelagic sedi- lowed by subduction processes within the crust. All this ments (limestones, cherts, etc.). The longitudinal distri- changed the future sedimentation processes, which bution of their outcrops suggests an adequate (longitu- included conglomerates, sandstones, siltites, shales, dinal) common “furrow”. It remains to be seen if it was rudist bioherms, platy limestones with globotruncanids, within the carbonate platforms (HERAK, 1986, 1991, turbidites (with slope and bottom influences), etc. They 1995, 1997, etc.) or within the oceanic realm itself, at are either in superposition or represent only lateral the oceanic margin of the platform (AUBOUIN et al., facies. The true relationships are difficult to explain due 1970). The latter opinion was common before the mobi- listic concept was introduced. However, there are still to subsequent tectonic disturbances. many adherents (e.g., PAMI∆ et al., 1998). My concept is based on the fact that at several places the pelagic 2.6. PREDOMINANCE OF FLYSCH DEPOSITS deposits are emplaced between two carbonate platform From the Senonian the “continental” and “oceanic” units (Budva Zone, Una spring area, Slovenian Trough, troughs were not so well delimited being narrowed due etc.) which would be impossible if the “furrow” were to subduction and bottom uplift. The transgression upon adjacent to the oceanic realm. Initially, the deposition the adjacent land surfaces is often mentioned because was confined to the “furrow” itself, then the surfaces flysch elements also overlie different platform surfaces. widened upon the platform margins, lagoons and basins Despite the interfingering with other facies, the pre- of clastic deposition. dominance of the flysch in the time span from the Ma- After the Lias, within the northern (northeastern) astrichtian to the Palaeocene is evident (CRNJA- part of the platform a new deep oceanic trough was for- KOVI∆, 1981; DEVIDÉ-NEDE˘ LA et al., 1982; BUK- med, being characterized by “eudynamic” processes OVAC, 1988; MARIN»I∆ et al., 1995; ©IKI∆, 1995, during the Jurassic and a larger part of the Cretaceous. etc.). Later on, the events in all labile areas were characte- rized predominantly by clastic deposits not only within 2.7. FINAL TECTOGENETIC CONSEQUENCES the basins but also upon the adjacent platforms. According to the mentioned interrelationships, it is After the Palaeocene continental subduction proces- obvious that the reconstruction of single major tectonic ses caused piling up and squeezing of different tectonic zones is very difficult. However, this may be attempted, units, emplacement of granites, etc. Afterwards, uplift taking into account their composition and recent posi- occurred, followed by Oligocene and Neogene volcani- tion. It is possible to distinguish several homogenous sm, tilting, strike-slip faulting, rotation, and, possibly, nappe units. They will be differently named in order to Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 91 distinguish them from the morphotectonic entities (Out- exceeds the frame of the Vardar Zone as defined by er Dinarides, Inner Dinarides, Southern Alps, Mid- KOSSMAT (1924). The western extension of the S u p - Transdanubian Zone, etc.), which are usually heteroge- radinaricum is covered by the Uppermost Nappe. neous, composed of elements of two or more subducted (underthrusted) homogeneous units. As the names are a 3.3. THE DINARIC NAPPE (Dinaricum, D) question of convention, the possibility is open for new proposals if they can be supported by better reasons. At the southern (southwestern) side, the rocks of the Dinaric carbonate platform (Figs. 1 and 2, D) bordered 3.1. THE UPPERMOST NAPPE (U) the oceanic belt (S u p r a d i n a r i c u m , s. str.). As a major tectonic unit, it is called Dinaricum and it underlies the The overlying components of the region under dis- Supradinaric Nappe. Within the D i n a r i c u m s e v e r a l cussion (Figs. 1-4, U) form a nappe composed predomi- “strange” outcrops of pelagic deposits have been found. nantly of Triassic dolomites with some limestones, Their origin and tectonic position were repeatedly dis- accompanied by Lower Triassic clastics including well- cussed (citations in HERAK, 1993). In the contact area bedded limestones, as well as by Upper Palaeozoic of the S u p r a d i n a r i c u m and D i n a r i c u m, including the molasse deposits (which do not derive from the Inner marginal flysch (with some karstifications in the base- Dinarides). They are characterized by west-east, or ment), the nappe relations are obvious (PREMRU et al., southwest-northeast extension. The nappe is disintegra- 1977; HERAK, 1986; BUKOVAC, 1988). Consequent- ted and it comprises elements which have been descri- ly, “La sous-zone prékarstique” (BLANCHET et al., bed as the Pannonian Nappe (MILADINOVI∆, 1981, 1970) is also included into this megaunit. and earlier), as well as the Sava Nappe (MIO», 1981, Previously, the contact zone of the Dinaric platform and earlier), or the inverse basement of the Inner Dinar- and oceanic formations was treated as a “flexion” or ides (HERAK, 1991) as a part of the S u p r a d i n a r i c u m. “bending” zone, making a slope of the platform towards Recent additional data (©IKI∆, 1995) justify the tecton- the basinal complexes including magmatites. It was ic distinction of this Uppermost Nappe deriving outside supposed that this zone existed probably since the Tri- the Dinaric realm (s. str.), i.e., from the Southern Alpi- assic, representing “the Adriatic microplate toward the ne area, emplaced on the northern side of the Oceanic Tethys ocean” (DIMITRIJEVI∆, 1982, p. 11). Howev- Trough (S u p r a d i n a r i c u m, s. str.). This Nappe overlies er, it is obvious that this contact zone was created as a not only the oceanic S u p r a d i n a r i c u m , but also parts of consequence of two events. The first, was the opening Jurassic and Cretaceous carbonate rocks of the Dinaric of the ocean after the Lias (more or less vertical con- carbonate platform (D i n a r i c u m), mostly in the form of tacts). The second was continental subduction during klippen. The final emplacement may be at least partly the Palaeogene, when the Dinaric carbonate platform, caused by gravitation. together with the overlying marginal flysch, was sub- At this point, it is necessary to note that some Trias- ducted under the basinal “magmatic-sedimentary” com- sic and Palaeozoic deposits may not belong to the plex (S u p r a d i n a r i c u m) and even under the Uppermost Uppermost Nappe but to Dinaridic major units as their Nappe. The corresponding contacts are inclined. direct basement. Therefore, the utmost care is required The opposite margin of this megaunit, together with in interpretation of the tectonic position of different Tri- the underlying “strange” pelagic outcrops, are discussed assic and Palaeozoic outcrops. below.

3.2. THE SUPRADINARIC NAPPE 3.4. THE INTERPLATFORM MEGAUNIT (Supradinaricum, s. str., S) (Epiadriaticum, E)

This Nappe (Figs. 1-4, S) comprises the oceanic part The range of the isolated outcrops of pelagic and of the S u p r a d i n a r i c u m (s. l.), overlain by the Upper- basinal deposits without ultramafic and mafic intrusions most Nappe. The Nappe is characterized by formations range from the Upper Triassic to the Upper Cretaceous, originated as a consequence of “eudynamics” from the and are to be found as well in the Outer as in the Inner Lias to the Turonian. In the Senonian, differentiation Dinarides (Figs. 1-4, U). Their distribution is extremely increased under pelagic and terrestrial influences. difficult to explain in a generally acceptable way. The Simultaneous uplifts widened the influences of this continuous outcrops extend only in the Budva-Krasta- basin upon adjacent platform margins, in the form of Pindus Zone on the southeastern side and in the Sloven- extensions of flysch deposits (marginal flysch) which ian Trough on the northwestern side. Between these hide the boundaries between the basin and the plat- areas, numerous tectonically delimited outcrops may forms. Therefore, only flysch deposits, which are tec- indicate that their interconnection could be traced tonically connected with oceanic formations, belong to beneath the nappes mentioned earlier. In such a case this Nappe. The rest of it (the marginal epiplatform fly- even the Bosnian Zone (AUBOUIN et al., 1970) may sch) is to be treated together with the next tectonic be connected with the Budva-Krasta-Pindus Zone megaunit (D i n a r i c u m). The Vardar elements are also below the D i n a r i c u m due to continental subduction. included in the S u p r a d i n a r i c u m. However, their frame The indications of such a connection were noticed earli- 92 Geologia Croatica 52/1 er. MEDWENITSCH (1964, in SIKO©EK & MEDWE- basins are separated from the ocean by a platform, they NITSCH, 1965) distinguished the Subdinaricum which have to be partially open to the ocean (p. 313). Howev- should consist of Budva, Mirdita and Raduπa elements er, due to oscillations the deposition itself, character- together with the central ophiolites. Their extension is ized by pelagic fossils, occurred in various depressions, supposed to be beneath the carbonate Dinarides. In this i.e. even upon the platforms (in lagoons). The only con- way, typical Inner Dinaric elements (Mirdita, Raduπa, dition is in the interference with the open sea (in our central ophiolites), which normally overlie the Outer case the eastern Tethys). Dinarides, were connected with the Budva Zone which Consequently, the pelagic components had neither underlies them and now can be interpreted as a subduct- oceanic nor platform characteristics. Within the deriva- ed unit. On the contrary, PAMI∆ (1993, etc.), tried to tion trough itself the pelagic column seems to be more connect the Bosnian Zone with the Budva Zone (united or less complete. Upon both the adjacent marginal parts with the Mirdita Zone) upon the surface lithologic of the carbonate platforms the range and extension var- analogies. ied. The peripheral common boundary (at different However, the main problem, concerning all the horizons) has been characterized by the transition of pelagic outcrops, is that they are delimited to small pelagic deposits to carbonate shallow-water sediments. areas, which are dispersed and tectonically encircled Such exposures are, in a tectonical sense, part of the with deposits of different provenance, belonging to var- platforms, while, below the Dinaricum a consistent tec- ious morphostructural units. For instance, the deposits tonic complex is to be supposed. in question in western Slovenia are in contact with the The fragmental exposures require an explanation Dinaric platform, the Julian Alps and the “Sava Folds” introducing either erosion of a common overlying and (= Sava Nappe sensu MIO», 1981). In Mt. Æumberak, tectonically disintegrated megaunit or by numerous Mt. Medvednica, Mt. IvanπËica and Mt. Kalnik pelagic localized uplifts of a consistent major unit outcropping outcrops occur within “magmatic-sedimentary” forma- in tectonic windows which were afterwards slightly dis- tions and, exceptionally, within platform elements. turbed, i.e. fractured, tilted, and eroded. Likewise, the pelagic elements of the Bosnian Zone The erosion as a main factor, which would disinte- (AUBOUIN et al., 1970) are mostly in tectonic contact grate a homogeneous pelagic major unit, cannot be with different Inner Dinaric rocks, including the ophio- accepted, because, in that case, this unit should primari- lites. Also there are localities in Western Serbia (OBR- ly cover the deposits of different ages and environ- ADOVI∆ & VASI∆, 1996), as well as in Albania, ments. Such a case is improbable even when there were where localized “strange” bodies (Rubik complex, Kal- no tectonic contacts of single outcrops with adjacent ur cherts, and Lumi i Zi sections) are distributed as iso- deposits. However, in many cases the contacts are dis- lated bodies within the Mirdita Zone (CAROSI et al., tinct. At some localities younger deposits outcrop 1996; MARCUCCI & PRELA, 1996). through the older ones, thus favouring allochthony. The Besides, numerous Jurassic and less numerous Cre- relationships within carbonate terrains are characterized taceous isolated pelagic outcrops, often in visible tec- by a very important phenomenon: the rocks of the Adri- tonic contacts with shallow-water carbonate rocks, are atic carbonate platform primarily and tectonically widespread within the Dinaric carbonate platform in underlie the pelagic deposits. At the same time, the Slovenia, Croatia, Hercegovina and Montenegro, while D i n a r i c u m overlies the pelagic distal deposits (together the Budva Zone is overthrust upon the Adriatic carbon- with the underlying rocks of the Adriatic platform) sug- ate platform (HERAK, 1986, with older citations). The- gesting nappe relationships. The participation of pelagic se facts and opinions require comparison with other deposits in the Dinaricum is not obvious due to subduc- possible alternative explanations, to determine which is tional contact. In the subduction process within the con- the most convincing. tinental crust, the ductile deposits were a detachment The first possibility would concern the model with level, making possible long-rate continental subduction facies differentiation. In that case, tectonic contacts even under the “magmatic-sedimentary” formations, with adjacent facies would be uncommon. Besides, it is indicating that the dispersed pelagic outcrops within impossible to assume that similar pelagic environments them are tectonic windows. Such a concept respects the would prevail at the same time within a basin, which is dispersion of pelagic and other deposits with open sea influenced by magmatic activity and on a stabilized car- influences within the belts of different provenance and bonate platform without influences from a common their contacts with platform and basinal formations. source of the pelagic components. Comparing recent The relationships of platform and pelagic deposits are and fossil global radiolarian localities, DE WEVER & still hidden due to nappe relationships. The interior BAUDIN (1996) came to the following conclusions: (a) reconstruction of their allochthonous disturbances are “Distal basinal or oceanic environments are often opti- omitted. mal sites for the preservation of siliceous and lipid-rich organic material derived from plankton” (p. 310); (b) 3.5. THE ADRIATIC NAPPE (Adriaticum, A) “The long held assumption of a relationship between abundance of radiolarians and volcanic processes is The next lower tectonic major unit consists predom- largely erroneous” (p. 311). Even in the case when the inantly of carbonate rocks with some pelagic sediments Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 93 and flysch. It is extended on the southwestern side of are preserved within all the major facies, indicating a the overlying E p i a d r i a t i c u m (Fig. 2, A). There are also general northward (northeastward) movement (caused some detached bodies of the D i n a r i c u m overlying the by the movements in the asthenophere). All the com- A d r i a t i c u m (possibly, due to younger gravitational dis- plexes of the Outer and Inner Dinarides behaved acco- placements). The differences between them are difficult rding to their constitution, being either brittle or ductile. to establish, and require detailed analyses and regional Anyway, the rate of the disturbances suggests the exis- correlations. Recently, DROBNE & TRUTIN (1997) tence of weak zones at several levels, which made a palaeontologically confirmed the existence of a tectonic strong allochtonous imbrication possible. The continen- window of the marginal part of the A d r i a t i c u m t h r o u g h tal subductions were preceded by very complex dynam- the D i n a r i c u m at BuniÊ in the Lika. BLA©KOVI∆ ics, and have been followed by uplift of the area (verti- (1999) proposed a major tectonic classification based cal faulting), tilting, possible additional subduction and on the A d r i a t i c u m, E p i a d r i a t i c u m and D i n a r i c u m f o r obduction, rotation, and often neglected gravitational purpose of oil prospection. ROMANDI∆ & ALJINO- displacements. The time relations of the tectogenetic VI∆ (1999) easily recognized the A d r i a t i c u m b e n e a t h process are relatively easily distinguished. the D i n a r i c u m in strongly disturbed sedimentary sequ- 1. During the Variscan orogeny, vast continental sur- ences, with cumulative thickness of up to 17 km, using faces originated, upon which, later, intensive depo- geoelectric and palaeomagnetic methods. sition of terrigenous fragments occurred. However, The A d r i a t i c u m is delimited by the E p i a d r i a t i c u m in that time the continental crust was not completely on one side and by (?)Ionian deposits on the other. Lon- stabilized. Rifting and magmatic processes in the gitudinally it continues toward the southeast into the Middle Triassic (and at the beginning of the Late Gavrovo-Tripolitza domain. Sporadically, it occurs wit- Triassic) were renewed, and accompanied by ande- hin the D i n a r i c u m as tectonic windows. Remarkable is sitic extrusions (tardy-Variscan dynamics). This dis- also the Hercegovinian half-window. quiet was relatively short and final, and it prepared the basis for vast and temporally extensive sedimen- 3.6. ?THE IONIAN UNDERTHRUST (?Ionicum, I) tation of carbonate platform deposits. In the Upper The insular region of the Adriaticum is underlain by Triassic an oscillating interplatform trough was Cretaceous-Palaeogene deposits (LAWRENCE et al., formed. It remained directly connected with the 1995), possibly belonging to the Ionian Basin, and sub- open sea, from which pelagic components were sup- ducted under the Adriaticum (Fig. 2, I). This fact may plied during the whole Mesozoic era. The oscilla- justify the distinguishing of the Adriatic and Apulian tions within the trough caused periodic ingressions platforms. of pelagic deposits upon the adjacent platforms, especially in the Late Jurassic and the Late Creta- ceous. 4. CONCLUSIONS 2. North of the interplatform trough, after the Lias, the opening of the ocean (including our western branch) To avoid some discrepancies in the interpretation of occurred with simultaneous extrusions of already the Alpino-Dinaridic realm in a “geosynclinal” way, consolidated mantle rocks (ultramafites). So, the one of the posibilities is to follow the partially emended “miodynamics” and “eudynamics” were contempo- concept of continental subductions as accompanying raneous with mutual influences in their final phase. process of oceanic subduction, based upon new litho- After the extrusions of the mantle rocks (peridotites, stratigraphic and structural notions previously cited. serpentinites), the equilibrium was disturbed and The approach to the subduction mechanism encoun- northward movements of lithospheric complexes ters great difficulty due to the fact that the traces of the were initiated (as a consequence of adequate dyna- oceanic subduction are quite hidden. Only the presence mics in the asthenosphere). All this resulted in oce- of restricted outcrops of ultramafic rocks (©IMUNI∆ & anic subduction and the consuming of subducted PAMI∆, 1989; PAMI∆, 1997), secondarily emplaced material, while the more resistent ultramafites rema- into Cretaceous deposits, testifies such a process. The- ined on the surface, submitted to further distur- refore, they do not reflect primary relationships which bances. would define their origin and later tectonic displace- ments. Even the essential problem related to our part of 3. The asthenospheric northward movements were not Tethys is not obvious; it concerns the question of only localised under the oceanic lithosphere, but whether we are dealing only with a branch of Tethys or were also active under the continental part, includ- if there was a connection with the Penninic Belt below ing the trough between the Adriatic and Dinaric the Southern Alps and the Austroalpine Nappes. Also, platforms. The influence was different upon the pla- the time of the tectonic emplacement of the Slavonian tform surfaces in comparison with the oscillating Mountains (as a part of Tisia) is still under discussion. trough, in which continental subduction started. The only certain geotectonic phenomena are the Therefore, the trough narrowed and the sea level consequences of continental subductions. Their traces rose, with the ingression of pelagic material upon 94 Geologia Croatica 52/1

the marginal platform areas, overlying platform for- ed and the thickness of sedimentary complexes mations and interfingering with them. increased, not only due to piling up of subducted units but also due to the rise of the Cretaceous- 4. The Oceanic Trough was, in the Late Jurassic and Palaeogene S-granites, final volcanism, etc. the Early Cretaceous, still a place of intensive “eudynamics” accompanied by strong magmatism 7. The concentrated thermal “diapirism” was distrib- and low to medium-grade metamorphism. The clo- uted within all the tectonic units, and in this way sure of the Trough, approximately in the Middle numerous tectonic windows originated, predomi- Cretaceous, was followed by deposition of clastics nantly of the ductile flysch and pelagic deposits. At accompanied by small reefs, platy limestones, and such places the chaotic carbonate breccias on the by flysch deposits. At that time, there were no sharp northern slope of Mt. Medvednica (“Horvatove boundaries of the sedimentary basins within the stube”, Pronjak), as well as in Mt. Kalnik and Mt. frame of the Dinaridic part of the Tethys. Ravna Gora, have been interesting to many authors (e.g. BABI∆ et al., 1973; ©IMUNI∆ et al., 1993; 5. Due to the closure of epicontinental and oceanic PRTOLJAN et al., 1995), but a final explanation belts, the crust generally coalesced and afterwards has not yet been found. Their emplacement is char- behaved more or less as a single major unit com- acterized by tectonic contacts with the adjacent posed of rigid and weak domains. This fact deter- rocks. The age of the fragments belong to different mined the future behaviour in respect to the north- horizons of the Mesozoic, with a matrix of Campan- ward movement in the asthenosphere, which contin- ian age. ©IMUNI∆ et al. (1993, p. 614) assume that ued. The multiple continental subductions were inf- the upper boundary of these “exotic breccias” is luenced by ductile horizons. In this way a complex post-Palaeocene, and suggest “that they might have allochthonous structural pattern has originated. Alo- been originated along subduction zones”. It could be ng the Interplatform Trough, the subduction was added that also localized rise of parts belonging to most intensive, resulting in the carbonate rocks with different subducted nappes contributed to the gene- the flysch of the Adriatic platform (A d r i a t i c u m) sis of the breccias, making in fact the (additionally underlying not only the pelagic elements (of Epi- disturbed) tectonic windows. I am conscious that adriatic provenance), but elsewhere are also directly such an unconfirmed opinion might be considered overlain by the carbonate rocks of the Dinaric plat- as too courageous, but it should be taken into acco- form (D i n a r i c u m). The D i n a r i c u m has been sub- unt in future discussions. ducted under the oceanic formations (S u p r a d i n a r - icum, s. str.) which underlie Palaeozoic and Triassic 8. The mentioned vertical diversification was intensifi- platform elements of the Uppermost Nappe. More- ed during the Neogene, and caused disintegration, over, in the frames of the major nappes imbrication tilting, rotation and gravitational displacements of is also present. Delimitation and gradation of tecton- parts of the nappes. Therefore, fragments with dif- ic units is difficult due to the fact that parts of pelag- ferent vergencies are to be found even upon Neo- ic and flysch deposits primarily overlie platform gene sediments. The process itself is considered as margins, and are, in the tectonic sense, only parts of very complicated (possibly combined with slight the platform nappe units. Along the major contact subductions), and an explanation exceeds the topic zones, the underthrusting character of contacts is of this paper. obvious, though not necessarily equal to one anoth- 9. The proposed model can be understood on the basis er. Then, subduction process increased towards the of the mobilistic interpretation of geotectonic prob- west (northwest) and, therefore, the zones wedge lems. The assumption of continental subductions out. In this way the Dinaric strike (SE-NW) was helps to explain not only major structures but also finally established. Only the elements of the Upper- “strange”, “uncommon”, “isolated”, and “exotic” most Nappe have not been essentially influenced, phenomena, as single constituents of major tectonic and so the difference in strike between this Nappe units, within logical, though not anticipated structur- and the Dinaridic structural units (nappes) could be al frameworks. explained. Such a dynamics lasted approximately 10. Due to a nappe system, it is necessary to distinguish until the end of the Oligocene and, thus, the basis not only the previously discussed homogeneous tec- for the Neogene indentation process was prepared. togenetic units (Uppermost Nappe, Supradinaricum, The consequences of the process itself have been s. str., D i n a r i c u m, E p i a d r i a t i c u m , A d r i a t i c u m a n d interpreted in several papers (e.g., RATSCHBACH- (?)Ionian underthrust) but also some more or less ER et al., 1991), though the moving forces were not individualized morphotectonic complexes, e.g., the well defined. According to this proposal, they shou- Adriatic area, High Karst Belt, Outer Dinarides, ld be represented by continental subductions. Inner Dinarides, the Pannonian Basin, etc. To this 6. Simultaneously, in the main Alpine and Carpathian category of terms also belong the Mid-Transdanu- domains, the subductions were directed generally bian Zone, Zagreb Zone, and “Sava Folds”. They all toward the south. Therefore, our region was squeez- are characterized by a heterogeneous, composite Herak: Tectonic Interrelation of the Dinarides and the Southern Alps 95

constitution terminated during neotectonic dynam- BABI∆, Lj. & ZUPANI», J. (1973): Najmlaa jura i ics, and are used in the regional geology and geo- najstarija donja kreda u IvanπËici (uppermost Juras- morphology. sic and Early Cretaceous deposits on Mt. IvanπËica - northern Croatia).- Geol. vjesnik, 26 (1972), 267- 11. I hope that the intention of this paper to explain the 272. tectonic setting of the Alpino-Dinaridic realm in a mobilistic sense may be generally acceptable base BABI∆, Lj. & ZUPANI», J. (1978): Kossmatovi “Æele- for further discussions. Therefore, the concept may znikarski vapnenci i dolomiti” i “Zaliloπki krovni not be considered as final. Many pecularities remain πkriljavci” u predgorju Julijskih Alpa; podaci o open to further confrontations, based upon addition- stratigrafiji, facijesu i paleogeografskom znaËenju al, more accurate (confirming or emending) data. (Kossmat’s “Kalke und Dolomite von Eisnern” and “Dachschiefer von Salilog” in the Julian Prealps: data about stratigraphy, facies and paleogeogra- Acknowledgements phy).- Geol. vjesnik, 30/1, 21-42. ˘ The preparation of the manuscript required addition- BABI∆, Lj., GU©I∆, I., & DEVIDÉ-NEDELA, D. al discussions of some elementary data with experts of (1973): Senonski krπnici na Medvednici i njihova different research fields, e.g., with Ljubomir BABI∆, krovina (Senonian breccias and overlying deposits Stjepan BAHUN, Mirko BELAK, Josip BUKOVAC, on Mt. Medvednica - northern Croatia).- Geol. vjes- Ivan GU©I∆, Domagoj JAMI»I∆, Vladimir JELASKA, nik, 25 (1971), 11-27. Vladimir MAJER, Pero MIO», Jakob PAMI∆, Branko BELAK, M., PAMI∆, J., KOLAR-JURKOV©EK, T., SOKA», Antun ©IMUNI∆, Marko ©PARICA, Ivo VE- PECSKAY, Z. & KARAN, D. (1995a): Alpinski LI∆, etc. The drawings have been executed by Miroslav regionalnometamorfni kompleks Medvednice - sje- KLADNI»KI. To all of them I express my sincere gra- verozapadna Hrvatska.- 1. hrv. geol. kongres (Opa- titude. tija, 1995), Zbornik radova, 1, 67-70, Zagreb. BELAK, M., SREMAC, J., CRNKO, J. & KOLAR- 5. REFERENCES JURKOV©EK, T. (1995b): Paleozojske stijene nis- kog stupnja metamorfizma na jugoistoËnoj strani AUBOUIN, J., BLANCHET, R., CADET, J.-P., CEL- Medvednice (sjeverozapadna Hrvatska).- 1. hrv. ge- ET, P., CHARVET, J., CHOROWICZ, J., COUSIN, ol. kongres (Opatija, 1995), Zbornik radova, 1, 71- M. & RAMPNOUX, J.-P. (1970): Essai sur la géo- 74, Zagreb. logie des Dinarides.- Bull. Soc. géol. de France, 12, BERCZI-MAKK, A., HAAS, J., RALISCH-FELGEN- 1060-1095. HAUER, E., & ORAVECZ-SCHEFFER, A. (1993): BABI∆, Lj. (1973): Bazenski sedimenti gornjeg titona i Upper Paleozoic-Mesozoic formations of the Mid- valendisa zapadno od Bregane (Upper Tithonian to Transdanubian Unit and their relationships.- Acta Valanginian basinal sediments west of Bregana).- geol. Hungar., 36/3, 263-296. Geol. vjesnik, 26, 11-27. BLANCHET, R., CADET, J.P. & CHARVET, J. BABI∆, Lj. (1974): Razdoblje otriv-cenoman u Æum- (1970): Sur l’existence d’unités intermediaires entre berku: stratigrafija, postanak sedimenata i razvoj la Zone Haut-Karst l’unité du flysch bosniaque, en prostora (Hauterivian to Cenomanian time in the Yougoslavie: la sous-zone prékarstique.- Bull. Soc. region of Æumberak, Northwestern Croatia: stratig- géol. de France, 12, 227-236. raphy, sediments, paleogeographic, paleotectonic BLA©KOVI∆, I. (1999): Subsurface tectonic relations - evolution).- Geol. vjesnik, 27, 11-33. a basis for determination of the zones of petroleum- BABI∆, Lj. (1975): Kondenzirani lijas Medvednice i geological prospectivity.- Working materials, 2nd IvanπËice i njegovo znaËenje za interpretaciju paleo- intern. Symposium of Petroleum Geology, Croat. geografskog razvoja unutarnje dinarske regije (Con- Acad of Sci. and Arts, Faculty of Mining, Geology densed Liassic sedimentation on Mt. Medvednica and Petroleum Engineering and INA, 133-145, and Mt. IvanπËica - northern Croatia - and its signi- Zagreb. ficance for the interpretation of the paleogeographic BUKOVAC, J. (1988): Tectonics of the contact zone of evolution of the Inner Dinaric belt).- Geol. vjesnik, the Dinaricum and Supradinaricum in the area of Zagreb, 28, 11-18. Krnjak-BariloviÊ-Karlovac, Croatia, Yugoslavia (Tektonski odnosi u kontaktnoj zoni Dinarika i BABI∆, Lj. (1980/81): The origin of “Krn Breccia” and Supradinarika u podruËju Krnjak-BariloviÊ-Karlo- the role of the Krn area in the Upper Triassic and vac, Hrvatska, Jugoslavija).- Acta geol., 18/1, 1-12, Jurassic history of the Julian Alps (Postanak “BreËe Zagreb. Krna” i uloga predjela Krna u povijesti Julijskih Alpa u gornjem trijasu i juri).- Vesnik Zav. geol. BUSER, S. (1977): Osnovna geoloπka karta SFRJ geofiz. istraæ., (A), Beograd, 38-39, 59-75. 1:100.000. List Celje L33-67.- Geol. zavod Ljub- 96 Geologia Croatica 52/1

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Manuscript received February 3, 1998. Revised manuscript accepted May 28, 1999.