Tisljar et al.indd Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits of the Karst Dinarides Josip TIŠLJAR1, Igor VLAHOVIĆ2, Ivo VELIĆ2 and Branko SOKAČ2 1. INTRODUCTION Platform carbonate deposits found along the NE Adri- atic coast, usually referred to as the “Karst Dinarides”, represent a belt approximately 700 km long and, (after tectonic reduction), 80–210 km wide. This huge carbo- nate body stretches from the Julian Alps along the border between Italy and Slovenia, through the western and central parts as well as the coastal area and Adriatic islands of Croatia, through the western and southern part of Bosnia and Herzegovina to SE Montenegro and NW Albania (Fig. 1). The entire area was characterised by the long-term (Middle Triassic to Middle Eocene, or in some areas, from Carboniferous) existence of carbonate platform environments, resulting in a very thick sequence of deposits. After POLŠAK (1965a), who suggested that “the most appropriate term for the entire depositional area with characteristics of carbonate sill (the old term for carbonate platform – auth. comm.) stretching from NW Slovenia to Montenegro would be Adriatic Zone”, the area of Karst Dinarides was treated by numerous authors as a united carbonate platform, although with different names. The most common terms were “Car- bonate shelf of Dinarides” (JELASKA, 1973), “Plat- form of the Outer Dinarides” (GRANDIĆ, 1974), “Adriatic Plate (“carbonate platform”)” (POLŠAK, 1981), “Carbonate Platform of the Outer Dinarides” (TIŠLJAR, 1983), “Mesozoic Carbonate Platform” (TIŠLJAR et al., 1983b), “Dinaric Carbonate Platform” (OGORELEC, 1987; DRAGIČEVIĆ & VELIĆ, 1994; BUSER, 1989), “Adriatic–Dinaric Carbonate Platform” (VELIĆ et al., 1987; GUŠIĆ & JELASKA, 1993), “Adriatic–Dinaridic Carbonate Platform” (PAMIĆ et al., 1998) and “Adriatic Carbonate Platform” (GUŠIĆ & JELASKA, 1990). All these names are synonymes for a single carbonate platform without regard to the recent geotectonic situation. Since the 2nd International Symposium on the Adri- atic Carbonate Platform, which was held in 1991 in Zadar, Croatia (VLAHOVIĆ & VELIĆ (eds.), 1991), it seems that most of the authors refer to this carbonate platform as the Adriatic Carbonate Platform. A second, smaller group of authors accepted the geotectonic concept of the Dinarides according to HERAK (1986), considering the existence of several Geologia Croatica 55/2 139–170 7 Figs. ZAGREB 2002 Key words: Carbonate platform facies, Carbonate plat- form slope, Carbonate debrite and turbidite, Emer- sion, Bauxite, Dolomite, Sabkha evaporite, Synsedi- mentary tectonics, Jurassic, Cretaceous, Adriatic Carbonate Platform, Karst Dinarides, Offshore and coastal Adriatic areas, Croatia, Slovenia, Bosnia and Herzegovina, Montenegro. 1 University of Zagreb, Faculty of Mining, Geology and Petroleum Engineering, Pierottijeva 6, HR-10000 Zagreb, Croatia; e-mail: jtisljar@rgn.hr 2 Institute of Geology Zagreb, Sachsova 2, HR-10000 Zagreb, Croatia. Abstract Platform carbonate deposits of the Karst Dinarides area have a strati- graphic range from the Middle Triassic (or even Carboniferous in some places) to the Middle Eocene, forming a belt nearly 700 km long and, (after reduction by younger tectonics) 80–210 km wide. Besides their significant thickness (4500 to 8000 m) they are characterised by frequent lateral and vertical alternations of differ- ent facies, mostly associated with shallow marine environments. Environments ranging from peritidal through low-energy shallow subtidal–lagoons, restricted inner platform shallows, high-energy tidal bars, beach and shoreface to reefal–perireefal predominate, but there are also carbonate slope deposits and those representing temporarily drowned platform facies and intraplatform troughs. The Jurassic to Cretaceous part of this carbonate succession has been subdivided into 19 megafacies units (9 for the Jurassic and 10 for the Cretaceous), the majority of which represent an inner part of the ancient Adriatic Carbonate Platform. Marginal parts of the plat- form are mostly buried, either by the recent Adriatic Sea along the SW margin, or younger deposits along the NE margin; at some locali- ties such Jurassic and Cretaceous deposits are represented by debrites and/or carbonate turbidites. An additional short review of the overly- ing Uppermost Cretaceous and Palaeogene deposits (4 megafacies units) enabled a better insight into the post-platform evolution. The very complex vertical and lateral alternation of different megafacies units, including emerged areas which were observed throughout the studied sequence in different parts of the Karst Dinarides, indicate the significant palaeogeographic dynamics of the region. This variability resulted from interaction of the global eustatic signal and local factors, including extensive organic production on the carbonate platform and synsedimentary tectonics controlled by the specific palaeogeographic position of the platform during its geologi- cal history. 140 Geologia Croatica 55/2 141Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... palaeogeographic units in the same area during the Mesozoic. According to HERAK (1986, 1989, 1991, 1993) two carbonate platforms existed in the area of the Karst Dinarides from the Late Triassic to the Eocene – the Adriatic Carbonate Platform (Adriaticum) and the Dinaric Carbonate Platform (Dinaricum), separated by a persistant deep-water interplatform trough (Epi- adriaticum). For more information on this concept see BLAŠKOVIĆ (2001) and VLAHOVIĆ et al. (2002c – this vol.). However, in this paper we will not use any specific term for the carbonate platform on which most of the carbonate deposits originated – instead we will use the term Karst Dinarides. Namely, the Adriatic Carbonate Platform s.s. comprises deposits of a stratigraphic range from the Upper Lias to the end of Cretaceous ? Fig. 1 Location map with schematic drawing of the Mesozoic platform carbonate deposits of the Karst Dinarides region. Z welllM-6 ". we111M-3 .0" welllM-4 well~ welIIM-2- 2b weill':, offshore well Kollllljka -1 .,. Study area: ". ". " . ". ". "'. ". "'. ". 20. ~. ... Wa.t.m, central and southern Istria Northern Istria ". So. 3d. •• 50. ". 50. ". 50. M. Eastern Istrla - CIC:arlja ML Southern Isbia - well Pula-1 BriJunl Adriatic aea (aIflIhore wells Jadran-86) Adriatic aa. (offshore weill lfira More 1M - 1 to 5) Adriatic sea (afl'shore wells Jadran J-15) Island of Susak. (well Su-1) Island ofPremuda (well Pr-1) 1.landa of Komati (well Kale-1) V.1.bit Mt. - Mali Halen V.lsblt Mt. - Kubus Velebit Mt. - Lifko Cerja Mazln Brunj - PlllYlce Lakee Suha KllIIjina Dolenjska Nanos ML Hrullca ML Logdka Planota Trnovski Gozd 1Ia . Kar10vac area (MllflinlCa.k - Duga RealI) ISbell Velika Kapala MI.- Sanj-Ogulin profile 8d. GorKi Kotar - PIaIIIk- Gomje Jelenje lie . GorKi Kotar - SknIcI area 81". GorKi Kotar - ZIobin IU'H 7 • Nikiic II • Podgortca II • CeUnje 10.. Dlnara Mt. lOb. Kamelnlca MI. 11 • Biokovo Mt. 12 • Trogirarea (well Boraja-1) 13 • Island of Brae 14 • Drvar area 15 • Smelica MI. " " , .. 10' 100 , .. 19 " " 22 " " , .. '" "" ,., " " " " '" '" " 33 " Platform carbonates . ..1 a MI Banjaluka ar ... GlamcK! 8rea Trebinja .I'M Dubrovnlk area (Siano - ZavaJa profile) Dubrovnlk area (OeoJnlk - GllIIpcI profile) Dubrovnlk area (KonaYOska brda proftl.) Dubrovnik ..... (Cerovac - Hum profile) Island of L.astovo Kupl'M area PokuplJe Bihafarea Lamel, MaovIce Vinodol Ravnl Kotarl (wells RK-1 to RK-4) Wells Nln (Nln-1) Island of Olib (outcrops and well OL-1) Island of 1st Island of Dugl otok (outcrops and well 00-1) Island of Hvar Island of Crea Island of Krk Island of LoIinj Island of Pag OI'fshore well Koraljka-1 Island of Vis (VIa-1) Island of Korfula 50 BOSNIA AND 100 kin I HER EGOVINA 35 • Island of Mljet sa • Peljelac peninsula 37 • Primolten area sa.. Janj area 311b. Jajeearea 3k. Oonji Beipelj area 3!1 • Banjaluka area I 140 Geologia Croatica 55/2 141Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... (see discussion by DRAGIČEVIĆ & VELIĆ, 2002 and VLAHOVIĆ et al., 2002c in this vol.), and we will discuss also some older and younger deposits. Carbonate platform deposits of the Karst Dinarides are, besides their significant thickness (4500–8000 m, 6000 m in average), characterised by frequent lateral and vertical alternations of different facies, mostly associated with shallow marine environments. Environ- ments ranging from peritidal through low-energy shallow subtidal – lagoons, restricted inner platform shallows, high-energy tidal bars, beach and shoreface to reefal–perireefal areas are the most common, but the succession also comprises deposits of carbonate slopes and temporarily drowned platform facies and intraplatform troughs. On the basis of their main sedimentological, lithological, biofacies and lithofacies characteristics, the deposits accumulated in this area from the Early Jurassic to Eocene can be subdivided into several mega- facies units characterised by their extensive occurrence, i.e. regional importance, regardless of their thickness. For subdivision of rock sequences into megafacies, the additional works of numerous other investigators were also consulted. Unfortunately, it was commonly impossible to use data from older publications, because although information on stratigraphy, palaeontological composition and general lithology was provided elements needed for facies reinterpretation were lacking; therefore these papers were neither used nor cited. This paper deals with a several thousand metre thick sequence of deposits covering a huge area, and therefore only simplified typical geological columns are presented. For detailed sedimentological and stratigraphical interpretations and illustrations, interested readers should check the original literature cited in this paper. The lateral and vertical pattern of different mega- facies units, their locations, thickness and duration of sedimentary environments resulting in their depo- sition provide significant information not only about conditions in the depositional area but also about synsedimentary tectonics and the palaeogeomorphologi- cal evolution of the carbonate platform. Temporal and spatial correlation of the megafacies identified here document the main sedimentological and tectonic events in the area of the Karst Dinarides. Additionally, these data provide important arguments for interpretation of the palaeogeography of the entire area during the Jurassic and Cretaceous (and Palaeo- gene to a certain extent). 2. CARBONATE MEGAFACIES OF THE JURASSIC DEPOSITS Jurassic carbonate deposits of the Karst Dinarides can be subdivided into 9 megafacies units (Figs. 2–4): J–1: Megafacies of peritidal micritic, fenestral and vadose limestones with interbeds of early-diagenetic dolomites and emersion breccia, emersions and occasional bauxites; J–2: Megafacies of lagoonal and subtidal inner platform oncoid, pelletal and skeletal mudstones/wackesto- nes; J–3: Megafacies of bioturbated and late-diagenetically dolomitized “spotty limestones” – mudstones and wackestones deposited in isolated and restricted lagoon/deeper subtidal areas of the inner platform; J–4: Megafacies of lithiotid and brachiopod lithosomes and tempestite coquinas of shallow subtidal and lagoonal regions of the inner platform; J–5: Megafacies of ooid grainstones deposited in envi- ronments with agitated water and ooid bars; J–6: Megafacies of skeletal and intraclastic grainstones/ rudstones deposited in shallows with agitated water; J–7: Megafacies of peri-reefal bioclastic limestones (rudstones and grainstones) with hydrozoan, stroma- toporoid and coral patch reefs and biostromes; J–8: Megafacies of “limestones with cherts” (including “Lemeš deposits”), deposited within intraplatform troughs with temporary or continuous connection to the open sea, and J–9: Megafacies of late-diagenetic dolomites. 2.1. Megafacies of peritidal micritic, fenestral and vadose limestones with interbeds of early- diagenetic dolomites and emersion breccia, emersions and occasional bauxites (J–1) Deposits of megafacies J–1, i.e. peritidal micritic, fenestral and vadose limestones with interbeds of early- diagenetic dolomites and emersion breccia, emersions and occasional bauxites, are most common in the Lower and Middle Lias, Dogger, Oxfordian, Kimmeridgian and Upper Tithonian deposits (Figs. 2–4). They are mostly composed of fenestral and/or vadose limestones (mudstones, pelletal and/or skeletal wackestones), with layers of LLH-stromatolites and skeletal/pelletal packstones and grainstones, while black-pebble and tempestite breccias and early-diagenetic dolomites are infrequent (TIŠLJAR, 1976; TIŠLJAR & VELIĆ, 1991). At some localities, mostly within Middle Lias and Tithonian sediments, deposits of this megafacies are characterised by numerous shallowing-upward cycles on a dm- to m-scale. Cycles ending with desiccation cracks, desiccation breccia or vadose features (“desic- cation cycles” – TIŠLJAR et al., 1983a; “vadose rhythms” and “vadose cycles” – TIŠLJAR, 1983; TIŠLJAR & VELIĆ, 1993) are common. A very good example of these cycles was described from Upper Tithonian deposits in western Istria (locality 1a on 142 Geologia Croatica 55/2 143Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... a: w it :::l 6b-c SENJ - OGULIN PROFILE __ ~M=-EGAFACIES UNITS ~ J-9 ~ K-10 1 ~.,. ~ .,.1 J-8 U:: ] K-9b I:lFafl J-7 ~ ~ J-6 J-5 J-4 J-3 1 1 J-2 Iiii J-1 TRIASSIC 1 1 T-3 [11';,1;1 '. :'. ,.'. CJ 3 ~ K-9a K-8 K-6a K-6 K-5 K-4 K-3 K-2 142 Geologia Croatica 55/2 143Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... Fig. 1), but similar deposits were also found in a penecontemporaneous succession in offshore wells in the northern Adriatic (locality 2c, wells J–15/3, J–15/4, J–15/6, J–18/5; VESELI, 1999). Early-diagenetic dolomites without traces of eva- porites, formed by early-diagenetic dolomitization of supratidal carbonate muds under a relatively humid climate have been found only as thin interbeds within peritidal limestones of Liassic age, e.g. in the Lika region near Ličko Cerje and Mazin (localities 3c and 3d), and within Tithonian subtidal algal “clypeina limestones” near Slunj in central Croatia (locality 4). Emersion breccias with typical palaeokarstic features and stratigraphic hiatuses, with sequences characterised by reductions of several tens to several hundreds metre thick intervals, partly with bauxite (Figs. 2–4) have been documented from various stra- tigraphic levels in different regions of the Karst Dinari- des. A hiatus lasting from the Middle Lias to the Kimme- ridgian has been documented in Trnovski Gozd (NIK- LER, 1978), the Suha Krajina in Slovenia (locality 5a – BUSER, 1969; DOZET, 1994), the Karlovac environs in Croatia (locality 6a – BUKOVAC et al., 1974; ŠPARICA, 1981; DRAGIČEVIĆ & VELIĆ, 1994), western and central Bosnia (ŠPARICA, 1981; MOJI- ČEVIĆ et al., 1978; MARINKOVIĆ & AHAC, 1980; VUJNOVIĆ, 1980) and in Montenegro west of Nikšić (locality 7 – RADOIČIĆ & VUJISIĆ, 1970), and north and northeast of Podgorica (locality 8 – ŽIVALJEVIĆ et al., 1971). Upper Jurassic hiatuses or shorter gaps with karsti- fication and/or bauxite formation were determined in different regions of the Karst Dinarides, usually in a stratigraphic range from the Oxfordian to the late Tithonian. E.g., in Slovenia important emersions occur mostly within Kimmeridgian beds (BUSER et al., 1967; DOZET & MIŠIČ, 1997) in the Nanos Mt. (locality 5c), near Hrušica Mt. (locality 5d), in Logaška Planota (locality 5e) and Suha Krajina (locality 5a). In Croatia emersion in western Istria (locality 1a) lasted from the latest Oxfordian/earliest Kimmeridgian to the late Tithonian (VELIĆ & TIŠLJAR, 1988), on the Biokovo Mt. (locality 11, Fig. 3) from Early Oxfordian to Early Kimmeridgian and from Late Kimmeridgian to the Middle Tithonian (TIŠLJAR et al., 1989; TIŠLJAR & VELIĆ, 1991), and on the Dinara Mt. (locality 10a) from late Tithonian to the Early Valanginian (Fig. 5). In western Bosnia emersion of similar duration to that in Istria was recorded NW of Drvar (locality 14 – ŠUŠNJAR & BUKOVAC, 1978), in Srnetica Mt. SE from Bosanski Petrovac (locality 15 – VRHOVČIĆ et al., 1983) and NW from Glamoč (locality 16 – AHAC et al., 1977), in eastern Herzegovina N and NW from Trebinje (locality 17 – NATEVIĆ & PETROVIĆ, 1967), and in Montenegro in the region of Nikšić (locality 7 – RADOIČIĆ & VUJISIĆ, 1970; VUJISIĆ, 1972) and NW of Cetinje (locality 9 – ANTONIJEVIĆ et al., 1969). 2.2. Megafacies of lagoonal and subtidal inner platform oncoid, pelletal and skeletal mudstones/wackestones (J–2) Megafacies J–2 is a dominant facies type within Juras- sic deposits (Figs. 2–4). It is composed of thick-bedded to massive wackestones/packstones to floatstones with algal oncoids (“cyanoids”– RIDING, 1983), as well as pelletal and skeletal wackestones and mudstones containing faecal pellets, gastropod cortoids and centripetally micritized benthic foraminiferal tests and mollusc bioclasts. Massive and/or thick-bedded mudstones and wacke- stones of megafacies J–2 are predominant in the Middle Lias, Lower and Middle Dogger, Oxfordian and Kimme- ridgian carbonates. This megafacies prevails in Velika Kapela Mt. and in the Senj–Ogulin profile (locality Fig. 2 Correlation of Jurassic and Cretaceous platform carbonate megafacies from the Senj–Ogulin profile (modified after MATIČEC et al., 1997), Triassic, Jurassic, Cretaceous and Palaeogene carbonates of northern margin of the carbonate platform in the Karlovac–Duga Resa area (modified after BUKOVAC et al., 1974; DRAGIČEVIĆ & VELIĆ, 1994, 2002), and Cretaceous–Palaeogene carbonates of northern margin of the carbonate platform in the Donji Bešpelj area, Bosnia and Herzegovina (modified after DRAGIČEVIĆ, 1987; DRAGIČEVIĆ & VELIĆ, 1994). Legend: K–10: Megafacies of calclithite–marly flysch; K–9a: Megafacies of slope carbonates: carbonate debrites and coarse-grained carbonate turbidites; K–9b: Megafacies of slope carbonates: middle- to fine grained carbonate turbidites or allodapic limestones; K–6: Megafacies of rudist coquinas/coquinites with small rudist biostromes and lithosomes; K–6a: Megafacies of coarse-grained rudist coquinas/coquinites accumulated within shallows with agitated water, “intra-shelf troughs”, and particularly on the slope toward the open sea; K–5: Megafacies of intraclastic/peloidal and skeletal foreshore and shoreface grainstones and packstones; K–4: Megafacies of inner platform lagoonal and shallow subtidal oncoid and peloidal micritic limestones; K–3: Megafacies of peritidal–tidal flat pelletal and stromatolitic limestones forming shallowing-upward cycles; K–2: Megafacies of peritidal and vadose limestones, black-pebble breccia/conglomerates, emersion breccia, clays, swamp deposits and palaeosols, long-lasting emersions and bauxites; J–9: Megafacies of late-diagenetic dolomites; J–8: Megafacies of “limestones with cherts” (including “Lemeš deposits”), deposited within intraplatform troughs with temporary or continuous connection to the open sea; J–7: Megafacies of peri-reefal bioclastic limestones (rudstones and grainstones) with hydrozoan, stromatoporoid and coral patch reefs and biostromes; J–6: Megafacies of skeletal and intraclastic grainstone/rudstones deposited in shallows with agitated water; J–5: Megafacies of ooid grainstones deposited in environments with agitated water and ooid bars; J–4: Megafacies of lithiotid and brachiopod lithosomes and tempestite coquinas of shallow subtidal and lagoonal regions of the inner platform; J–3: Megafacies of bioturbated and late-diagenetically dolomitized “spotty limestones” – mudstones and wackestones deposited in isolated and restricted lagoon/deeper subtidal areas of the inner platform; J–2: Megafacies of lagoonal and subtidal inner platform oncoid, pelletal and skeletal mudstones/wackestones; J–1: Megafacies of peritidal micritic, fenestral and vadose limestones with interbeds of early-diagenetic dolomites and emersion breccia, emersions and occasional bauxites; T–3: Megafacies of peritidal and supratidal carbonates – Main Dolomite (Hauptdolomit). 144 G eologia C roatica 55/2 145 Tišljar, V lahović, Velić & S okač: C arbonate P latform M egafacies of the Jurassic and C retaceous D eposits... 6b–c on Fig. 1), in the D ogger of Velebit M t. (localities 3a–b), and B iokovo M t. (locality 11), as w ell as in the Trnovski G ozd (locality 5f) and K arlovac area (locality 6a), and Low er M alm of the D ubrovnik region (locality 18b – O sojnik–G repci area). Sim ilar deposits are also know n w ithin Jurassic deposits of other areas of the K arst D inarides, but lite - rature data are quite scarce. E.g., deposits belonging to m egafacies J–2 can also be found in the D ogger of the central part of the K arst D inarides in w estern B osnia 3a SOUTH.VELEBIT Mt. UPPER n '//////) ?'..?'".az..-... n 11 BIOKOVOMt. :E .......... _ ............. -....., ...J ,,_ r. ....... ,.~~ -.....,~-'~n ..... ~ o Kim""",,,,,,,g Zw <~ I ~;'//-%:Q ~ a: " wQ "" o ~ UPPER '\";';";"';";';'~~~::?-~--'~ r ... ~ ~;;;~ .... ,~ .. -.... -. : .... :: ... : .... ~:.!: ... ~Z£L£LC..-.. ULZ~ --'azr-£.t'T~ .-." ', .. " '~' ;,,',;:., ~ .... : mmmmr;:!:'*'~:";';~;:·"~';~ I ::... ~~ UPPER TRIASSIC T-3 Main Dolomite -J-1 J-2 .. MEGAFACIES UNITS ~~ ~':\:i;':~': J·3 J-4 J-5 J-6 18a SLAND - ZAVALA jROFILE :" '.,~ :, . " ~:,,,, , -c;.""~'."" " ' ;;, .~."". J-7 18b OSOJNIK·GREPCI , ...... . ~ .•. J-9 K-2 K-3 18e KQNAVOSKA BRDA L. ~/////) .////// . "~, ,-, "~, ,-, ,-, UPPER TRIASSIC 144 Geologia Croatica 55/2 145Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... and Croatia, in Malm deposits of Suha Krajina in Slovenia (locality 5a; DOZET, 1995), the Oxfordian and Kimmeridgian of SE Montenegro, and Upper Kimmeridgian and Tithonian of Eastern Herzegovina (RADOIČIĆ, 1966), etc. Upper Malm deposits are frequently composed of algal wackestones, (so-called Clypeina limestones), which usually represent the initial members of small- scale shallowing-upward cycles (TIŠLJAR & VELIĆ, 1991). 2.3. Megafacies of bioturbated and late- diagenetically dolomitized “spotty limestones” – mudstones and wackestones deposited in isolated and restricted lagoon/deeper subtidal areas of the inner platform (J–3) Deposits of megafacies J–3 are typical for the Upper Lias of the Velebit Mt. (Figs. 2 and 3; localities 3a – Mali Halan and 3b – Kubus), Velika Kapela Mt. and Senj–Ogulin profile (locality 6b–c), and Platak–Gornje Jelenje in Gorski Kotar (locality 6d). This megafacies is widely distributed in the western part of the Karst Dinarides, stretching from W Bosnia and S Croatia (northern Dalmatia) towards the NW into southern Slo- venia (TIŠLJAR & VELIĆ, 1991; DOZET & ŠRIBAR, 1998a; DRAGIČEVIĆ & VELIĆ, 2002). However, it is completely missing in the ESE, from central Bosnia towards Herzegovina, Montenegro and the Croatian southern Adriatic coast (Fig. 3). The main characteristic of these “spotty limestones” is intense bioturbation of carbonate muds in restricted areas with very reduced fossil assemblages, indicating low sedimentation rates during late Lias. The depositi- onal area was probably an isolated, restricted lagoon in the inner part of the platform, formed by the interaction of gentle synsedimentary tectonics and eustatic sea- level change. This spotty appearance is a consequence of biotur- bation and different amounts of organic matter in a host rock (predominantly mudstones) and bioturbation infillings (mostly wackestones to packstones), although differences have been subsequently exaggerated by the variable influences of late-diagenetic dolomitization and recrystallization. 2.4. Megafacies of lithiotid and brachiopod lithosomes and tempestite coquinas of shallow subtidal and lagoonal regions of the inner platform (J–4) Deposits separated into megafacies J–4 are present only within the Middle Lias deposits (Figs. 2 & 3), in Velebit Mt. (localities 3a–b), near Duga Resa in the Karlovac area (locality 6a), Velika Kapela Mt. and Senj–Ogulin Profile (locality 6b–c), and Dubrovnik area (locality 18c – Konavoska Brda). Biostromes are 0.3–0.8 m thick, and are characteri- sed by their limited lateral extent. They are composed of very large shells of lithiotids and brachiopods lithified in living position, and occur only at some localities, for example, on the Kubus ridge of Velebit Mt. (locality 3b) and Konavoska Brda near Dubrovnik (locality 18c). However, shell coquinas and tempestite coquinas consisting of coarse debris of lithiotids and brachiopods very often occur in penecontemporaneous deposits, both in these and other aforementioned localities (e.g. JELASKA & VELIĆ, 1971; TIŠLJAR & VELIĆ, 1991; BUSER & DEBELJAK, 1996; DEBELJAK & BUSER, 1998). Limestones with lithiotids can be found throughout the area of the former platform except for its margi- nal parts (Fig. 1; DRAGIČEVIĆ & VELIĆ, 2002). Depending on bathymetry and morphology of the sea bottom, the frequency of these beds varies from place to place, with maximal 4 to 12 beds in Middle Lias of the Velebit Mt. (locality 3b; SOKAČ, 1973), and minimal 1 to 3 beds in the W Gorski Kotar (Platak–Gornje Jelenje – locality 6d). Tempestite coquinas were deposited by storm waves and storm tides in shallow subtidal to lower intertidal environments, and are associated with limestones of megafacies J–1, J–2 and J–6. 2.5. Megafacies of ooid grainstones deposited in environments with agitated water and ooid bars (J–5) Deposits of megafacies J–5 are most common in the Middle and Upper Lias and Dogger of the Trnovski Gozd (locality 5f on Fig. 1), in the Upper Lias, Dogger and Malm succession of Velika Kapela Mt. and the Senj–Ogulin profile and Karlovac area (Fig. 2), and Fig. 3 Correlation of the Jurassic platform carbonate megafacies units of Velebit Mt. (Mali Halan), Biokovo Mt. (area of Kozica) and the southern Adriatic (locations 18a – Osojnik and 18b – Konavoska brda). Partly modified after TIŠLJAR & VELIĆ (1991). Legend: K–3: Megafacies of peritidal–tidal flat pelletal and stromatolitic limestones forming shallowing-upward cycles; K–2: Megafacies of peritidal and vadose limestones, black-pebble breccia/conglomerates, emersion breccia, clays, swamp deposits and palaeosols, long-lasting emersions and bauxites; J–9: Megafacies of late-diagenetic dolomites; J–7: Megafacies of peri-reefal bioclastic limestones (rudstones and grainstones) with hydrozoan, stromatoporoid and coral patch reefs and biostromes; J–6: Megafacies of skeletal and intraclastic grainstone/rudstones deposited in shallows with agitated water; J–5: Megafacies of ooid grainstones deposited in environments with agitated water and ooid bars; J–4: Megafacies of lithiotid and brachiopod lithosomes and tempestite coquinas of shallow subtidal and lagoonal regions of the inner platform; J–3: Megafacies of bioturbated and late-diagenetically dolomitized “spotty limestones” – mudstones and wackestones deposited in isolated and restricted lagoon/deeper subtidal areas of the inner platform; J–2: Megafacies of lagoonal and subtidal inner platform oncoid, pelletal and skeletal mudstones/wackestones; J–1: Megafacies of peritidal micritic, fenestral and vadose limestones with interbeds of early-diagenetic dolomites and emersion breccia, emersions and occasional bauxites; T–3: Megafacies of peritidal and supratidal carbonates – Main Dolomite (Hauptdolomit). 146 Geologia Croatica 55/2 147Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... in the Lower, Middle and Upper Dogger and Lower Malm of Velebit Mt., Upper Lias/Lower and Middle/ Upper Dogger of Biokovo Mt. and Upper Lias and Lower to Middle Dogger in the Dubrovnik area (Fig. 3; DRAGIČEVIĆ & VELIĆ, 2002). Ooid grainstones and bioclastic–ooid grainstones are also common in Oxfordian strata of western Istria and western Gorski Kotar area (Fig. 4). Deposits of this megafacies are also widely distri- buted in several levels of Jurassic rocks in other parts of the Karst Dinarides, most commonly in Upper Lias–Lower Dogger, Dogger and Malm in general, and Oxfordian and Tithonian. The best outcrops are described from Bosnia and Herzegovina, SE of Kupres (locality 20), Montenegro (see DRAGIČEVIĆ & VELIĆ, 2002 – this Vol.; FARINACCI & RADOIČIĆ, 1964; RADOIČIĆ, 1966; D’ARGENIO et al., 1971), and especially Slovenia (BUSER, 1978, 1979; ORE- HEK & OGORELEC, 1979, 1981; OGORELEC & DOZET, 2000), in different levels of stratigraphic range Middle Lias to Kimmeridgian (DOZET & ŠRIBAR, 1998a), and in some places throughout the Dogger, Oxfordian and Lower Kimmeridgian (STROHMEN- GER & DOZET, 1990; DOZET, 2000). Ooid grainstones were frequently deposited in the form of ooid bars, exhibiting large-scale cross-bedding, but also ooid grainstones or ooid–bioclastic–intraclastic grainstones to rudstones are common as the first member of the shallowing-upward cycles. In this type of parasequences the second member is pelletal or oncoid wackestone or peloid–oncoid floatstone, while the third, upper member of the cycles, is pelletal or oncoid wackestone with fenestral fabric, locally with vadose features (TIŠLJAR & VELIĆ, 1991). Ooid grainstones are composed of well-sorted, spheroidal and frequently broken ooids and mosaic and/ or fibrous calcite cement. Rocks comprise different ooid types: most common are radial, tangential and micritic, although there are also oomoldic, leached and broken and regenerated ooids. Oomoldic and leached ooids are more frequent only within oolitic grainstones of Lower Dogger age in the Dubrovnik area (locality 18b – Osojnik–Grepci profile) and from the Lower Lias on Velebit Mt. (locality 3a – Mali Halan). Their abundance indicates that ooid tidal bars were occasionally exposed to the influence of fresh water, causing complete or partial leaching of their probably originally aragonitic cortex. Ooid grainstones of megafacies J–5 were deposited in environments of ooid shoals and bars with high water-energy. 2.6. Megafacies of skeletal and intraclastic grainstone/rudstones deposited in shallows with agitated water (J–6) Megafacies J–6 consists of bioclastic grainstones and rudstones, and sporadically of floatstones containing well-sorted and rounded intraclasts, bioclasts and coated bioclasts (“cortoids”), 0.5–10 mm in size. Bioclasts of hydrozoans and other stromatoporoids, intraclasts and ooids are predominant, while fragments of corals and gastropods are relatively rare. These rocks are cha- racterised by their high content of drusy mosaic and often fibrous rim calcite cement, and they originated by the destruction of skeletons of reef and patch-reef organisms in open shoals with high water energy and normal marine salinity and by migration and deposition of bioclasts in shoals with agitated water. Deposits of megafacies J–6 (Fig. 4) are common only in the Malm of western and southern Slovenia in the Trnovski Gozd area (locality 5f – TURNŠEK et al., 1981; OGORELEC et al., 1996), and in Croatia in the Pokuplje (locality 21) and Karlovac area (locality 6a), in western Istria (locality 1a – “tidal bar facies” in TIŠLJAR & VELIĆ, 1987), in Oxfordian sediments of western Gorski Kotar area (locality 6d – Platak–Gornje Jelenje), in the Upper Tithonian of Velika Kapela Mt. and Senj–Ogulin profile (locality 6b–c), and in the Oxfordian of Velebit Mt. (Mali Halan – locality 3a) and Biokovo Mt. (locality 11). A variety of megafacies J–6 deposits, composed of well-sorted and rounded intraclasts and bioclasts of pachyodont shells and echinoderms deposited in shallows with agitated water, occur in the Lower and Middle Lias in western Slovenia, in the Middle Lias and Upper Dogger of Velebit Mt. (Mali Halan – locality 3a), while in the Lower Dogger of the Biokovo Mt. (locality 11) skeletal and intraclastic grainstones/rudstones occur (Fig. 3). Deposits of this variety of megafacies J–6 are especially important for the Middle Dogger succession of the Dubrovnik area (localities 18a–c on Fig. 3). 2.7. Megafacies of peri-reefal bioclastic limestones (rudstones and grainstones) with hydrozoan, stromatoporoid and coral patch reefs and biostromes (J–7) Deposits of megafacies J–7 only occur sporadically in typical carbonate platform deposits, usually within the succession of megafacies J–6 in Malm deposits (Figs. 2 & 3). Smaller coral and/or hydrozoan patch-reefs were well developed in the Oxfordian of the Island of Lastovo (locality 19), in the Tithonian of Velika Kapela Mt. and the Senj–Ogulin profile (locality 6b–c) and in the Gorski Kotar (Zlobin area – locality 6f). During the Late Jurassic the northern, NE and SE margins of the platform were characterised by an almost continuous belt of coral–hydrozoan barrier reefs stretching from W Slovenia (TURNŠEK, 1966; TURNŠEK et al., 1981) to SE Montenegro and NW Albania (VELIĆ et al., 2002a). In addition, there were also coral–hydrozoan reefs within the platform interior, where they surrounded intraplatform depressions, e.g. in Gorski Kotar (VELIĆ et al., 1994, 2002b) or the “Lemeš” trough extending approximately from the vicinity of Bihać in W Bosnia (locality 22) towards 146 Geologia Croatica 55/2 147Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... the south to Central Dalmatia, i.e. Knin, Drniš and Sinj (VELIĆ et al., 2002a). Besides this, barrier reefs, extending for tens or hundreds of kilometres, there were also isolated patch reefs, for example near Senj (locality 6b), in Gorski Kotar near Zlobin (locality 6f), in Biokovo (locality 11) in Croatia, as well as in the area of Nanos, Hrušica (localities 5c–d) and Dolenjska (locality 5b) in Slovenia (TURNŠEK, 1997). Most of these reefs were not preserved in situ as skeletal reefs – they occur as smaller or larger quantities of skeletal detritus in the form of peri-reefal bioclastic limestones of a rudstone/grainstone type. Large organic reefs or reef complexes have not been recognized within Jurassic carbonates in the Croa- tian part of the Adriatic Carbonate Platform. Some of these ancient reefs have been completely destroyed and redeposited (TIŠLJAR & VELIĆ, 1991), e.g. there are relics of destroyed reefs in the Upper Malm of the Pokuplje and Karlovac area (localities 21 and 6a), in Gorski Kotar near Zlobin (locality 6f), in the Oxfordian of western Istria (locality 1a), in the Lower Tithonian of Velika Kapela Mt. (locality 6b) and in the Upper Malm of Biokovo Mt. (locality 11). Opinion is divided concerning the stratigraphic posi- tion of reefal/peri-reefal deposits within Upper Jurassic deposits in Slovenia. For example: TURNŠEK et al. (1981), BUSER (1989) and TURNŠEK (1997) consider these deposits to be of Oxfordian–Kimmeridgian age, while NIKLER (1978) considered that they are of Upper Kimmeridgian–Tithonian age, similar to the age of corresponding deposits in Croatia (MILAN, 1965, 1969; NIKLER, 1965, 1969, 1978; BUKOVAC et al., 1974, 1984; VELIĆ, 1977; TIŠLJAR & VELIĆ, 1991; VELIĆ et al., 1994). Reefal/peri-reefal deposits with abundant corals and hydrozoans are very common along the NE margin of the platform in the area from central Bosnia to southern Montenegro, but their stratigraphic age is generally determined as Upper Jurassic (e.g. PAPEŠ, 1972, 1985; VUJNOVIĆ, 1980; MIRKOVIĆ & VUJISIĆ, 1989; MIRKOVIĆ et al., 1977, 1979). 2.8. Megafacies of “limestones with cherts” (including “Lemeš deposits”), deposited within intraplatform troughs with temporary or continuous connection to the open sea (J–8) Megafacies J–8 comprises “limestones with cherts”, and it is especially well developed in the Kimmeridgian of Velika Kapela Mt., in the area of Karlovac (Fig. 2) and within the so-called “Lemeš beds” which can be found in the central part of the platform from Bihać in NW Bosnia, along the Una valley, through E Lika (Donji Lapac, Udbina) and N Dalmatia (Knin, Drniš) to central Dalmatia (Sinj) (Fig. 7 in VELIĆ et al., 2002a). Comparable deposits are completely missing in the coastal area and on the islands of the central and southern Adriatic (TIŠLJAR & VELIĆ, 1991). “Limestones with cherts” deposited within an intra- platform trough in the area of the present day Velika Kapela Mt. (locality 6b–c) had only weak, temporary connections with the open sea. On the contrary, for deposits of the so-called “Lemeš beds” a continuous and direct connection with the open Tethys is supposed. “Limestones with cherts” have also been found in Slovenia, where according to BUSER (1989) in the region of Trnovski Gozd (locality 5f) they were accu- mulated somewhat earlier, during the Oxfordian, in a deeper trench formed within the platform, which was connected towards the north with the Slovenian Basin. In the area of Velika Kapela Mt. and the Senj–Ogu- lin profile (locality 6b–c, Fig. 2) thin- to well-bedded grey to dark grey mudstones/wackestones with inter- beds of cherts gradually overlaid Oxfordian deposits of megafacies J–2. Their thickness is very variable, and their upper boundary is also gradual with redeposited bioclastic limestones of megafacies J–5 (Fig. 2). In their lower part “limestones with cherts” are com- posed of grey to dark grey pelletal–bioclastic wacke- stones and mudstones with nodules and rare lenses of cherts. In their upper part within the well-bedded rocks of similar lithology, but including small peloids, oncoids, pelagic crinoids, bioclasts of echinoderms, corals, hydrozoans and stromatoporoids, rare ooids and very rare ammonites, there are lot of nodules, lenses and intercalations of cherts. Cherts comprise numerous relics of radiolarians and spicules of silica sponges. They originated by early- diagenetic silicification of carbonate muds under the influence of solutions enriched in silicic acid origina- ting from fine volcanoclastic detritus, and some beds are direct products of the alteration of tuffs, as first mentioned by ŠĆAVNIČAR & NIKLER (1976). “Lemeš beds” were described as platy to thick- bedded limestones with interbeds and lenses of cherts and/or thin-bedded silicified limestones (IVANOVIĆ et al., 1977, 1978; KRKALO et al., 1995). Limestones are mostly pale brown fossiliferous mudstones to wackestones, but also wackestones to packstones comprising pellets, ooids, oncoids and bioclasts. They contain relatively numerous ammonites, aptichuses, fish remains, brachiopods, benthic and pelagic foraminifera, calcisphaeres and radiolarians. According to KRKALO et al. (1995) “Lemeš beds” at a typical locality in Svilaja Mt. (Lemeš, Maovice – locality 23) within the continuous succes- sion of Upper Jurassic deposits overlie dark grey Oxfordian limestones (probably representing deposits of megafacies J–2). In their basal part there is an alter- nation of platy and thin-bedded limestones (beds up to 20 cm thick) with chert lenses and nodules (cm- to dm-thick). Limestones predominate, but the proportion of cherts increases upwards. Interbeds and lenses of montmorillonitic clays containing volcanic glass and pyroclastic quartz have been determined. In the central part of the succession thin bedded siliceous sedi- ments prevail – silicified carbonates (predominantly mudstones) and 5–10 cm thick cherts with relics of ammonites and bivalves, characterised by occurrences 148 Geologia Croatica 55/2 149Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... 1a W&S ISTRIA ~ i Ii: w 0- w i 2b l OFFSHORE ~ WELL IM-1 i ., ~ ::> 0 w ~ I-' W '" 0 I '" ~ w .. F ~ .. ::> ~ I ~ 0 ., ::> 0 w i 0 ~ " w l '" 0 ~ .nergy sl10als ana bars ~, ~ ::I. m i!l: trough g~ .,0 :i"i ~q~~HI ~ t rTi I'Tn C;~ , f------I~ VI~h--Hf'I\ ~ ~~~/ -8--T-l-r-~----~ ---~-I-rl-~-"""-'-' ~ ~t rr rNncalily 6c P . P~ II~ LatE>- II diagen.etic t dolOmites ~ ~ I ~ I@I ~~ I ~ I I ~ I I ~l;J I I II ~ ~ 13.BI 6.B I 5.71 9.5 3.61 7.3 14.B 15.0 15.313.41 B.B 15.414.515.0 I B.O I B.B 13.3 5.414.513.2~.3 12.2 I 6.3 I 10.1 ~~-~~---~~(---~>-I~----~-~--~~--~- 25.B m.y. 20.7 m.y. 17.5 m.y. 43.0 m.y. 33.9 m.y. B3.B m.y. 77.0 m.y. 3. ~- • 160 Geologia Croatica 55/2 161Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... panian or Maastrichtian to the Eocene in the entire coastal area and Adriatic islands, as well as in western Herzegovina. In Istria there are some localities with stratigraphic hiatus from the Valanginian, Hauterivian, Barremian or Albian to the Eocene. The opposite situation is recorded in periods characterised by eustatic sea-level rise resulting in establishment of drowned platform environments (megafacies K–7), e.g. near the Cenomanian/Turonian boundary or from the Late Turonian–Santonian to the earliest Campanian. However, both the aforementioned regionally important phases of emersion and platform drowning had different consequences on different parts of the Adriatic Carbonate Platform, since the regional or glo- bal eustatic signal was significantly corrected by local factors, especially synsedimentary tectonics. Although the influence of synsedimentary tectonics on the carbonate platform is rarely clearly visible, espe- cially because of the high organic production enabling fast infilling of any available accommodation space, its understanding is essential for the correct interpretation of the geological history of the platform. By careful examination of different penecontemporaneous succes- sions it is possible to extract the tectonic signal resulting in the formation of environments which otherwise would not be possible. A very good example of the influence of synsedi- mentary tectonics can be seen in the Upper Jurassic successions in different parts of the karst Dinarides. The Latest Oxfordian (or earliest Kimmeridgian) was, in the area of present Istria (locality 1a on Fig. 1), characterised by the beginning of the long-lasting emersion – shallow-marine deposition recurred in the Late Tithonian, i.e. practically the complete Kimme- ridgian and Lower Tithonian deposits are missing. At Biokovo Mt. (locality 11) there are two emersions: from the Early Oxfordian to the Early Kimmeridgian and from the Late Kimmeridgian to the Middle Tithonian, divided by a relatively thin sequence of Kimmeridgian deposits (TIŠLJAR & VELIĆ, 1991). In the same period the western part of the Gorski Kotar area (Platak–Gornje Jelenje and Zlobin – loca- lities 6d and 6f) was characterised by continuous shal- low-water sedimentation, while in its eastern part (Velika Kapela Mt. and Senj–Ogulin area, localities 6b–c) an intraplatform trough was formed. It was chara- cterised by deposition of limestones with cherts (mega- facies J–8 – see VELIĆ et al., 2002b for more informa- tion). Somewhat deeper marine environments in this area prevailed only temporarily – intense progradation of calcitic detritus (ooids, intraclasts, and especially peri-reefal bioclasts) from marginal areas gradually fil- led in the sedimentary basin, resulting in the final reco- very of shallow-water deposition in Tithonian (mega- facies J–5, J–6, J–7 and J–2). Along the northern margin the Kimmeridgian was characterised by a transgression over an area emergent for a long period (emersion started in the Middle Lias). Such variability in the sedimentary record definitely cannot be interpreted without the important influence of local synsedimentary tectonics. Namely, the Oxfordian deposits are more or less similar throughout the area, while during the Kimmeridgian completely different environments were formed. Some parts were affected by emersion, in others shallow-marine deposition continued, some parts were characterised by deepening and an open marine influence, while in others transgres- sion over areas which had been exposed for a long time was recorded. Tithonian successions are again similar throughout the area, represented mostly by shallow- water algal limestones. An interesting example of the influence of extensive organic production on a carbonate platform is provided by a study of Late Cretaceous environments colonized by flourishing rudist communities. According to their ecological preferences, different rudist types usually accompanied by different molluscs (mostly chondro- donts and nerineids) occupied a wide range of different environments, from the inner, restricted parts of the platform, shallows with agitated water, somewhat deeper lagoons and inner parts of the platform margins. Their carbonate production was very high, and the material produced by disintegration of their skeletons by bioerosion and mechanical processes represented an important part of the total carbonate production in the Late Cretaceous. This material was reworked and continuously removed to other areas by waves and currents, enabling infilling of former smaller or larger depressions and the formation of a variable sea-bottom morphology by different mechanisms, e.g. migration of subaqueous dunes, but also transportation to far distances by turbidity currents. In this way organic pro- duction interacted with the environment, since it was influenced by its environment, but also the environment was significantly changed by organic production. The very complex vertical and lateral alternation of different megafacies units therefore indicate the significant palaeogeographical dynamics of the Karst Dinarides. This variability resulted from the interaction of a global eustatic signal and local factors, first of all extensive organic production on carbonate platform and synsedimentary tectonics controlled by the specific palaeogeographic position of the platform during its geological history. Acknowledgement The authors are sincerely grateful to the reviewers, Dr. Bojan OGORELEC and Dr. Bogdan JURKOVŠEK (Geological Survey of Slovenia) for their numerous comments and useful suggestions, especially concer- ning data on the Slovenian part of the Adriatic Carbo- nate Platform. 162 Geologia Croatica 55/2 163Tišljar, Vlahović, Velić & Sokač: Carbonate Platform Megafacies of the Jurassic and Cretaceous Deposits... 7. REFERENCES AHAC, A., PAPEŠ, J. & RAIĆ, V. (1977): Osnovna geološka karta SFRJ 1:100.000. List Glamoč L33–142 (Basic Geologic Map of SFRY 1:100.000 – the Glamoč sheet).– Geološki zavod Sarajevo (1963–1965), Savezni geol. zavod Beograd. ANTONIJEVIĆ, R., PAVIĆ, A. & KAROVIĆ, J. (1969): Osnovna geološka karta SFRJ 1:100.000. List Kotor K34–50 (Basic Geologic Map of SFRY 1:100.000 – the Kotor sheet).– Zavod za geol. geofiz. istraž. Beograd (1962–1969), Savezni geol. zavod, Beograd. BABIĆ, Lj. & ZUPANIČ, J. 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