2017 | 70/1 | 11–25 | 5 Figs. | 2 Pls. | www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society

Early evolution of carbonate depositional environments recorded in the Čikola Canyon (North Dalmatian Foreland Basin, Croatia) Jelena Španiček1, Vlasta Ćosović1, Ervin Mrinjek1 and Igor Vlahović2

1 University of Zagreb, Faculty of Science, Department of Geology, Horvatovac 102a, HR-10000 Zagreb, Croatia; (corresponding author: [email protected]) 2 University of Zagreb, Faculty of Mining, Geology and Petroleum Engineering, Department of Geology and Geological Engineering, Pierottijeva 6, HR-10000 Zagreb, Croatia doi: 10.4154/gc.2017.05

Abstract Article history: The stratigraphic succession in the Čikola Canyon (part of the North Dalmatian Foreland Basin) Manuscript received November 08, 2016 was studied in detail to describe both the sedimentological characteristics and fossil assem- Revised manuscript accepted February 25, 2017 blages of the Lower Eocene deposits during the initial stage of the foreland basin formation. Available online February 28, 2017 The North Dalmatian Basin now represents a part of the Outer Dinarides, and was developed in front of the evolving Dinaric structures by tectonic deformation and marine transgression of an emerged and denuded Mesozoic Adriatic Carbonate Platform (AdCP). During the initial phase, a distal ramp of a foreland basin was formed, characterised by carbonate sedimenta- tion, lasting until the Middle Eocene. In a studied section more than 300 m thick, porcelaneous foraminifera, Alveolina, Orbitolites and complex miliolids (Idalina, Periloculina) prevail, associated with conical agglutinated forms, nummulitids and red algae. These samples belong to the SBZ 11–12 (Ypresian), according to occurrences of Alveolina decastroi, Alveolina cremae, Alveolina multicanalifera and Coskino- lina liburnica. Two main lithological units have been described: 1) mudstones to wackestones with sporadic occurrences of ostracods and charophyceae, deposited in restricted lagoonal settings with several episodes of freshwater influences, and 2) foraminiferal packstones to grain- stones with complex miliolids, alveolinids, corallinacean algae and nummulitids, deposited with- in inner and middle ramp settings. Palaeogene deposition of ramp carbonates in the Outer Dinarides area was mainly controlled by the continuous compressional tectonics, and the deposits today appear in more or less dis- continuous outcrops. Palaeogene transgression occurred at different times over various parts Keywords: Larger Benthic Foraminifera, microfacies, palaeoenvironment, Foraminiferal of the former carbonate platform area, and subsequent carbonate sedimentation was charac- limestones, North Dalmatian Foreland Basin, terised by deposition in similar environments during different time intervals over spatially restrict- Lower Eocene ed carbonate ramps controlled by synsedimentary tectonics.

1. INTRODUCTION locally within restricted lagoons are marked by a shift from fresh- The aim of this study was primarily to determine the microfacies and brackish-water environments to a fully marine regime in the properties of the Čikola river canyon carbonate deposits rich in area. During the Eocene the shallow-marine (neritic) carbonate Larger Benthic Foraminifera (LBF). These determined forami­ succession rich in LBF, known as the Foraminiferal limestones, niferal assemblages and their ecological requirements combined was deposited within carbonate ramp environments (DROBNE et al., 1991; BABIĆ & ZUPANIČ, 2016 with references therein) with the study of other carbonate-producing biota (corals, bryo­ over either the Kozina beds or directly onto karstified zoans, echinoids, molluscs, coralline red algae), enabled the defi- deposits. The ramp deposits pass upward into glauconite-bearing nition of the palaeoenvironmental settings of the Lower Eocene marly Transitional beds, overlain in some areas by a turbiditic deposits known as the Foraminiferal limestones. succession of flysch and/or by a thick succession of Promina beds The studied section is located in the Outer Dinarides, the unit (MRINJEK et al., 2012). being composed mainly of carbonate rocks, ranging in age from The most important characteristic of the studied Palaeogene the Upper to the Eocene (VLAHOVIĆ et al., carbonate deposits are the abundance and diversity of the LBF. 2005). The studied deposits belong to the more or less continu­ They are an endosymbiont-bearing (LEE, 1998; HALLOCK, ous Palaeogene belt oriented NW−SE along the NE Adriatic coast 1999, and references therein), highly diversified and specialized (ĆOSOVIĆ et al., 2008a) (Fig. 1), i.e. to the North Dalmatian group of organisms with specific environmental preferences re­ Foreland Basin (BABIĆ & ZUPANIČ, 1983, 2007, 2012; MRI- garding temperature, salinity, water energy, light intensity, and NJEK et al., 2012). substrate type, numerous in the photic zone of oligotrophic tropi- The Lower Palaeogene carbonate succession in the area is cal and subtropical seas (HOTTINGER, 1983, 1997; BOUD­ underlain by karstified Upper Cretaceous rocks (subaerial expo­ AGHER-FADEL, 2008). This makes them, apart from being ma­ sure commenced during the Campanian; MAMUŽIĆ, 1975). The jor carbonate producers, excellent shallow-water environmental/ Kozina beds, the oldest Palaeogene deposits, which originated palaeoenvironmental indicators (HOTTINGER, 1983, 1997; HO­ Geologia Croatica LBF, the Foraminiferal limestones in the Outer Dinarides are are Dinarides Outer the in limestones Foraminiferal LBF, the Based conditions. on bottom of groupsthe abundance specific of salinity, light andcificenergyconditions, watersea- temperature, 2004, 2005), HENEGGER, because their presence spe indicates and Lower Eocene Foraminiferal limestones, whichare conformably overlain by thePromina MRINJEKetal., beds(modified after 2012). NJEK etal., Late panoramic 2012),and(C) viewofthestudiedČikolaCretaceous section. rudistlimestones are unconformably overlain by thestudiedKozina Beds geological columns from Fig. 5,(B)geological map(modifiedafter MAMUŽIĆ, 1971;IVANOVIĆ etal., 1973,1977; ĆOSOVIĆ etal., etal., 2008a;DROBNE 2011;MRI­ Figure 1.(A) Simplifiedlocation mapofthe after (modified Palaeogene depositsintheDinarides ĆOSOVIĆet DROBNE et al., 2008a; of al., 2011)withthelocation 12 ­ ronmental conditions, and their spatial and temporal distribution and conditions, spatial and their distribution ronmental temporal palaeoenvi different under of Deposits originated member each limestones. orthophragminid and/or nummulitid-, alveolinid-, miliolid-, members: separate into subdivided informally often Geologia Croatica 70/1 ­ Geologia Croatica ­ ­ ­ ­ ­ ­ ­ - ­ ­ ­ ­ ­ ­ ­ ­ ­ 13 was 2 sp. sp. aggregates in over Microcodium Microcodium ed, and each grain within a grid was counted. From there, The S1 The unitS1 transgressively overlies massive light-coloured Carbonate microfacies were distinguished according to The oldest Palaeogene deposits, stratigraphic unit S1, are are S1, unit stratigraphic deposits, Palaeogene oldest The stratigraphicoverlying thepart consistsof Thelower unit S2 4. RESULTS 4.1. Stratigraphy of the Čikola section 2) 1, (Figs. section studied Čikola the indeposits Palaeogene The dividedbe may into twostratigraphic thenand S2, fur units, S1 ther subdivided into five sub-units (S1a, S1b, S2a, S2b and S2c), S2c), and S2b S2a, S1b, (S1a, sub-units five into subdivided ther foraminifera)(mainlycontent sedimentheirand basedfossil on tary textures. Upper Cretaceous rudist-bearing limestones. The non-deposi tional phase between the Upper Cretaceous and Palaeogene de studied the in since field, the in recognizable easily not is posits angular representedvisible any not unconformity isby section it not karstification even is infillingscontinental deposits, and of or clearly visible everywhere. The detailed studies thinof sections reveal a reduction of fossils towards the youngest Cretaceous rocks, and the presence of scriptions of identified microfacies, tosimplify the results, esti particular grainof typespresentedsemi-quan are volumes mated titatively by four subgroups: ‘no grains’, ‘rare grains’ (volume less than 15 ‘common %), grains’ to (15 49 and%), palaeoenviron ‘abundant the of typesforaminimicrofaciesandThe %). 50 over grains’(volume interpretation enabled assemblages feral mental al., conditions et the of studied deposits similar to existing ZAMAGNI car 2005; bonate-ramp BOSENCE, 2005; models& WRIGHT, GEEL,1992; 2000; POMAR, et ROMERO 2001; BASSI, (BUXTON 2002; &al., PEDLEY, 1989; BURCHETTE2008; TOMASSETTI et al., 2016). POMAR’s (2001)of subdivision shallow-water carbonatephotic ones was also applied. environments from euphotic to oligo mark an estimated volume of a given grain type proportional to the counted numbers of a particular grain type was calculated. In de 1960; 1960; DROBNE, miliolids1977), and 1985), (DROBNE, 1974, agglutinated conical foraminifera (HOTTINGER & DROBNE, VECCHIO & HOTTINGER,1980; 2007). DUNHAM’s classification (1962) modified by EMBRY For & the microfacies analysis(1971). KLOVAN the methods of were applied.and WILSON InFLÜGEL (2010) (1975) order to study environmental conditions, the visual examination and semi-quantitative analysis grainof lithology, types (biogenic or texturesabiogenic), and fossil assemblages was performed. The thinmodaldistributioncomponentsinestimatedsections was of by using a point-counting method (FLÜGEL,On 2010). each examined thin section, a two-dimensional grid of 1 cm lying beds, which are typical for the early stages of palaeosol de palaeosol of stagesearly the typical arefor beds, lyingwhich sections (KOŠIR, 2004). in manyvelopment Peri-Tethyan pack wackestonestowell-beddedalternation an of composedof beginthe thin-bedded At andwackestones.stones mudstonesto thin-beddedsuccession,the a limestones intercalatedningof are with a few cm thick coal layers. The lower part of unit,S1 the S1a, is characterised by a specificrophyceae and ostracods), while in the unit,fossilupper, S1b the de content (gastropods,creasingabundanceostracods of gastropodsand therelatedto is cha increasing abundance small of miliolids and discorbids. of well-bedded foraminiferal wackestones to packstones with a appearancecharacterisesmassive a whereasassemblage, LBF rich deposits in the upper part the of unit. In the lowermost part – the ­ ­ ­ ­ ­ ­ ­ ­ - ­ - - ­ ­ - ­ ­ ­ ­ Over 300 samples were collected for microfacies and microand microfacies for collected were samples 300 Over Ourresults could shed additional light on the deposition of Depositionduringsignificantlywas Palaeogenecontrolthe LBF assemblages were investigated in thininvestigatedinsectionsorder were inassemblages LBF tificationof foraminiferal testswas based on random thin 3. MATERIALS AND METHODS AND MATERIALS 3. road-cutwell-exposed along the inlocated studiedis sectionThe the local road passing intervals sampled last first and the across coordinatesgeographic Theof the Čikola river canyonare 43°50’8.9” (Fig. 1B, C). N, 16°2’49.3”E and 43°50’20.4”N, 16°2’58.2”E, re spectively. The section encompassescession which was measured and sampled in detail to document a 310 m thick carbonatebothsedimentologicalthe characteristics assemblages fossil and suc (Fig. 2). 2. GEOLOGICAL SETTING AND STRATIGRAPHY DalmatianNorth theForeland studiedrepresentsarea partTheof Basin developed in front of the evolving Dinaric structures by tectonic deformation and marine transgression anemerged of and During AdriaticCarbonate(AdCP). Mesozoic Platform denuded foredeep a distalpart of a asformed wasramp initiala phase,the in the Dinaric foreland basin system, and carbonate sedimenta the Foraminiferal limestones, and provide more data about the evolution of the Northern Dalmatian Foreland Basin during the evo thepicturecompleting inthe data willof Eocene.help New the lution sedimentaryof Eocene (neritic) shallow-water system of the Outer Dinarides, includingical terminology. a discussion of palaeogeograph tion existed on a flankof a broadforebulge until the Middle Eo 2008,cene & ZUPANIČ, (BABIĆ 2012). suggests an overall deepening of the sedimentarythe deepening settingsoverallof duringansuggests the Early Eocene and earlyMiddle Eocene. Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... led by tectonic deformation caused by the propagation of the Dithetectonic propagation theby of deformation causedled by naric orogeny towards Thethe PalaeogeneSW. shallow-marine carbonate(ĆOSO rampa carbonatesdepositedon were (neritic) VIĆ et al., 2008a), named the Palaeogeneupward The Adriatic Carbonate 2011). (2009, al. et DROBNE by (PgAdCP) Platform succesthick m 220 a carbonateproducedrampthe deepening of studiedregion. thecarbonates in of 1976) al., et (IVANOVIĆ sion The succession is composed palustrine of and marginal marine neri by overlain bedsKozina the carbonates,as referredtooften tic deposits known as the Foraminiferal limestones general (for turbi and overview 2008a) see VLAHOVIĆ al., et & VELIĆ, 2009). Deposition of the (ĆOSOVIĆ beds Transitional overlying ditic deposits started(flysch) when ramp carbonate production was unable to keep pace with subsidence. The subsequent shal pig small the inenvironmentsrecordeddepositional is of lowing gyback sub-basins within the Promina basin (KORBAR 2009; MRINJEK etwhere al., the 2012), succession of Promina beds (SCHUBERT, 1904, 2012; 1908; MAMUŽIĆ,deposi ZUPANIČ, were 1971; age IVANOVIĆ & OligoceneEocene Middletothe of 1977) et al.,1973, (BABIĆ m 2000 to up of thickness in ted MRINJEK 2012). et al., palaeontological studymicro 12 of total analysed.A typesmicrofaciesvariouswere and ing more than 270 thin sectionsfacies types have been representdefined based on LBF assemblages and sedimentary textures. to determine the age theof deposits, applying the Shallow Ben thic Zones of (SBZs) SERRA-KIEL et al. Taxonomic (1998). iden level species identification to allowed,sections when andsections was done, using key literature for alveolinids (HOTTINGER, Geologia Croatica 14 in theČikola Canyon, Dalmatia (MRINJEKetal., 2012) (right). Northern within ageneralized stratigraphic andpositionofthestudiedsection microfacies MFT1to MFT12(left), types column oftheUpper Cretaceous–Eocene succession Figure 2.Studied stratigraphic showing column thelithology, oftheČikola section identified biozones SERRA (SBZ after ­ KIEL et al., 1998) and distribution of the KIEL etal., ofthe 1998)anddistribution Geologia Croatica 70/1 Geologia Croatica

. - ­ - - ­ ­ ­ ­ ­ - ­ 15 ed sp., and (SILVE Coskino­ Quinque arniolica

cf. c sp., and Idalina Triloculina sp., Periloculina dalmatinaPeriloculina Pyrgo Cribrobulimina (VAN SOEST) and(VAN sp., Triloculina Pseudochrysalidina alva sp., , makarskae

sp., Pyrgo sp., and ostracods (Pl. 1, Fig. 4). Small, Spirolina According to HOTTINGER1997), (1983, The sedimentological and palaeontological Sedimentological and palaeontological cha palaeontological Sedimentologicaland carniolica sp., (STACHE). Other (STACHE). common benthic foraminifera sp., Spirolina Pfendericonus cf. sinjarica, as well as the rare to common presence of Cribrobulimina This microfacies occurs in the stratigraphic unit of S2b the Interpretation: Interpretation: This microfacies occurs in the first30 mof theČikola sec Interpretation: dominantmicro a is 3, MFTwith together microfacies,This teristics proportion (the smaller of and larger miliolids and lina liburnica are alveolinids and miliolids (including agglutinatednical sea-bottomforaminiferamuddy soft occupied at depths just below the tidal Thus,level. this microfacies is in terpretedashaving been deposited inthe protected, low-energy, shallowest parts the innermost of ramp. Čikola section. The first occurrence is at around 80 m andit is present almost until the the end section of 2). (Fig. DROBNE; Pl. 1, Fig. 5). Fig. 1, Pl. DROBNE; VECCHIO & HOTTINGER (2007) and AFZAL et al. (2011) co STRI), rac agglutinated conical foraminifera – GEEL, 2000; etROMERO 2011) al., AFZALet HOTTINGER,2007, & VECCHIO 2002; al., of the MFT 6 microfacies suggests deposition in low- to mo derate-energy environments the inner of ramp. tion (S1a stratigraphicaltion (S1a unit) and contains eight coal intercala tions, each cms a few in thickness 2). (Fig. 4.2.5. MFT 5 – Conical agglutinated foraminiferal packstone The main characteristic ofof conical MFT agglutinated 5foraminifera is the (Pl. Pl. 5; 6): Fig. 1, Fig. 1, abundance and diversityCribrobulimina cf. 4.2.4. MFT 4 – Bioturbated miliolid mudstone to 4 – Bioturbated miliolid 4.2.4. MFT wackestone MFT 4 consists of mudstones to wackestones. The micritic ma recrystallized,partlyfilledlocallyaretrix is numerousvoids and with micrite (due to intenseare rare to common, bioturbation) represented mostly by foraminifera such as and/or( miliolidscommon todiscorbids,rare abundantof tests sparite. Bioclasts loculina 4.2.6. MFT 6 – Miliolid wackestone to packstone The dominant lithology within MFT 6 are fine-grainedwacke Idalina agglutinatedforaminifera,conical stones to packstones 7), in (Pl. Fig. 1, which the micritic matrix is occasionally partially recrystallized. This microfacies is cha­ miliolids: complex andsmall both abundance of racterisedthe by Quinqueloculina sp.), thick,engulfed in and sparitic cement with filled mm-sized voids micritic coatings, have spherical, subspherical and/or tubular patternapparentany without together, clusteredoften are shapes, with similar orientation.or form anddimensionsVoids becould interpreted as tubular 2010). FLÜGEL, fenestral (cf. voids features imply depositionmarine environment, in where small a epiphytic very foraminifera (small shallow, low-energy, miliolids) and discorbids thrived. Occurrences restrict of agglutinated nutrient-rich protected,foraminifera,relatively conicalto related supportenvironmentalthis2000) environments lagoonal (GEEL, interpretation. facies in the lower 45 m of the Čikola section, but throughout it occursthe entire Čikola section, especially in stratigraphic section the 2). Čikola m of (Fig. units to the and 175 S2a S2b

­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ D. Stromatop Microcodium sp. In the upper sp.) occurred. A A occurred. sp.) Decastronema bara­ Orbitolites Microcodium The presence charophyceae of and gastro Carbonates of the MFT 1 microfacies were The low-diversity fossil assemblage composed sp.) and common charophyceae. sp.) The gastro Cosinia , known as a pioneeringorganismmodifyinga knowninas , envi the (DE CASTRO) cyanobacterialcharophy rare filaments and CASTRO) (DE Interpretation: Interpretation: This microfacies overlays the Upper Cretaceousrudist-bearUpper the overlays microfaciesThis Interpretation: This microfacies is typical for the basal part of the Čikola sp. and sp. 2a unit – miliolids dominate, while the middle part (the S2b unit) S2b part(the middle the dominate,miliolidswhile – unit 2a pods indicate a freshwater influence, thus deposition probably took place in a brackish environment, whereas the micritic ma trix suggests turbulence a low environment. MFT 3 is represented by wackestones to packstones (Pl. Fig. 1, particles Skeletal comprise abundant gastropods3). ( 4.2.3. MFT 3 – Dolomitized gastropod wackestone to packstone sis pod shells are often compressed, fragmented, and intraskeletal Fine- infilledfine-grainedpackstone. areby pores to wackestone grained micritic matrix is often recrystallized, with common to abundant dolomite crystals scattered in the matrix or within in terparticle cement. 4.2.2. MFT 2 – Ostracod mudstone to wackestone 4.2.2. MFT 2 – Ostracod mudstone to MFT 2 consists of mudstones to wackestones containing com mon to abundant ostracod shells, common ttoloi sp. clusters (Pl. 1, Fig. 1). Fig. clusterssp. (Pl. 1, sub of episodesinnersetting,rampwhere shallow, a indeposited mon scattered dolomite crystals, and locally visible visible crystals,locallyscattered anddolomite mon aerial exposure (as indicated by characterisedfossils innersupratidalwithinconditions anof lack ramp setting. 4.2.1. MFT 1 – Non-fossiliferous mudstone to wackestone 4.2.1. MFT 1 – Non-fossiliferous mudstone Microfacies MFT 1 is composed mudstonesof characterised by a lack of fossils, more or less intense recrystallization, often com 4.2. Facies association and microfacies types 4.2. Facies association foraminiferal of asRegardingcompositionandassemblagesthe glutinated conical foraminifera and part the of unit, massive coarse-grained S2c, foraminiferal pack stones occur with lenticular-shaped nummulites, fragments of zooaxanthellate coralsand corallinacean (z-corals) red algae (in cluding small and rare rhodoliths) orthophragminids. The top of the sectionČikola is conformably overlain by massive mudstone bedswiththin streaks, normal-graded interlaminae lensesand of silt or very fine-grained sand, interpreted as initial fine-grained subneritic deposits the Promina of beds (MRINJEK 2012). et al., sociated biota as well as sedimentary textures, the studied suc cession has been divided into twelve microfacies types, MFT 1 2). to MFT (Fig. 12 S has a diverse foraminiferal assemblage: miliolids, alveolinids, ag Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... of of thin-shelled ostracods, charophyceans and cyanobacteria sug ceae (Pl. Samples Fig. 2). 1, with abundant ostracods often show lamination. gests episodic fresh-water influxes. The common presenceof barattoloi ing limestones, and represents initial deposition over a regional unconformity (Cretaceous to Palaeogene stratigraphic hiatus). ronments to become more suitable for other organisms (ĆOSOVIĆ organismsother (ĆOSOVIĆ for suitableronments morebecome to interpretation.ansupports describedsuch These con 2008b), al., et ditions are typical protected low-energy, of brackish lagoons. stratigraphic section,unit,the S1a representing Palae theoldest depositsogene in the studied area 2). (Fig. Geologia Croatica aborescent aborescent sionally alveolinid tests are oriented, fragmented and abraded. abraded. and fragmented oriented, are tests alveolinid sionally Fig. 3). 2, (Pl. Occa fragments mollusc micritized and rotaliids, 9 MFT of bioclasts consists of well-sorted alveolinids, miliolids, 4.2.9. MFT9–Foraminiferal grainstone 120 m (Fig. from 2). starting Čikola section, GEEL, 2000; MATEU-VICENS et al., 2010; et POMAR al.,1993; (LANGER, 2014). influence marine open possible with settings photic the within conditions, shallow lagoon marine or ramp inner eu thus and covers, algal or sea-grass of occurrences probable circula restricted to 2010). moderate The abundance with of rotaliidstion (WILSON, environments and small 1975; miliolids intertidal TUCKER to indicatesdal & WRIGHT, 1990; FLÜGEL, fora well are remains are common. Skeletal and fragments bioeroded, and echinoderm which Porcelaneous are foraminifera, mostly minifera. deformed rotaliid fora skeletal Dominant allochems are trix. recrystallized ma micritic surrounding the from them distinguish to it hard is (sparitic trix matrix) occur, and where peloids are densely packed, ma recrystallized partially and matrix micritic the distributed, sparsely are peloids Where recrystallization. partial shows lly occasiona matrix micritic Fine-grained tests. foraminiferal and rounded, to irregular shapes, and sizes Fig.2) varying 2, of (Pl. peloids dominant with bypackstones represented is 8 MFT The 4.2.8. MFT8–Peloidal-foraminiferalpackstone 2). (Fig. of section end the the until almost continuously it present is and around 70 m is recorded occurrence Čikolathe first The section. 1983).(causing ‘deformed’ –HOTTINGER, tests orbitolitid pools tidal in observed as salinity, and/or temperature creased al., 2016), by short-lived occasional ofepisodes characterised in GEEL, 2000; BRANDANO1983,1997; (HOTTINGER, settings et lagoonal al., protected typical 2009a, b; TOMASSETTI et veolinids and miliolids are interpreted as having originated in Cribrobulimina rotaliids,of tests rarerare include bioclasts 1983)8).Fig.Other 1, to GER, (Pl. abundant agglutinated(HOTTIN conditions ‘extreme’of indicative are disks) dicular conical perpen foraminifera,additional ‘deformed’ (forms some with tests orbitolitid of occurrences The missing. are whorls final the cases, some in and bioerosion, of marks bear tests foraminiferal The common. Pyrgo GER, -RISPOLI, decastroi veolina and miliolids: alveolinids mainly foraminifera, porcelaneous of abundance an by characterised is microfacies Fig.1). 2, This 1,(Pl. Fig. 8;Pl. matrix (rarelycoarse-grained) micritic grained MFT 7 is represented by poorly-sorted4.2.7. MFT7– Alveolinid-miliolid packstone packstones with a fine- (Fig. 2). (Fig. S2a), and continues up S2 unit subunit (within to of stratigraphic the at prevails the beginning 110 m markS1b, unit but in thestratigraphic the Čikolawithin section Čikola the of base section 16 minifera are compacted. are minifera This microfacies occurs in the stratigraphic unit S2b of the the S2bof unit stratigraphic the in occurs microfacies This Interpretation: S2b unit microfacies This is in the dominant ofstratigraphic Interpretation: This microfacies occurs for time atmicrofacies occurs the This first c. 35from mthe Idalina LAMARCK tests are also are tests LAMARCK complanatus Orbitolites sp. Haddonia A. multicanalifera A. cf. s cf. sp., and and sp., SCOTTO DI CARLO, CARLO, DI SCOTTO ­ injarica sorted and some of the agglutinated conical conical of agglutinated some the and sorted Peloids are common in recent shallow subti shallow recent in common are Peloids Sea-grass influenced associations rich associations in influenced al Sea-grass sp., and fragments of echinoderms. sp., fragments and Pseudochrysalidina alva , Spirolina DROBNE, DROBNE, sp., Quinqueloculina sp., A. cremae A. levantina (SILVESTR I), I), (SILVESTR CHECCHIA HOTTIN sp. and and sp. Al - ­ ­ ­ ­ - ­ ­ - ­ - ­ ­ ­ tion within stratigraphic unit S2b (Fig. unit 2). stratigraphic within tion miliolids, and planktonic foraminifera are rare. are foraminifera planktonic and miliolids, magna nella energy to rework bioclasts and produce skeletal packstones. skeletal produce and rework bioclasts to energy 2012). In such settings,corals lived zone, the mesophotic the and highin grewthat known is along hydrodynamicsIt corals. as withquirements red algae (MORSILLI providedre environmental etsame the follow al., thetherefore and 2003) ZONI, microhabitats; BOSELLINI & PAPAZand semi-cryptic cryptic (occupying corals with associated are foraminifera encrusting The LBFs, and conditions. mesophotic such z-corals suggests as of mixotrophs, The a co-occurrences environment. higher-energy Neorotalia particular, (in clasts goons (HOTTINGER, 1974; al., et 2006). (HOTTINGER, goons TORRICELLI la hypersaline occasionally and, marine normal in abundant are alveolinids) and (miliolids foraminifera porcelaneous rally, Gene shoals. ramp inner on deposition probable their indicate grains well-sorted and tests alveolinid Abraded 2000).(GEEL, base wave fair-weather below and near shoals sand also, but, ramp (including settings) inner protected environments protected shallow-water, inhabited They substrates. of kinds all on lived have could they although substrates, sea-grass or algal ferred ment, under the ofinfluence wavesAlveolinidspre and currents. kola section. shoals. on deposited were microfacies this of rocks that suggests mm 8 than larger tests of prevalence The 2006). al., et (TORRICELLI shoals nearshore in frequent of Specimens 2000). GEEL, and the within platform interior, Small- and can form (AIGNER, banks 1983; 2005). environments various in lived forms lenticular HOHENEGGER, medium-sized (≥30m; depths oligophotic to mesophotic at dominant are but m, 30 than less depths at found be can and dwellers, bottom are Nummulitids significant. was action current and wave where environment, high-energy a in tests. nummulitid long mm 15 to up of abundance the of because are packstones easily macroscopically Nummulitid recognizable fragments. bioclastic fine of composed is matrix the and ented, ori randomly are tests The 4).Fig. 2, (Pl. nummulitids of tests and/or plete, (outerabraded fragmented whorl missing) lenticular The MFT 10 is with packstones composed com of coarse-grained 4.2.10. MFT10–Nummulitidpackstone sp., sp., ( foraminifera ing talia an one. abundant ( rotaliids Small nummulitids, lenticular red and algae coralline is foraminifera, also echinoderms, zoans, bryo of corals, association fossil diverse the matrix, the Within occur. sporadically Figs. 5, 6) Pl.2, matrix; skeletal the in tered scat (colonial solitary, and corals with grainstones while stones MFT 11 is mainly composed of bioclastic-foraminiferal4.2.11. MFT11 –Coral-foraminiferalpackstone pack tests. of ofup because to 3 the oriented, abundance cm long alveolinid are macroscopically easily Well-sorted recognizable grainstones Haddonia ex gr. gr. ex Interpretation: This This microfacies several appears along times the Čikola sec This microfacies appears in stratigraphic unit S2c unit of the Či stratigraphic in appears microfacies This Interpretation: Interpretation: lithotamnica lithotamnica LE CALVEZ) are common, whereas alveolinids, sp., sp., Fabiania cassis Acervulina linearis Acervulina Coarse-grained matrix with numerous bio with numerous matrix Coarse-grained The deposits identified as MFT 10 originat 10 MFT as identified deposits The MFT 9 represents a high-energy environ (UHLIG)) Nummulites spp.) within packstones suggests suggests packstones within spp.) , (OPPENHEIM) and Gyroidi and (OPPENHEIM) orthophragmids, and encrust orthophragmids, H A NZAWA, NZAWA, A H larger than 8 mm are Geologia Croatica 70/1 Miniacina Neoro ed ­ - ­ ­ ­ ­ ­ ­ - ­ ­ - ­ ­ ­ ­ ­

Geologia Croatica , ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ), 17 m ), ), tremato Orbitolites A. levantina , ) as as well Pseudochrysalidina alva A. multicanalifera , Coskinolina liburnica and Coskinolina A. cremae , Periloculina dalmatina Periloculina makarskae

have been identified within Conical agglutinated A total of 12 microfacies types (MFT 1 to MFT 12) have have 12) MFT to 1 (MFT types microfacies 12 of total A In the S2b unit of the Čikola section, ranging from 80 to 276 to rangingsection,80 from Čikola the of unit S2b the In This microfacies occurs only in the last 7 m of the Čikola Alveolina decastroiAlveolina 5. DISCUSSION Duringcar studied EocenetheinEarlyof thesuccessionarea, a bonatesaroundthickdepositedwas m 300 within shallow-water settings,(neritic) ranging from brackish to protected marine en vironments(representedMFT toby MFT1 to7)inner andmid MFTto 8 MFTenvironments carbonateramp by dle(represented A 12). palaeoenvironmetal model for the studied succession is provided in Fig. 3. The Čikolabeen deposited in succession subtropical, oligotrophic and euphotic to mix is (HOT interpretedophotic environments based on microfacies characteristics. as having preferences been distinguished, environmental demonstratingand palaeoenvironmental conditions. They reflect a great diver specific a diverse with arrayshallow-marine sityof biota, especially highlyasa LBF diversi of depositional group fied TINGER, 1983, 1997) within fluctuating environmental mined association fossil does attribution. age allow not section, at the the end stratigraphic of 2). unit (Fig. S2c 4.3. Biostratigraphy Theunit S1 of the Čikola section is characterised by occasional freshwater influences and alternating coal intercalations. The deterthe biostratigraphicso no dominantvalue, organisms have (Fig. 2), several stratigraphically( important species of alveolinids phore miliolids ( complanatus foraminiferalAlveolinid-miliolidpack and packstones (MFT 5) Late a therefore and 11–12 SBZ theindicate They (MFT7). stones this for age carbonate unit. (‘Cuisian’) Ypresian conical agglutinated foraminifera ( foraminifera agglutinated conical Pfendericonus - ­ ­ ­ ­ ­ ­ ­ Litho sp. and (PFENDER). Acervulina line­ Lithoporella me sp., sp., and Polystrataalba Mesophyllum Solenomeris sp., sp., Rhodoliths dominated by sporolithaceans porolithon (HOTTINGER, 1997). Small rhodoliths in pack rhodoliths Small 1997). (HOTTINGER, Miniacina sp. are today found between 30 and 80 m depth on (FOSLIE) and sp., S Schematic palaeoenvironmetal model of the Early Eocene Čikola carbonate ramp with interpreted facies belts: Brackish coastal environments (MFT 1–3); facies belts: Brackish environments coastal with interpreted ramp carbonate Čikola model of the Early Eocene Schematic palaeoenvironmetal This microfacies occurs in the last 30 m of the Čikola sec Interpretation: Based on the skeletal composition and textures, deposits of HANZAWA). Other skeletal allochems are ehinoderm frag Nummulites MFT is represented 12 poorly-sorted by fine-grained micritic to Themain coarse-grained characte 8). 7, packstones 2,Figs. (Pl. coralline fragmentsalgae: and rhodoliths of small risticsare thamnion 4.2.12. MFT 12 – Rhodolith-nummulitid packstone 4.2.12. MFT 12 – Rhodolith-nummulitid Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... tion, at the beginning stratigraphic of 2). unit (Fig. S2c ments, broken (nummulitids,LBFs orthophragmids), and rota- liids. characteristicaredepth,and m 60 occurbelow melobesioids and of recent carbonate environments below the fair-weather wave base in tropical and subtropicalfore-channels, and reef-flat settings, back-reef, including rietyof seas (BASSI, 2005) in a wide(BOSENCE,1983). m indeeperalsoand250 toreef waterdown va Rhodophyceae live at greater depths than other algae because they can better utilize the light blue that penetrates furthest into limitoccurrence their lower and marksthe 1998) (LEE,water the the zone. Coralline oligophotic of algae Lithotamnion Mesophyllum the Indo-Pacific 1979) and similar (ADEY, shelves facieswere interpretedoccurrencesthe suggestedby as as being2013), al., et NEBELSICK 2000; deposited in the upperof photic zone (RASSER, bottomfragmentedwithstones degreeof suggestsome bioclasts current reworking 2005). (BASSI, this microfacies probably accumulated in a moderate–high en ergyproximaltheinareas within probably zone,mesophotic the part the of middle ramp, well above the SWB, closer to FWWB. Fragments of corals or lithoclasts are overgrown by red algae and algae red by overgrown arelithoclasts or corals of Fragments ( foraminifera aris lobesioides Figure 3. Figure Protected lagoonal environments (MFT 4–7); Inner ramp environments (MFT 8, 11); Inner ramp shoals (MFT 9, 10), and Middle ramp environments (MFT 12). (MFT 8, 11); Inner shoals (MFT 9, 10), and Middle ramp environments ramp Inner (MFT 4–7); environments ramp lagoonal environments Protected Geologia Croatica was was controlled byposition ofthe palaeolatitudinal the North Dal 1997; TINGER, area PEARSON, the 2012). in occurrence Their (HOT environments carbonate Palaeogene Early the of ducers pro LBF,ofcarbonate major assemblage diverse and abundant deposits. gene Palaeo with areas other most for typical deposits, flysch and/or evidence of in subsequent the drowning form of Transitional beds no is there section Čikola the in as especially production, ment ­ sedi carbonate significant and space/subsidence commodation been between the established induced creation oftectonically ac having equilibrium fine a to testifies carbonates of amount sive 300 almost an period that during 1998)and al., et (SERRA-KIEL SBZ belong the to 11–12. deposits, overlying continuously from foraminifera associated and alveolinids identified that fact the ‘Cuisian’, middle be to on assumed based also is section studied Palaeo the DROBNE areas, et al., adjacent In 1991). section. gene The beginning Čikola the transgression of in sedimentation beds), Kozina in the (the deposits, Palaeogene oldest the startedof attribution age precise in the middle ‘Cuisian’beds. Promina up by filled sub-basin (SBZ 11; of a wedge-top a bedrock evolutionforeland basin represent and the of beginning the at deposited were limestones raminiferal Fo metres. 10 last the for except FWWB, the above deposits, inner-ramp of predominantly composed pattern, aggradational an showing (neritic)environments shallow-marine by acterised char was section Čikola the in Deposition suggesting sedimentation. stone 2012), al., et lime Foraminiferal of ending (MRINJEK induced tectonically probably beds a Promina the of ginning be the to belonging deposits subneritic fine-grained thrusting) (pre- initial representing sand, of lenses fine-grained silt or very and interlaminae normal-graded streaks, thin with beds stone mud massive with ends succession The settings. deeper what some indicates LBF with 2010)co-occurrence SICK, their and (BOSENCE, areas 1983; BASSI, 1998, 2005; BASSI & NEBEL have shallow-water from the been reported corallinaceans Tethy 2000).Fossilal., et (AGUIRRE settings warm–temperate water shallow- within mid-latitudes in melobesoid thrived assemblage A ramp. of middle the well-lit part high-energy, the indicate sils tions (Fig. 3). ofThe of dominance fragments LBF and macrofos propor decreased in present 12) are LBF while (MFT algae red by were a settings characterised ofhigh abundance corallinacean as formed, by indicated the MFT 9 and MFT 10. The middle ramp were shoals significant, was waveof action influence the Where representatives settings. ramp inner olids, characterised orbitolitids and z-corals forms, assem elliptical Diverse to mili larger foraminifera, conical ofA-generation), agglutinated (fusiform rotaliids. alveolinids of unidentified blages small, of occurrences radic of and spo bymiliolids the dominance characterised are ditions microfacies MFT 4 and MFT 6 under low-energy con originated The done. was assemblages in genera foraminiferal particular of proportion the on based sub-settings two between rentiation Diffe settings. ramp inner the in deposited were foraminifera, conical agglutinated orbitolitids)and and alveolinids (including composed of microfacies MFT 4 to MFT 12, with miliolids, LBF and 2),Fig. in (S2unit limestones ostracods 2).Fig. Foraminiferal in (S1 unit with along 3 MFT to 1 MFT units microfacies in charophyceae recorded are of gastropods) (occurrences influence water fresh with environments lagoonal Restricted, conditions. 18

m thick succession of was carbonates deposited. Such a mas As evidenced, the main characteristic ofAs the evidenced, main these characteristic deposits is the SBZs As mentioned, 11–12 Ypresianto Late the correspond prevented S1unit the in markers biostratigraphic of Lack an ­ ­ ­ ­ ­ ­ - ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ ­ - some parts of the entire sequence were documented. were sequence of entire the parts some Hvar and Pelješackotari, area) (Ravni only in Dalmatia whereas reveals its regions complete development Istria, in neighbouring ramp system succession was not developed. Comparison with to ofthe maximum 280 m DROBNEarea, (Benkovac et al., 1991). 1998)al., et (atMARJANAC Hvar,m 38 only from vary posits JANAC al., et 1998;2007). SCHWEITZER MAR 5;Fig. on 7 and 6 Hvar, and (Pelješac ‘Cuisian’ middle BABIĆ & ZUPANIČ, 2016) in the in Dalmatia Central the early– 1991;al., et DROBNE 5;Fig. on 5 and 4 (3,‘Cuisian’ middle the in Dalmatia Northern the 2008a),in 2004, ĆOSOVIĆal., et dian’ (2 onŠEK et al., 2016). in the ‘Iler in Istria commenced settings Ramp Fig.2012; 5;2008, al., et JURKOV (ZAMAGNI age ofMaastrictian is DROBNE,Fig. 1977; on 1 (Slovenia, region Kras the in part, NW DROBNE the In conditions. ramp of the beginning the concerning et noticed been has al.,crepancy 2011;Ravni kotari, Island of Hvar and Pelješac peninsula. An age dis bonate ramp system have been recorded in the region, Kras Istria, car a within environments) ramp outer to (inner settings of ray gions (Figs. 1A and 5) reveals the following: (Figs. the 1A 5) reveals gions and 28 – (EECO of temperatures Optimum ZACHOSal.,2001) et sea-surface tropical with Climatic Eocene Early the during ing in the Late global beginning Palaeocene and warming, culminat long-term The climate. “warm” Palaeogene early the by and 4) & SISSINGH, mately 38°N2000, 2003)(MEULENKAMP (Fig. approxi at Palaeogene, Early the during ForelandBasin matian middle ramp settings). ramp middle inner– to shoals and lagoons from – environments ferentiated (developmentdif of scenarios sedimentary such to contributed also rates, subsidence different and basins sedimentary the of configuration the in variations with along sea-levelfluctuations, The climate. temperate more by a characterised be aeolatitudes, production even in the which areas should, to according their pal MEULENKAMP & SISSINGH (2000, 2003) as presentedMEULENKAMP in HÖNTZSCH etal. (2013). tian Basin. The positionsofthecontinents andocean basinsare adapted from Dalma­ realm Eocene topositionoftheNorth intheEarly withmarked Middle Figure 4.SimplifiedpalaeogeographicMediterranean ofthe reconstruction

to

5), the older part of the succession, the Liburnian Formation Formation Liburnian the succession, of the older part 5), the 3) In some areas, including the studied one, the complete the one, studied the including areas, some In 3) 2) The thicknesses of Palaeogene carbonate ramp system de system ramp carbonate Palaeogene of thicknesses The 2) 1) From NW to SE of foreland ar the the different Dinaridic Comparison with similar deposits from neighbouring re neighbouring from deposits similar with Comparison

32°C (PEARSON et al., 2007), enabled abundant carbonate carbonate abundant enabled 2007), al., et (PEARSON 32°C Geologia Croatica 70/1 ­ ­ ­ - ­ ­ ­ ­ ­ ­ ­ ­ Geologia Croatica ­ ­ ­ ­ - ­ ­ ­ ­ ­ - - 19 teproduction (represented mostly by LBF) was an impor Therefore to avoid terminological confusion, a specific nameterminologicalspecific confusion, a avoid to Therefore bonate production keepingbalance with the subsidence (VLA HOVIĆ et al., 2005). et al., HOVIĆ for such a complex Palaeogene depositional system should be proposed, in order to clearly distinguish it from the underlying Adriatic Carbonate Platform. trolled by compressional synsedimentary tectonics and although carbona tant factor (as shown in the Čikola section example), the prevail ingin force modifying the accommodation space was tectonics, while on the the AdCP, dominant factor in sedimentation was car 6. CONCLUSIONS In the Canyon,Čikola Northern Dalmatia, during the Early Eo cene around 300 m of carbonates depositedtransgressivelyof were around cenem 300 theUpper Cretaceous over rudist-bearing(Campanian) limesto nes, representing one of thicker successions of Palaeogene car bonatesinthe Dinarides. During theEarlyEocene thesedimen tation took place along a neritic carbonate ramp depositional comprisescarbonatesuccessionthestudiedsection the In system. an older restricted, c. m 45 thick succession of veryForaminiferal shallow-ma 11–12) (SBZ Ypresian late a rinebeds,Kozinaand limestones succession deposited within inner to middle ramp en vironments.Foraminiferal limestones dominatedwere larger by benthic foraminifera conical(mostly agglutinated foraminifera, larger miliolids and alveolinids), and during the Upper Ypresian shallow-marinecarbonates of m 250 approximately Ma) 2.6 (cca. were deposited in relativelycarbonatesediandtectonicallybetween ancesubsidence induced stable environments, indicatingmentation. a bal ­ ­ ­ ­ - ­ - NI 5) The5) discrepancy in depositional and age of physiography Palaeogene deposits wereaccumulated on the deformed for­ 4) 4) Deposition in the entire North Dalmatian area, from the tional systems were formed, and (3) deposition was primarilywas depositioncon (3) formed,and weresystems tional ČAR, 2007; KORBAR, 2009; BRLEKAdCP deposits were during et the al., Palaeogene gradually 2014). drowned Gently depositionalenvironments of network folded complex a by covered and thetermwhich for PalaeogeneAdriatic Carbonate Platformwas duringof most However, 2011). 2009, al., et (DROBNE proposed the Palaeogene, a completely different depositional system was formed, the becauseformer (1) area of the Mesozoic AdCP was instead marine(2) deposits,Palaeogene by partiallyonlycovered of the previous vast, relatively flatshallow-marine Mesozoic duringAdCP, the Palaeogene complex carbonate ramp deposi tinuous shallow-marine environments, except for a narrowtrencha tinuousshallow-marine environments,for except characterised by deeper-marine environments that developed in the Palaeocene and extended westward from Montenegro and eastern MARINČIĆ Herzegovina1975; (CHOROWICZ, et al., 2006). et al., JELASKA ĆOSOVIĆ 2003; et al., 1976; settings probably resulted from diachronous deformation of the progressively evolving orogen (KORBAR, 2009) during the pre Intensehave tectonicactivityEocene.mightMiddle to Early - Pala thesettings. rampTherefore, of fulldevelopment the vented eogene deposits in the Outer Dinarides may be considered as evo the and development syn-orogenictheconnected depositsto andlution of foreland were basin(s) deposited in basins control al., et (SCHMIDDinaric orogen the to relateddeformation by led KORBAR,2008; 2009). mer mostly AdCP, above the regional unconformity (OTO middle ‘Cuisian’ onward, was characterised by more or less con less characterisedor wasonward,more by ‘Cuisian’ middle JANAC et al., 1998; PAVŠIČ & PREMEC FUČEK, 2000: SCHWEITZER et al., 2007; KORBAR et al., 2015), and (7) Pelješac, Orebić section (modified after MARJANAC et al., sectionMARJANAC Orebić (modified after 2015), and (7) Pelješac, et al., FUČEK, & PREMEC 2007; KORBAR 2000: SCHWEITZER et al., 1998; PAVŠIČ et al., JANAC 1998). Schematic correlation of Cretaceous to Palaeogene carbonate and clastic successions in the area of the Dinarides (for location see Fig. 1), from NW to SE: NW to 1), from see Fig. location the Dinarides of (for in the area and clastic successions carbonate Palaeogene to of Cretaceous 5. Schematic correlation Figure PAVLOVEC, 2008); (2) Istria (modified BENIĆ, 1991; et al., & DROBNE after & BABIĆ, 2003; ZAMAGNI 1991; ŽIVKOVIĆ PAVŠIĆ, (modified after DROBNE & (1) Krasregion section 1991); (4) Skradin–Dubravice 1976;DROBNE et al., (modified et al., after section 2004); (3) Korlat–Benkovac (modified after et IVANOVIĆ al., 1991; ĆOSOVIĆ section (modified after PUŠKARIĆ,MAR Podstina 1997; section 2000); (5) Čikola (this paper); (6) Hvar, & ĆOSOVIĆ, 1991; MARJANAC 1975; DROBNE et al., MAMUŽIĆ, Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... Geologia Croatica BASSI, BASSI, D. 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I. ­ ­ ­ - ­ - ­

Geologia Croatica 23 Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... Geologia Croatica 8) 7) 6) 5) 4) 3) 2) 1) Photomicrographs oftheLow Plate 2 24

­ Rhodolith nids andplanktonic foraminifera (rightfrom thecentre), sample Č1.302; Detail Fragments Coral­ Unidentified Foraminiferal Peloidal­ Alveolina foraminiferal of encrustingforaminifera foraminiferal cremae CHECCHIA foraminiferal of echinoids, coralline algae, alveolinids andunidentified small rotaliids in Coral Nummulites inNummulitidpackstone (MFT10),sampleČ1.275; grainstone (MFT 9)showing association ofmiliolids, alveolinids andmicritized echinoidradiolas, sampleČ1.158; packstone (MFT11)showing adetail ofacoral, sampleČ1.298, packstone (MFT8)defined by peloids, unidentified rotaliid foraminifera and fragmented alveolinids, sampleČ1.186; packstone showing fragmented foraminifera andLithothamnionsp. crusts, sampleČ1.301. er Eocene limestones microfacies inthestudied Čikola section: types ­ RISPOLI inAlveolinid­ sp.Solenomeris inRhodolith (ontheleft) miliolid packstone (MFT7),sampleČ1.232; ­ foraminiferal packstone (MFT12)withfragments ofechinoids, corals, orthophragmi ­ foraminiferal packstone (MFT 11),sampleČ1.296; Geologia Croatica 70/1 ­ Geologia Croatica 25 Španiček et al.: EarlyŠpaničekal.: et Eocene evolution ofcarbonate depositional environments recorded in the ČikolaCanyon ... Geologia Croatica 26 Geologia Croatica 70/1