Maastrichtian to Palaeocene and Eocene Pelagic Carbonates on the Island of Svetac (Central Adriatic, Croatia)

2020 | 73/2 | 95–106 | 7 Figs. | Appendix www.geologia-croatica.hr Journal of the Croatian Geological Survey and the Croatian Geological Society

Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) Tvrtko Korbar1*, Ladislav Fuček1, Vlasta Premec Fućek2 and Nenad Oštrić1

1 Croatian Geological Survey, Department of Geology, Sachsova 2, HR-10000 Zagreb, Croatia; (*corresponding author: [email protected]) 2 INA-Industrija nafte d.d., Lovinčićeva 4, HR-10000 Zagreb, Croatia doi: 10.4154/gc.2020.07

Abstract Article history: Maastrichtian to Palaeocene pelagic carbonates on the central Adriatic island of Svetac (Sveti Manuscript received January 17, 2020 Andrija) are the only outcrops reported to date that document pelagic deposition during the Cre- Revised manuscript accepted May 06, 2020 taceous–Palaeogene (K–Pg) transition within the Adriatic Basin. An approximately 3 m thick Available online June 30, 2020 succession at the Smokvica locality contains a rich and diverse planktonic foraminiferal assemblage which allows dating of the succession and the recognition of some biostratigraphic zones. The lower part of the Smokvica section consists of 1.5 m thick pelagic biomicrite characterized by the abundance of late Maastrichtian planktonic foraminifera that indicate the Abathomphalus mayaroensis Zone. An intercalation of intraclastic floatstone <0.5 m in thickness occurring on top of Maastrichtian pelagic biomicrite is characterized by unsorted pelagic intraclasts floating within the pelagic matrix, and both components only contain Maastrichtian planktonic foraminifera. The floatstone is overlain by another <0.5 m thick intraclastic-bioclastic floatstone characterized by rounded pelagic intraclasts (plasticlasts) containing Maastrichtian planktonic foraminifera floating in the pelagic matrix. The matrix of the later floatstone contains Maastrichtian and Palaeocene planktonic foraminifera mixed together. Thus, the transition from the Maastrichtian to the Palaeocene is not continuous but is characterized by amalgamated debrites that are related to at least two separated re-depositional events within the basin. The overlying pure pelagic biomicrite is rich in planktonic foraminifera that indicates the Palaeocene P3 Zone. A few metres apart, after the covered interval, there are also Eocene pelagic biomicrites with planktonic foraminifera which indicate the Eocene E9 Zone, characterized by the co-appearance of benthic foraminifera (Discocyclina) floating within the pelagic matrix. It is assumed that a Maas- trichtian opening of the deep-water environment connected to the Adriatic Basin within the for- Keywords: Adriatic Platform and Basin, Cretaceous, mer Adriatic Carbonate Platform west of the island of Vis could be related to a re-activation of Palaeogene, planktonic foraminifera an inherited transverse fault zone.

1. INTRODUCTION Although tropical Mesozoic carbonate platform successions in the proximately 50 million years of non-deposition and erosion peri-Adriatic region (Figs. 1A, B) are characterized by a hiatus (KORBAR et al., 2012) which is typical for the outermost ACP that encompasses the Cretaceous–Palaeogene (K–Pg) boundary tectonostratigraphic unit i.e., the Istrian Karst (KORBAR, 2009). (EBERLI et al., 1993; BOSELLINI et al., 1999; VLAHOVIĆ et The K–Pg hiatus within the shallow-water succession is also rec- al., 2005; KORBAR, 2009), there are rare outcrops characterized ognized in the boreholes located to the southeast of the island of by a more or less continuous record of the stratigraphic interval Svetac (Sveti Andrija), while to the southwest there is the realm of global interest (KORBAR, 2019, and references therein). The of the Adriatic Basin (GRANDIĆ et al., 1999, 2002; Fig. 1C). The Adriatic-Dinaridic Carbonate Platform (ADCP cf. PAMIĆ et al., K–Pg transition within the central part of the Adriatic Basin is 1998) that was separated into two major segments: Adriatic penetrated by the Koraljka borehole (125 km NW of the island of Carbonate Platform (ACP) and Dinaridic Carbonate Platform Svetac; Fig. 1C) is characterized by pelagic chalky limestones (D’ARGENIO et al., 1971; KORBAR, 2009; Figs. 1A, B), also with bioclastic (allodapic) platform-derived intercalations recognized as a unified Adriatic Carbonate Platform (AdCP cf. (LUČIĆ et al., 1993). VLAHOVIĆ et al., 2005; Fig. 1C), was the largest Mesozoic neritic Deeper-water carbonates deposited within the AdCP intra- depositional system in the region. Because of a regional emer- platform basins were characterized by calcisphere wackestone- gence of the platform during the Late Cretaceous into the Palaeo- packstones with rare planktonic foraminifera, indicating a re- gene, and the related hiatus within the succession, only a few stricted connection with the open sea (GUŠIĆ & JELASKA, exceptional localities from the central part of the Adriatic Car- 1990; FUČEK et al., 1991). The openings and durations of the bonate Platform sensu stricto (ACP cf. KORBAR, 2009) are charac intra-platform basins were diachronous, within the range from terized by a more or less continuous sedimentary record across the Turonian to the Campanian, while the Maastrichtian was gen- the K–Pg boundary. This boundary is marked within the sections erally characterized by platform emergence, although peritidal by a deposit which is a few centimetres to a few metres thick, deposition occurred within distinct tectonostratigraphic units of interpreted as the K–Pg tsunamite (KORBAR et al., 2015, 2017a). the ACP (KORBAR, 2009). The contact of the Upper Cretaceous and Palaeogene lime- Most of the data on the stratigraphy and palaeoenvironments stones on the island of Biševo (Fig. 1C) is characterized by ap- along the buried ACP margin and the Adriatic Basin in the cen- Geologia Croatica from the Late Cretaceous to the Early Palaeogene. Early the to Cretaceous Late the from transition the Tethys during of western palaeogeography tion the of Mesozoic end (Fig. reconstruc the the 1C), well for as as future at Adriatic of central the part this in environments depositional evolution for the and of palaeogeography of local the pretation for re-inter important is facies of island The Svetac. the on cies ceous to Palaeogene period. Palaeogene to ceous Creta latest the during sedimentation pelagic on data important revealed (Fig. island 1C), the on investigations detailed more new (2012) al. et BAR carbonates show shallow-water only Cretaceous (GELETTI KOR al., et 2008). by diapirs salt Although acterized char system complex tectonic of island along arather Svetac, the SW of 20 km some lying as ACP(1999) the margin interpreted al. et GRANDIĆ 2009). KORBAR, 2005; al., et VLAHOVIĆ 1999; al., et (GRANDIĆ papers published the in synthesised are and oil industry, for the collected have been area Adriatic tral 96 The aim of this paper is to document deep-water pelagic fa pelagic deep-water document to is paper of this aim The ------the surface (BELAK et al., et 2005; (BELAK al., KORBAR et 2012). surface the di The at appears and succession sedimentary the pierced places in that Triassic salt middle by mobilized driven were 2009). diapirs The (GRANDIĆ et al., 1999, 2002; GELETTI et al., 2008; KORBAR, rocks Triassic magmatic upper to middle incorporated contain that by diapirs salt mostly disturbed tectonically places in are that sediments pile of athick MesozoicQuaternary revealed to wells (Fig. deep 1A). and margins data Seismic circum-Adriatic orogeny, developed belts Alpine along the orogenic the the when of stage latest of the to Pangea phase Triassic rifting the from ing start thick kilometres several succession asedimentary within al., et 2008). evolution recorded The was al.,et SCHMID 2004; al., et 1979; ROSENBAUM (CHANNELL region peri-Adriatic the evolution characterizing Mesozoic Cenozoic geodynamic to complex by a very affected been (Adria) has microplate atic that of Adri the part central the belongs to area Adriatic central The SETTING GEOLOGICAL 2. and t Adriaticern coast (majorCroatian islands VLAHOVIĆ et al., 2005) along the northeast (AdCP) domain(light grey, modifiedafter theAdriatic Carbonate2019); C) Platform (modified after KORBAR, 2009and KORBAR, ADCPdomain:theAdriaticthe andDinari showing theexistence oftwo segments of per KORBAR, sketchtectonic (after 2009);B)a Svetac (arrows) on:A) aperi-Adriatic geo Figure 1.Location mapoftheisland i-Adriatic palaeogeographic mapsketch owns are indicated). Geologia Croatica 73/2 dic - - - - -

Geologia Croatica - - - - 97 et al., 2001; STEUBER 2005) et and al., (KOR Hvar 2001; et al., TEŠOVIĆ 3. MATERIALS AND METHODS The first discoveryof the pelagic facies on the islandof Svetac was in documented 2005, the by analyses thesample of from the 43.026051N; 15.762892E, (WGS: observation point VN-214 focused mapping was In 2014, HTRS(E/N): 439927/4765401). performed thefor purpose definingof the spatial distributionof the pelagic facies. The narrow pelagic zone carbonates of strikes andeast-west is bordered distinct by and indistinct faults. The Cove, ploča Crnaincolluvium by partlycovered carbonateswere fault that a major along borders the zone from the north 2 (Figs. and – APPENDIX). 2/Supplement Because the faults of and in distinct bedding seems (it that the bedding within the tectonic is nearlyblock vertical), was to it possible measureand sample only one section the along narrow pedestrian trail in the Smokvica The section extendsarea 2). (Fig. from the southwest where is it in tectonic contact with predominantly bioclastic recrystallized carbonates containing radiolitid rudist bioclasts, to the northeast BAR et al., 2010). The Gornji Humac formation on the island of 2010). BAR et al., Svetac, outcropping on the south-eastern coasts the island of ischaracterized 2), Fig. locality, (Slatina recrystallized by me dium to thick-bedded limestones with typical peritidal rudist lithosomes composed various of radiolitidrudists. In contrast, the northern and western outcrops referred to as the Gornji Humac Formation are recrystallized built of thick-bedded to bi massive oclastic limestones rich in rudist fragments and recrystallized biomicrite. The carbonates are in distinct tectonic contacts with the Lower Cretaceous peritidal carbonates of the Goveđari and formationsBabino polje (HUSINEC, from 2002) thesouth and from 2 and 2/ the north, Fig. respectively (KORBAR 2012; et al., Supplement – APPENDIX). ------CVETKO The Svetac island is the of outermost the island central of The wider area the island to of belongs the Adriatic foreland The Upper Cretaceous rudist-bearing carbonates outcrop Geological map of the island of Svetac (KORBAR et al., 2012), showing the position of the studied section VSS and sample VN-214 at SmokvicaVN-214 at locality VSS and sample the position of the studied section 2012), showing et al., (KORBAR of the island of Svetac map 2. Geological Figure (hatched). carbonates pelagic massive to thick-bedded Palaeogene of Maastrichtian to zone within a narrow (black arrow) phological featuresphological the central of Adriatic islands (KORBAR et that been have recognized 2012), recentlyal., as UNESCO Global Geopark archipelago. Vis Adriatic (Dalmatian) archipelago, located km about 50 south of the mainland, Pal and 1C). km 22 the (Fig. Vis island of west of aeogeographically, the Svetac island is considered of to be an in tegral part of the Adriatic Carbonate Platform (VLAHOVIĆ et and 2005), is the at al., surfacetectonic built of derived blocks thick m successiontypical of fromCretaceous >1500 a shallow- carbonateswater (neritic) (KORBAR 2012). et al., of both the Dinarides and the Apennines (SCISCIANI & CA The CretaceousLAMITA, 1A). to Palaeogene 2009; Dinaric Fig. stageforebulge and the long-lasting subaerial exposure the of deposition by platform during was followed the Oligocene fore land stage at the the end Dinaric of foredeep migration phase 2009). (KORBAR, apirs outcropped presumably during the Miocene (PIKELJ et al., al., (PIKELJoutcroppedduringMiocenepresumablyet apirs the al., et BABIĆ 2008; al., et growing(GELETTI stillare and 2015), Thus, salt tectonic related deformations2012). the overlying of Adriatic carbonate platform succession and Quaternary erosion created prominent structures geological and interesting geomor Korbar et al.: Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) ping on the Svetac island is recognized of as a typical suc ACP cession of the Gornji Humac Formation& JELASKA,(GUŠIĆ although the uppermost1990), part resembles the open-platform and carbonates slope reported from domain: the ACP the Turo nian carbonates in the western part the Dugi island of of Otok (FUČEKthe et Turonian–Santonian al., 1991), of the islands of Premuda, Ist and Silba (MORO & ĆOSOVIĆ, or 2013), the Mid dle Campanian facies on the islands of Brač ( Geologia Croatica The species concept for Cretaceous taxa after SLITER (1989) SLITER after taxa and for Cretaceous concept species The keels. or thickenings of peripheral number and position sence, orab presence of wall, the thickness of chambers, rangements ar and number shape, size, of test, shape the the and size the as such characteristics of morphological the observations and tests of foraminiferal the sections cross un-oriented on based were era foraminif of planktonic determinations SZX12. taxonomic The Olympus by an taken were thin-sections of selected the crographs 2010). (FLÜGEL, photomi analyses and microscopy optical The micropaleontological and for microfacies procedure standard the to according Survey Geological Croatian the at prepared were Thin-sections lens. hand by field the in undertaken were 439906/4765407). (E/N): (Fig. 3), VSS-5 sample to (WGS: 15.762635E, 43.026106 N; HTRS 439905/4765404), of part covered the north afew metres and, (WGS: VSS-4 sample to 15.762635E, 439905/4765400) 43.026076 (E/N): N; HTRS (E/N): HTRS 43.026043N; 15.762634E, (WGS: VSS-1 sample from starting of carbonates, zone massive pelagic (Fig. 2). biomicrites lagic pe of zone Maastrichtian the with contact tectonic it in is where of polishedslabsintraclastic floatstonesMaastrichtian andthe of (debrites) the that mark contact Palaeocene: A) sample B)sample VSS-3, VSS-3A. Figure 3.Illustrated stratigraphic column showing thepositionofsamples, ofthedetermined fossils, distribution Vis-Svetac-Smokvica andphotographs (VSS) 98 The preliminary palaeontological and facies observations observations facies and palaeontological preliminary The the within sampled and measured is section Smokvica The - - - - - clastic and bioclastic intercalations (Fig. 3/Supplement 3and – intercalations bioclastic and clastic C of by a~3 thick-bedded succession mthick characterized is of island Svetac the on (VSS) section Vis-Svetac-Smokvica The carbonates atSmokvica 4.1. CretaceoustoPalaeogene (K–Pg)pelagic fossils.benthic any lack that foraminifera planktonic in rich -abiomicrite cies fa pelagic typical resemble places in wackestones skeletal dish grainstone. to packstone bioclastic crystallized skeletal wackestones (rarely floatstones)with intercalations of re to mudstones predominantly 3, 4). are and These – APPENDIX, massive in carbonates the Crna ploča cove (Figs. 2, 2/Supplement to thick-bedded of pelagic the discovery in resulted research The RESULTS 4. tions of YOUNGtions (2017) al. et used. been also has sec (2003), al. et foraminifera (2006). al. et The PEARSON and OLSSON (1999), al. et after PREMOLI SILVA determined were the with together species Eocene and (2006, 2009). of used, Palaeocene SARI papers was (2004) VERGA & SILVA PREMOLI retaceous and Palaeocene pelagic limestones with afew intra with limestones pelagic Palaeocene and retaceous Geologia Croatica 73/2

Fine-grained red Fine-grained

- - - - - Geologia Croatica - - - 99 Directly overlying the intraclastic floatstone (Fig. 3) Directly there 3) is intraclastictheoverlying floatstone (Fig. wackestone to packstone (polished slab VSS-3; Figs. 3A and 4). and 4). 3A wackestone to Figs. packstone (polished VSS-3; slab Both lithological components Maastrichtian contain exclusively 5). (Fig. foraminifera planktonic character thick) (<0.5m intraclastic-bioclasticanother floatstone, ized a pelagic by matrix and semi-rounded intraclasts (plasti similar of clasts) pelagic facies, with along tiny molluscan bio clasts (polished slab VSS-3A on Fig. 3B). The floatstone is - - - A) Composite photomicrograph of the sample VSS-3A showing the mixture of Palaeocene and Maastrichtian pelagic lime mud and intraclasts/plasticlasts intraclasts/plasticlasts and mud lime Maastrichtian pelagic and Palaeocene mixture of the VSS-3A showing sample the of photomicrograph Composite A) 4. Figure from the parts magnified foraminifera B and D) of the planktonic Maastrichtian rim; C and E) magnified arrows); by (rim is indicated of a Maastrichtian intraclast matrix. Palaeocene tonic foraminifera An 5). intercalation (Fig. thick intra <0.5m of clastic floatstone islocated above the Maastrichtian pelagicbi mmcharacterized intercalationunsortedis Theomicrite. 2−20 by light-greylong intraclasts pelagic wackestone of to packstone (biomicrite) that are “floating” within thepinkish-grey pelagic APPENDIX). part The lower the succession of is characterized metre thick a 1.5 by package pelagic limestones of (biomicrite) characterized the by mass occurrence Maastrichtian of plank Korbar et al.: Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) Geologia Croatica pelagic limestone only contains Palaeocene planktonic foraminif planktonic Palaeocene contains only limestone pelagic (Fig. 3). thick not observed are metre overlying The sociations as foraminiferal planktonic (Danian) Palaeocene lowermost the that noted be should It floatstone. pelagic Maastrichtian the lies over directly foraminifera, planktonic Palaeocene and trichtian Maas mud containing lime and intraclasts Maastrichtian mixed by characterized is that floatstone pelagic Palaeocene the Thus, (Fig. 4). intraclasts the in and matrix the in foraminifera tonic plank F) 6A−C,(Fig.and Palaeocene and H) and G, 5E, (Figs. floating Maastrichtian bioclasts containing packstone and to wackestone apelagic in intraclasts long mm 2−20 by characterized omphalus mayaroensis, sample VN-214. Allscalebars0.2mm. VN-214; J– canita insignis,sample F–KuglerinaVSS-3A; rotundata , sample GlobotruncanellaVN-214; G,H– havanensis, sample I– GlobotruncanellaVSS-3A; pschadae,sample ple B–ContusotruncanaVSS-2; contusa, sample VN-214; C–Contusotruncana fornicata, sample , sample GlobotruncanitaVN-214; D– stuarti Globotrun E– VSS-3; Figure 5. Photomicrographs planktonic Maastrichtian foraminifera ofselected from sample VN-214 andsamples VSS 1-3.A–Contusotruncana patelliformis, sam 100 Racemiquembelina fructicosa, sample , sample PlanoglobulinaVN-214; K– acervulinoides andfragment L-Planoglobulina acervulinoides VSS-3; ofAbath------tian pelagic mudstone outcropping north of fault. the north outcropping mudstone pelagic tian Maastrich a light-grey with contact tectonic in is limestone lagic (Fig. pe 6O). mudstone pelagic Eocene Eocene The the within floating (discocyclinids) foraminifera benthic Palaeogene of appearance by the characterized is that 6) (Figs. 3and limestone pelagic of long Eocene outcrop ametre is there – APPENDIX), Fig. by covered vegetation, is 3/Supplement trail sion (the walking solely Palaeocene pelagic intraclasts. pelagic solely Palaeocene contains that floatstone of intraclastic-bioclastic intercalation an is there of limestone the part 6D). (Figs. middle 3and the era In Two metres north of the Maastrichtian to Palaeocene succes Palaeocene to ofTwo Maastrichtian the north metres Geologia Croatica 73/2 - - - - - Geologia Croatica - - 101 , sample VSS-5; J – Subbotina eocaena , sample crassatus VSS-5; I – Morozovelloides , sample VSS-5; H – Subbotina yeguaensis , sample frontosa Turborotalia sample VSS-3A; C – Igorina tadjik angulata, sample VSS 3A-5. A,B – Morozovella samples from foraminifera planktonic of selected Palaeogene 6. Photomicrographs Figure bull VSS-5; N – Acarinina , sample mcgowrani VSS-5A; M – Acarinina , sample bolivariana VSS-5; L – Pseudoglobigerinella , sample kugleri VSS-5; K – Globigerinatheka Parasubbotina pseudobulloides, VSS-4; F – Parasubbotina sample VSS- ; sample VSS-4A; E – Globanomalina ehrenbergi , sample VSS-3A; D – Subbotina velascoensis istanensis, sample 3A; G, – VSS-5A.mm. All scale bars 0.2 matrix of sample within the pelagic VSS-5; foraminifera O – discocyclinid benthic brooki, sample Korbar et al.: Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) Geologia Croatica Discocyclina f benthic of large the specimens many taxa niferal 2005; WADE al., et 2011). forami planktonic the to addition In (BERGGREN & PEARSON,(HO) of aragonensis Morozovella of LO the rangezone between taxa ofasthethe fined concurrent nominate Zone ( Zone bullbrooki bolivariana 6J), 6J), tus Turborotalia as such frontosa VSS-5 samples 5A. in and Species observed been has association ( P3Zone Palaeocene chapmani triloculinoides botina (Figs. 6A, B), Morozovella angulata determined: have been taxa laeocene VSS-3A. sample in following Pa occurs The foraminifera tonic S. cancellataS. (Fig. 6D), triloculinoides S. velascoensis botina & VERGA, 2004). trichtian Maas Late the indicates foraminifera ofassemblage planktonic helix tilabrella species: species: foraminiferal following planktonic the Sample VSS 4contains observed. been also has foraminifera benthic of small occurrence (WADE al., et 2011). pseudomenardii lina rare very The (LO) ofrence Morozovella angulata the between lowest asZone, the interval defined occur currence Oc Lowest i.e. Morozovella P3Zone, angulata the Palaeocene banomalina chapmani loides 5J), 5J), tusa 5F), Abathomphalus mayaroensis conica (Fig. 5D), stuarti Globotruncanita Globotruncanita botruncanita insignis insignis botruncanita semble intra-platform basinal facies reported from elsewhere on on elsewhere from reported facies basinal semble intra-platform of not do re island Svetac the on described facies pelagic The DISCUSSION 5. Globotruncanella Globotruncanella vanensis (Fig. 5A), patelliformis ha Globotruncanella Contusotruncana foraminifera. planktonic of Maastrichtian sections thin- well preserved of exceptionally the because here analyzed is and mudstones, pelagic of light-grey zone the same the within 2, VN-214 point vation of VSS-1 samples 20 meast and observed is obser the from sample The species. Eocene contain that bonates car pelagic also are there interval, acovered after succession, the of north Afew metres 3/Supplement–(Figs. 3and APPENDIX). VSS geological column the in a ~3 succession m thick cies within the successi indicate unambiguously foraminifera planktonic analysed The 4.2. Biostratigraphy 102 (Fig. 6H), (Fig. yeguaensis (Fig. Subbotina 6I), Macroglobigerinelloides Contusotruncana con Contusotruncana 5C), fornicata (Fig. Contusotruncana A rich and highly diverse Eocene planktonic foraminiferal foraminiferal planktonic Eocene diverse highly and A rich A mixed assemblage of Maastrichtian and Palaeocene plank Palaeocene and of assemblage Maastrichtian A mixed The following Maastrichtian taxa have been determined: determined: have been taxa following Maastrichtian The Globigerinatheka kugleri Globigerinatheka (Fig. 5B), L) (Figs. 5K, Planoglobulina acervulinoides Pithonella ovalis, P. innominata P. ovalis, Pithonella innominata sp., Globigerinatheka kugleri Globigerinatheka (Fig. Globanomalina 6F), ehrenbergi (Fig. Glo and 6E) Morozovella angulata Abathomphalus mayaroensis (Figs. 5G, H), sp., sp., . The planktonic association indicates upper part of the of the part upper indicates association planktonic . The Globigerinatheka kugleri Globigerinatheka (Fig. 6N) are characteristic of the middle Eocene E9 Eocene of middle the characteristic are (Fig. 6N) ve appearance of Maastrichtian and Palaeocene spe Palaeocene and of Maastrichtian ve appearance (Fig. 6L), mcgowrani Acarinina sp. are also present (Fig. 6O). present also sp. are , Gublerina Gublerina Igorina tadjikistanensis Globanomalina cf. cf. , Morozovella angulata S. triangularis S. . The association is characteristic for the for the characteristic is association . The (Fig. 5E), petaloidea sp., sp., Globotruncanella pschadae (Fig. (Fig. (Fig. 5L), rotundata Kuglerina (Fig. Racemiguembelina (Fig. fructicosa sp., sp., (Fig. 6G), crassa Morozovelloides Pseudoglobigerinella (Fig. 6K), Pseudoglobigerinella

ehrenbergi , / Muricohedbergella Igorina tadjikistanensis Morozovella aragonensis Morozovella Globotruncana Globotruncana , , arca Globotruncana and the highest occurrence occurrence highest the and and the LO of LO Globanoma the - and , Parasubbotina pseudobul Parasubbotina (Fig. pusilla 6C), I. Zone (PREMOLI SILVA (PREMOLI Zone and Globanomalina Globanomalina and ). A. A. and (Fig. 6M) P. sphaerica S. eocaena S. , S. triangularis S. cf. cf. oraminifera sp., sp., orientalis (Fig. 5I), Hetero , , , Ven , (Fig. (Fig. . The The . ) de Sub Glo Sub ------, , ,

SEI & MOUSSAVIAN, 1997; BOSELLINI et al., 1999). The The 1999).al., et BOSELLINI MOUSSAVIAN,1997; & SEI al., et 1996; VEC (MUTTI K–Pg the transition during starvation sediment and by emergence characterized were region the in gins mar platform carbonate the that highlighted It be must platform. carbonate the from influence the without basin the within tion re-deposi to points that of section the part lower (Maastrichtian) the in absent are rudists and foraminifera shallow-water benthic the to of referred is one afew biozones (Fig. latest the 5),mixing while suggests foraminifera planktonic of Maastrichtian ciation late (Fig. 3). asso The foraminifera planktonic Palaeocene lack that matrix a pelagic in of (plasticlasts) carbonates pelagic traclasts in the area of the island of of island Svetac. the area the in Palaeocene to Maastrichtian the during environment depositional basinal acontinuous and slope imply instability mud intraclasts pelagic Palaeocene and of Maastrichtian the mixing osition and respectively. of Re-dep Palaeocene, bottom atthe and trichtian of top Maas atthe deposited 0.5m debrites thick amalgamated by two (Fig. characterized one is 3). K–Pg the transition Thus, lower the eroded one upper the that it seems and amalgamated are twodebrites The the slope. on or basin the within flows bris depositional deep-water a de from deposited have probably been debrites the environment, Considering 2001). ma cohesive a ALEXANDER, in & floating as the intraclasts arefloatstones muddytrix, interpreted (MULDER debrites pelagic the and mud pelagic of (Fig. 3). abundance deposits the to Palaeocene According and pelagic intraclastic floatstones atthe contact ofthe Maastrichtian of of (Fig. types island Svetac two the on 3) are succession there al., et 2012; (KORBAR island the Fig. 2). from reported are 2005) al., et ACP (AdCPVLAHOVIĆ cf. the of top on deposited shallow-water formations well-known by the represented carbonates peritidal typical the of since land Svetac, of is the area the in of Cretaceous most the during not exist did developed Visment west (Fig. of island embayment the 7). The embay adeep Maastrichtian the during that it inferred is Thus, sea. open the with environment of depositional the connection adirect suggesting foraminifera, of planktonic species various in rich of are island Svetac the on carbonates pelagic the Instead, (Gof calcispheres abundance an and foraminifera of planktonic by apaucity terized (ACP) charac Platform are that Carbonate domain, Adriatic the indicated by broken lines. central Dalmatian islands (contoured by dotted lines). Inferred transverse faults transition. Conservative reconstruction related to the recent arrangement ofthe (grades ofgray theCretaceous–Palaeogene during and italicisedtext) (K–Pg) Figure 7.Central-Adriatic palaeogeography and depositionalenvironments The lower (top Maastrichtian) debrite is characterized by in characterized is debrite lowerThe (top Maastrichtian) pelagic Palaeocene to Maastrichtian 3mthick the Within Abathomphalus mayaroensis Skeletons Zone. (bioclasts) of UŠIĆ & 1990;JELASKA, FUČEK et al., 1991). Geologia Croatica 73/2 ------Geologia Croatica . ------103 ). 181-1811096-1093) ” ( Zone and the upper part The Basic Gological Map Croatian Geological Congress), Opati- rd Morozovella angulataMorozovella Abathomphalus mayaroensis Abathomphalus . (eds.): 3. Hrvatski geološki kongres (3 BENČEK, Đ. (2005): Novi prinos stratigrafiji evaporitno-karbonatno-klastično- Hrvatska) [New Contribu- Vis, vulkanogenog kompleksa Komiškog zaljeva (otok Complex tion to the Stratigraphy of Evaporitic-Carbonate-Clastic-Volcanogenic Biondić, & I. Vlahović, In. Croatian].– in – Croatia) Vis, of (Island Bay Komiža of R sediments of the Central Adriatic Island of Brusnik.– Geologia Croatica, 65/2, sediments of the Central 223–232. doi: 104154/gc.2012.13 ja, Abstract Book, 13–14. ja, 1) The unusually1) thick-bedded to pelagicmassive limestones The thick 3m succession2) is characterized the by assem- Nevertheless, the discovery pelagic carbonates of on the is 3) The transition3) from Maastrichtian to Palaeocene pelagic Although4) the direct contact Palaeocene of and Eocene pe 5) It is possible to is possible suppose It 5) that the Maastrichtian opening of 6. CONCLUSIONS According to themicropaleontological andsedimentological analyses the pelagic of carbonates on the Svetac is island it of topossible the conclude following: on the Svetac island are of rich in various species planktonic of foraminifera that imply direct a connection the depositional of environment with the open the sea nearby of Adriatic Basin. BELAK, M., KOCH, G., GRGASOVIĆ, T., VLAHOVIĆ, I., VELIĆ, I., SOKAČ, B. & B. SOKAČ, I., VELIĆ, I., VLAHOVIĆ, T., GRGASOVIĆ, G., KOCH, M., BELAK, REFERENCES REFERENCES marine Pleistocene Uplifted (2012): Y. ASMEROM, & M. CRNJAKOVIĆ, LJ, BABIĆ, ACKNOWLEDGEMENTS This was supported work the by CroatianMinistry Science, of “Stratigraphy project scientific Sportsthrough theandEducation and Geodynamic Cretaceous Context of Deposits in the NE Adri atic Region” (181-1191152-2697) and “ atic (181-1191152-2697) Region” thelication paper. of of the Republic of Croatia, the of Republic of scale 1:50000 would We like to thank to VlatkoBrčić for technical anonymous a composite photomicrograph.of reviewers are Two preparation greatly acknowledged their for constuctive also suggestions. We wish to thank the editors handling for the manuscript until pub land of Šolta that Šolta land of is characterized the by same strike (KORBAR The intraplatform Šolta basin is situated 2017b). etal., thealong northeastern continuation the supposed of transversal lineament further However, 7). (Fig. investigations are necessary to test this hypothesis. blages of planktonic of blages foraminifera that indicate the Late Maas trichtian land of Svetacland is important of the reconstruction for the latest of Cretaceous to Palaeogene palaeogeography the central of Adri aticarea. Considering the hypothetical boundary K–Pg tsunami thatoriginated possibly in the Atlantic Ocean (KORBAR, 2019), the local palaeogeography could also be important the for recon struction the at the western the of end Mesozoic. of Tethys of the Palaeoceneof P3 Zone ( carbonates continuous is not is characterized but amalgamated by debrites that are related to least at two separated re-depositional events withinthe basin. lagic carbonates is documented, not the Eocene pelagic facies, outcropping metres a few from the Maastrichtian to Palaeocene succession, implies continuous a possible Maastrichtian to Eo cene pelagic environment on this part the former of Adriatic Car bonate Platform. the deep-water pelagic environment the Adriatic of Basin within the former Adriatic Carbonate the Platform Vis island of west of could be related to a re-activation an inherited of transverse fault zone. ------Considering the unusual beds event reported from the is The Palaeocene debrite contact at the on the K–Pg island of Considering the fact that the thin-sections Palaeocene of The benthic foraminifera in the separated Eocene part the of Although the typical Upper Cretaceous lithostratigraphic Zone, defined according to the youngest association of plank of youngest association defined accordingZone,the to BAR, 2009), and the starvation could stronglymentation influence rate within the supposed embayment 7). (Fig. the sedi emergence is also recognized southern on the ACP margin (KOR Korbar et al.: Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) lands of Hvar (KORBAR et al., both deposited within2015) the peritidal and at domain2017a), the ACP of Brač (KORBAR et al., boundarythe K–Pg the 7), Maastrichtian (Fig. part the com of debriteplex on the Svetac island could of be tentatively inter preted deposit. event could If as it be so, related the to K–Pg an extraordinary hydrodynamic or an event earthquake that was able to mobilize pelagic and mud semiconsolidated pelagic sediment mud mixture of the redeposit and floor, embaymentdeep thefrom and the intraclasts (plasticlasts) as a sedimentary load within the same pelagic depositional environment 7). (Fig. Svetac contains both Maastrichtian and Palaeocene planktonic foraminifera in the matrix and Maastrichtian pelagic intraclasts The content the debrite of 3). implies(Fig. the existence a slope of which re-depositionalong unconsolidated of and semi-consoli dated pelagic occurred. mud The content thus implies mixing of mudstone intra fluidizedpelagic Maastrichtian and mud pelagic 2007).clasts, et al., as as BICE well Palaeocene pelagic (cf. mud (Danian?) planktonic foraminifera cannot be determined to spe the the upper of age cies level, debrite is related to the Palaeocene P3 tonic foraminifera Thus, in the the sample VSS-4 Pal 3). (Fig. aeocenedebrite could be tentatively correlated the to Pal one of aeocene regional submarine landslides that are recorded within the pelagic succession the neighbouring of Umbria-Marche basin 2007). The et al., Maastrich BICE (MONTANARI 1989; et al., tian toPalaeocene was a period intermittent of collapses the of northern margin the Apulian of Carbonate Platform into the Adri atic Basin and into (BOSELLINI the Ionian 1999) et al., counter least At 1B). Fig. part 2012; et al., on the southwest (RUBERT the regionalone of Danian events is also recorded probably within the Danian peritidal succession on the neighbouring island (KORBAR Hvar 2015). etof al., presumably discontinuous pelagic succession on the island of shallowing imply a possible upward trend 3) Svetac (Fig. or a de nearby of neriticvelopment environments. In case the it later, of could also be interpreted as a skeletal muddy debrite. unit the Gornji of Humac Formation is characterized peritidal by limestones, the Upper Cretaceous carbonates referred to the for mation on the the map Svetac geological Basic island of (KOR of are BAR characterizedet al., 2012) by highly diversified facies. Besides, the carbonates are intensively tectonically fractured and recrystallized. to Therefore, possible distinguish always is not it between typical peritidal and deeper-water facies (pelagic lime stones with bioclasticintercalations, resembling allodapic lime the presented However, resultsstones). suggest that during the Maastrichtian the area the Svetac island became of of part a of the Adriatic Basin, in probably the form a deep of embayment withindeveloped theformer platform ispos domain It 7). (Fig. that the sible embayment has been opened transversea along lin eament that has been active during the various periods the of andMesozoic, could be related to the intermittent activity the of deeprooted fault zone striking which along the SW-NE, Vis- Šolta trough/graben formed during the Triassic (GRANDIĆ et Presumably 2002). al., the deep-rooted fault also initiated devel a Cenomanian-Turonian intraplatformopment of basin on the is Geologia Croatica 104 BOSELLINI, A., MORSILLI, M. & NERI, C. (1999): Long-term event stratigraphy of of stratigraphy event BOSELLINI, Long-term (1999): C. NERI, & M. MORSILLI, A., BICE, D.M., MONTANARI, A. & RUSCIADELLI, G. (2007): Earthquake-induced tur BERGGREN, W.A. & PEARSON, P.N. (2005): A revised tropical to subtropical Paleo- GRANDIĆ, S., BOROMISA-BALAŠ, E., ŠUŠTERČIĆ, M. & KOLBAH, S. (1999): (1999): S. KOLBAH, & M. ŠUŠTERČIĆ, E., BOROMISA-BALAŠ, S., GRANDIĆ, GELETTI, R., DEL BEN, A., BUSETTI, M., RAMELLA., R. & VOLPI, V. 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Geologia Croatica 105 (PETTERS, 1954) (GANDOLFI, 1955) EL-NAGGAR, 1966 (BOLLI, 1957) (CUSHMAN, 1925) (PARR, 1938) (PARR, (PLUMMER, 1926) (PLUMMER, (BOLLI, LOEBLICH & TAPPAN, 1957) & TAPPAN, (BOLLI, LOEBLICH sp. (BY KOVA, 1953) (WHITE, 1928) (WHITE, 1928) (SUBBOTINA, 1953) petaloidea BLOW, 1979 BLOW, (BOLLI, 1957) (KAUFMANN, 1865) (KAUFMANN, (CUSHMAN, 1926) sp. (GUEMBEL, 1868) orientalis cf. cf. (BOLLI,1957) sp. sp. sp. Palaeocene planktonic foraminifera chapmani Globanomalina angulataMorozovella Subbotina triangularis Igorina tadjikistanensisIgorina Planoglobulina acervulinoidesPlanoglobulina (EGER, 1899) fructicosa (EGGER,Racemiguembelina 1899) Ventilabrella Globanomalina ehrenbergi pusilla Igorina Parasubbotina pseudobulloides (BOLLI, 1957) Subbotina cancellata Subbotina triloculinoides Eocene planktonic foraminifera Acarinina bullbrooki Globotruncanella pschadae (KELLER, 1946) Globotruncanita conica (WHITE, 1928) Globotruncanita insignis (GANDOLFI, 1955) Globotruncanita stuarti (de LAPPARENT, 1918) Gublerina Heterohelix 1952) Kuglerina rotundata (BROENNIMANN, Macroglobigerinelloides Muricohedbergella innominata (BONET,Pithonella 1956) 1865) Pithonella ovalis (KAUFMANN, sphaericaPithonella Subbotina velascoensis (CUSHMAN, 1925) & PEARSON, 2006 Acarinina mcgowrani WADE Globigerinatheka kugleri Morozovelloides crassatus Globotruncanella havanensis (VOORWIJK, havanensis Globotruncanella 1937) Globotruncanella bolivariana Pseudoglobigerinella eocaena Subbotina Subbotina yeguaensis (WEINZIERL & APPLIN, 1929) frontosa Turborotalia Maastrichtian planktonic foraminifera (BOLLI, mayaroensis Abathomphalus 1951) Contusotruncana contusa (CUSHMAN, 1926) Contusotruncana 1931) fornicata (PLUMMER, Contusotruncana patelliformis (GANDOLFI, 1955) arca Globotruncana Globotruncana APPENDIX Maastrichtian, of List Palaeocene and Eocene taxa cited in the text and figure captions(in alphabetical order according genus): to Korbar et al.: Maastrichtian to Palaeocene and Eocene pelagic carbonates on the island of Svetac (central Adriatic, Croatia) Geologia Croatica breccia (p)deposited alongagenerally Sveti east-west fault(Fig. Andrija striking 2).Outcrops ofLower Cretaceous carbonates are visibleinthe background. Figure 2/Supplement. Outcrops ofmassive pelagic Maastrichtian carbonates ontheeastern coastcovered oftheislandSvetac partly by colluvial carbonate 106 walking trail at Smokvica. Note trail theheavily at Smokvica. vegetatedwalking area around thesection. Figure 3/Supplement. The mainsampling points within thethick-bedded to massive oftheislandSvetac pelagic carbonates alongthe on the eastern part Geologia Croatica 73/2