269 - Korbar & Husinec.indd 1. INTRODUCTION The Croatian island of Cres is situated in the northern part of the Adriatic Sea (Fig. 1). It is built up of predominantly Cretaceous carbonates, although there are some minor scattered outcrops of Palaeogene deposits (POLŠAK, 1967a; MAGAŠ, 1968; MAMU- ŽIĆ, 1968; ŠIKIĆ et al., 1969). A succession of Lower Cretaceous carbonates, approximately 800 m thick, ranges in age from the early Neocomian to the latest Albian, and is characterized by shallow- marine deposits sporadically interrupted by minor emersion horizons (FUČEK et al., 1995). Major facies differentiation took place during the Cenomanian (HUSINEC et al., 2000; KORBAR et al., 2001), as shown by lateral changes from peritidal restricted facies with radiolitid bouquets, via marginal coarse-grained bioclastic facies predominantly with recumbent rudists (ichthyosarcolitids and caprinids) to deeper-water calcisphaerulid facies. Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates: A Case Study from the Island of Cres (Northern Adriatic, Croatia) Tvrtko KORBAR and Antun HUSINEC From the fossil association studied by them, previous authors (POLŠAK, 1967a; MAGAŠ, 1968; MAMUŽIĆ, 1968; ŠIKIĆ et al., 1969; MAMUŽIĆ et al., 1982) considered the youngest Cretaceous deposits on the island of Cres to be of Cenomanian–Lower Turonian age. However, that association is now considered to be restricted to the Cenomanian (GUŠIĆ & JELASKA, 1990). Later, JELASKA et al. (1994) proposed that sedimentation was interrupted close to the Cenomanian–Turonian boundary and that the gap lasted until the Eocene (Lutetian) transgression. In contrast to the NE part of the island, where the youngest strata below the regional K–T emersion horizon are of Cenomanian age, deposition continued in the SW part into the post-Cenomanian (KORBAR, 1999; KORBAR et al., 2001; KORBAR & HUSINEC, 2002). The aim of this paper is to describe the fossil assemblage in the youngest Cretaceous carbonate deposits on the island of Cres, as well as to interpret the age and depositional palaeoenvironment of the investigated strata. The boundary between these and the underlying Cenomanian–Turonian deeper-water limestones is marked by a fault. Nevertheless, field inve- stigations indicated that no significant relative vertical displacement has occurred between these two limestone packages. An approximately 70 m thick succession situated west of the village of Martinšćica was sampled and analysed (Fig. 2), and its palaeoenvironments and fossil assemblages are described here. The succession defines a lithostratigraphic unit of post-Cenomanian deposits occupying exclusively the southwestern part of the island (see location map, Fig. 1). Several samples containing embedded hippuritids were also collected from deposits belonging to the unit (sampling points CI, CL and CN; Fig. 1). On the basis of detailed geological mapping of the area and micropalaeontological ana- lyses of the samples, the deposits represent laterally equivalent strata of the same age and depositional environment as those analysed at the Martinšćica section. The morphotype nomenclature and terminology for rudist bivalves, e.g. “elevator”, “recumbent”, “bou- quet”, “cluster”, is used according to the scheme of SKELTON & GILI (1991), summarised by ROSS & Key words: Adriatic Carbonate Platform, Turonian, Coniacian, Rudists, Benthic foraminifera, Island of Cres, Croatia. Institute of Geology, Sachsova 2, P.O.Box 268, HR-10000 Zagreb, Croatia; e-mail: korbar@igi.hr Abstract The shallow marine carbonate deposits on the island of Cres, overly- ing deeper-water Cenomanian–Turonian limestones, are characterized by an assemblage of rudists, benthic foraminifera, and associated microfossils. The paucispecific character of the fossil association sug- gests deposition in shallow areas of a carbonate platform, with low current-energies and restricted circulation. Similar assemblages indi- cating similar palaeoenvironments, are common in the Upper Creta- ceous deposits of the Adriatic Carbonate Platform and adjacent areas. The assemblage of rudists (hippuritids) and microfossils indicate the Turonian to (?)Coniacian age of the investigated carbonate suc- cession. The biostratigraphic importance of the so-called “primitive” hippuritids within the micropalaeontologically poorly defined bios- tratigraphy of deposits of this age, is accentuated. Geologia Croatica 56/2 173–185 2 Figs. 2 Pls. ZAGREB 2003 174 Geologia Croatica 56/2 175Korbar & Husinec: Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates... SKELTON (1993). Since radiolitids are poorly preser- ved and of minor biostratigraphic value, only several hippuritid specimens were analysed. 2. PALAEOENVIRONMENTS The strata investigated are characterized by predomi- nantly mud-rich limestones with numerous specimens of Aeolisaccus and Thaumatoporella (Pl. II, Figs. 5, 6). The paucispecific character of the fossil asso- ciation suggests deposition in shallow areas of the carbonate platform, with low current-energies and restricted circulation. Contrary to the older mid- Cretaceous shallow-water limestones that yield several important cosmopolitan foraminiferal index taxa of the family Orbitolinidae (HUSINEC et al., 2000; HUSI- NEC, 2001), the post-Cenomanian strata contain a low-diversity association. However, the association implies that following the deposition of the deeper- water limestones that characterize the underlying succession, the environment again became favourable for population by larger foraminifera and, sporadically, rudists. Rudist bivalves are the most frequent macrofossils within the strata investigated. Radiolitids (Radiolitidae) have been found both in autochthonous (in situ bou- quets, clusters and small lenticular thickets) or para- autochthonous position (displaced locally in the vicinity of their habitats). Rare hippuritids (Hippuritidae) have been found in bouquets characterized by three to four conjoined specimens. In the vicinity of the village of Martinšćica (Martinšćica section, Fig. 2), thick- bedded peritidal limestones (Pl. I, Fig. 1) contain some radiolitid clusters and thickets (biostromes) sporadically including hippuritids. Radiolitids commonly occur in the uppermost part of some beds (Pl. I, Fig. 4). Minor subaerial exposure surfaces are also common at the tops of some beds. Solitary hippuritids (elevators) or small hippuritid bouquets (sample CN–864d contains an embedded bouquet of 4 hippuritid specimens – Pl. I, Fig. 7) were found within subtidal mud-rich limestones. Depositional environments were similar to those characterized by the Turonian to Upper Santonian limestones of neighbouring southern Istria (MORO, 1997; VLAHOVIĆ et al., 2002). Thus, the carbonate platform regime was re-established in the area during the Middle Turonian, following the Cenomanian/Turo- Fig. 1 A) Location map of the island of Cres; B) Location map of the area of post-Cenomanian deposits outcrops (hatched), the sampling points and the Martinšćica section (arrows). 174 G eologia C roatica 56/2 175 K orbar & H usinec: B iostratigraphy of Turonian to (?)C oniacian P latform C arbonates... Fig. 2 S tratigraphic distribution of m icrofossils and rudists w ithin the M artinšćica section (m odified after K O R B A R , 1999). J nrnmrn ]< "Ii '" a ~ ~ ~ ~ ~ I I I I I I ~ ~.a 3 C"l '" r ""C en ;;c en ::i: l:: m~mQ) m OCDcCD 0> -"cn(l)3 CD:::lOC"- Rl :::::J-a--·o CD- 5,.CI.I :f C c: c.o"'C " CD 3 <> iil' CT::e en CD 0 '0) J~mCDC:~ .9 03= Q) :::l.=r=mc: c.:f a CUC'enD) --_. "C -CD c- Q.n ::r CD c':;:::t.,= "" "':$. >< c.., 3 o:1} CD "8~!ilCD I cn en rn ~tT Q) c: 'C en a- CD_.:::l OICD::J 050 a. :::3. CD _~ en=::::!: rn 0a c:g.::e r- 01 3 iil'= "" m CD !il 3· ::r COl ~ cnCD m , z ~ iii o~G C Peritidal, mainly mud-rich and skeletal limestones with common o i~ subaerial exposure surfaces and small radiolitid biostromes. Upper part t~i LITHOLOGY is highly recrystallised and redish coloured with paleokarst 4" features at the top. • it .' .J' Spiro/oculina sp. Biplanata peneropliformis Pseudonummo/oculina heimi -------------------- Aeolisaccus kotori ------------------ Thaumatoporel/a paNovesiculifera 3: Nezzazata simplex c; ?Nummo/oculina sp. i!! OJ ),. :;! ;;c I CD ~ '" c: _. ::J C. "C ~ iii' § _. "C ::r f!l. c: ('j. :::I • ., '" CT ~ 0' " - 0· 0: iil ~ 1 !2 ., CD 3 .. ~ en 5· fir en is' ° if ~ iil -< 0 , en 3 !ll, Pseudocyclammina sphaeroidea "T1 0 Peneroplis paNus en Scandonea samnitica en i'" Vemeuilina sp. en Tritaxia sp. -- Valvulammina sp. Moncharmontia apenninica - - - - - -- Radiolitidae ;;c Hippurites ct. resectus c: - - - C NOTE: Most of the detennined rudists were found in laterally iii -I equivalent strata (see location map on fig. 1). en CT 0 c: .c c: 1} TURONIAN - (?)CONIACIAN ""II APPROX. CHRONOSTRATIGRAPHY CD ~ 176 Geologia Croatica 56/2 177Korbar & Husinec: Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates... nian drowning of the platform (GUŠIĆ & JELASKA, 1990, 1993; JENKYNS, 1991; DAVEY & JENKYNS, 1999; VLAHOVIĆ et al., 2002). Similar associations, and consequently depositional environments, are common in the Upper Cretaceous of the Adriatic Carbonate Platform and adjacent areas. The investigated sequence of strata on the island of Cres can be correlated with the lower part of the Gornji Humac Formation, (above the Gračišće Member) of (?)Late Turonian–Early Campanian age, and was originally described from the island of Brač, (GLOVACKI JERNEJ & JELASKA, 1986; GUŠIĆ et al., 1988; GUŠIĆ & JELASKA, 1990). Similar deposits of (?)Late Turonian–Early Santonian age, are known from the island of Dugi Otok (FUČEK et al., 1990), and from the islands of Ist and Olib (MORO & JELASKA, 1994). On the Trieste–Komen plateau it corresponds to the lower part of the Sežana Formation, which is of Late Turonian–Early Campanian age (JURKOVŠEK et al., 1996). Furthermore, in terms of facies and biostratigraphy, the studied sequence can be correlated with the lower part of the Borgo Grotta Gigante Member from the Trieste Karst (CUCCHI et al., 1989), and the lower part of the Calcari di Aurisina (“Calcari a Rudiste”) from the Isontino Karst (TENTOR et al., 1994). In the central Apennines, the Upper Turonian–Lower Campanian carbonate deposits are also characterized by predominantly mud-rich lithologies, sporadically containing numerous fragments of radiolitids and hippuritids, and with microfossil associations that become richer and more diversified upwards in the section (CHIOCCHINI et al., 1994). In general, this distribution represented by radiolitids dominating hippuritids in more internal peritidal cycles, seems to be typical of the central/southern Tethyan carbonate platforms (CARANNANTE et al., 2000; STÖSSEL & BERNOULLI, 2000; MORO et al., 2002; KORBAR, 2003). 3. SYSTEMATIC PALAEONTOLOGY 3.1. Rudists Analysed rudists are referred to the family Hippuritidae according to the diagnoses of DECHASEAUX & COOGAN (1969), SKELTON (1978) and SKELTON & SMITH (2000). Rudist determinations were made according to descriptions of European rudist fauna (DOUVILLÉ, 1890–94; TOUCAS, 1903–04) and des- criptions of rudist fauna collected in the neighbouring areas (POLŠAK, 1967b). Order HIPPURITOIDA NEWEL, 1965 Superfamily Hippuritoidea GRAY, 1848 Family Hippuritidae GRAY, 1848 Genus Hippurites LAMARCK, 1801 Hippurites sp., cf. H. resectus DEFRANCE, 1821 (Pl. I, Figs. 2, 3, 5–8) 1903 Hippurites (Orbignya) requieni MATHERON; TOUCAS, text-fig. 23–29. 1903 Hippurites (Orbignya) requieni var. resecta DEFRANCE; TOUCAS, text-fig. 30, 31. 1903 Hippurites (Orbignya) requieni var. subpolygonia TOUCAS, text-fig. 32. 1967 Hippurites (Hippuritella) incisus DOUVILLÉ; POLŠAK, p. 109, text-fig. 33. 1997 Hippurites requieni; MORO, pl. 9, fig. 3. 1999 Hippurites requieni MATHERON; CAFFAU, pl. 2, fig. 1. 2002 Hippurites cf. requieni/incisus; VLAHOVIĆ et al., p. 126, text-fig. 5. Material: Ten limestone samples containing embedded rudists were collected within the Martinšćica sec- tion (Figs. 1, 2) – CMB (1 specimen), and within laterally equivalent strata occupying the investigated area (location map of the sampling points CI, CL and CN on Fig. 1): CI–861 (1 specimen), CL–1195 (2 specimens), CN–864 (1 specimen), CN–864a (3 specimens), CN–864c (1 specimen with broken ligamental pillar), CN–864d (1 specimen as a part of a bouquet of four hippuritid specimens), CN–952 (1 specimen), CN–953 (1 specimen) and one unlabelled sample (1 specimen). All of these 13 specimens are transverse sections of right valves embedded in slightly recrystallized limestones. The samples are stored at the repository of the Institute of Geology in Zagreb (Croatia). Description: The valves are 12–30 mm in diameter. Anterior (ligamental) pillars are triangular with wide bases and truncated apical parts. Central pillars are slightly wider and shorter than the more protruding posterior one. Central and posterior pillars are characterized by rounded heads. Some specimens are characterized by central and posterior pillars that are as long as the anterior ones, while the posterior pillars have a slightly narrower bases than the central ones. The angles between anterior and posterior pillars ranged between 80 and 110 degrees. Stratigraphic distribution: Turonian (TOUCAS, 1903–04; MAMUŽIĆ et al., 1976; SÁNCHEZ, 1981; PHILIP, 1998; VLAHOVIĆ et al., 2002), Upper Turonian (POLŠAK, 1967b; SLIŠKOVIĆ, 1968; POLŠAK & MAMUŽIĆ, 1969; POLŠAK et al., 1982; CAFFAU, 1999), Upper Turonian–?Coni- acian (STEUBER, 1999a) or Middle–Upper Turo- 176 Geologia Croatica 56/2 177Korbar & Husinec: Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates... nian (PHILIP in HARDENBOL et al., 1998; PLA- TEL, 1998; SIMONPIÉTRI, 1999). Remarks: There are a few transverse sections of right valves of Hippurites requieni MATHERON shown in TOUCAS (1903–04) that are characterized by a wide range of the angles between the anterior (ligamental) pillar and the second pillar. It is not clear what the reason is for such a strict value as 120° for a determination of the species as established by TOUCAS (1903–04) in the text. Moreover, these angles vary in relation to the departure of the right valve transverse section from circularity, which in turn depends on the available space during growth (STEUBER, 1999a). That is why we are of the opinion that all specimens described in this paper are consistent with the description of the morphologically variable species Hippurites resectus DEFRANCE revised by SIMONPIÉTRI (1999). According to the same author Hippurites requieni MATHERON represents a synonym of H. resectus DEFRANCE. Complete synonymy lists of all synonyms, including references, are given in SÁNCHEZ (1981) and STEUBER (1999c). The small number and poor preservation of collected specimens did not allow morphometric analysis. Therefore, specimens are referred to the species by comparison of the internal morphological cha- racters of their right valves (i.e., resemblance of morphology of the pillars and their distribution along the shell interior). We are aware that determination based only on pillar morphology can be difficult and is not always reliable (STEUBER, 1999a). Consequently, our determinations are tentative, but can be used for the purpose of this paper (i.e., to prove post-Cenomanian carbonate deposition on the island of Cres). 3.2. Microfossils Ten samples were obtained from the Martinšćica section (see Fig. 2) and were examined in thin sec- tions. The following microfossil taxa have been deter- mined: Aeolisaccus kotori RADOIČIĆ, Biplanata peneropliformis HAMAOUI & SAINT-MARC, Mon- charmontia apenninica (DE CASTRO), Nezzazata simplex OMARA, ?Nummoloculina sp., Peneroplis parvus DE CASTRO, Pseudocyclammina sphaeroidea GENDROT, Pseudonummoloculina heimi (BONET), Scandonea samnitica DE CASTRO, Spiroloculina sp., Thaumatoporella parvovesiculifera (RAINERI), Trita- xia sp., Valvulammina sp. and Verneuilina sp. Other foraminifera found in the area investigated belong to the families Miliolidae, Nezzazatidae, Charentiidae, Coskinolinidae, Spiroloculinidae, Hauerinidae, Ver- neulinidae, Tritaxidae, and Valvulinidae (according to LOEBLICH & TAPPAN, 1988). They are not important in terms of biostratigraphy because of their relatively long stratigraphic ranges. The morphologic characteristics of the biostratigraphically and palaeoeco- logically most important species are briefly discussed, while their stratigraphic ranges are discussed in the following chapter. Order FORAMINIFERIDA EICHWALD, 1830 Suborder TEXTULARIINA DELAGE & HÉROUARD, 1896 Superfamily Biokovinacea GUŠIĆ, 1977 Family Charentiide LOEBLICH & TAPPAN, 1985 Genus Moncharmontia DE CASTRO, 1966 Moncharmontia apenninica DE CASTRO, 1966 (Pl. II, Fig. 1) 1966 Neoendothyra apenninica DE CASTRO; DE CASTRO, p. 14–19, text-figs. 5, 6, pls. I–V 1988 Moncharmontia apenninica DE CASTRO; GUŠIĆ et al., pl. II, figs: 8, 10, 11 1990 Moncharmontia apenninica DE CASTRO; FUČEK et al., pl. II: fig. 8 1994 Moncharmontia apenninica DE CASTRO; MORO & JELASKA, pl. II: fig. 5 Material: A few specimens were observed in thin sections (samples CMA–6, CMA–7, CMA–8, and CMA–10; Fig. 2). The samples and thin sections are stored at the repository of the Institute of Geology in Zagreb (Croatia). Description: Test planispirally enrolled, involute, with- out uncoiled stage. Wall finely agglutinated, outer wall seemingly perforated, inner visibly smooth. Aperture cribrated with pores. Remarks: Despite the lack of appropriate sections and small number of specimens studied, they are attributed to Moncharmontia apenninica due to their characteristic overall morphology. Stratigraphic distribution: Turonian–Campanian (DE CASTRO, 1966). Superfamily Loftusiacea BRADY, 1884 Family Cyclamminidae MARIE, 1941 Subfamily Choffatellinae MAYNC, 1958 Genus Pseudocyclammina YABE & HANZAWA, 1926 Pseudocyclammina sphaeroidea GENDROT, 1968 (Pl. II, Fig. 2) 1968 Pseudocyclammina sphaeroidea GENDROT, p. 674–675, pl. IV: figs. 1–5 1990 Pseudocyclammina sphaeroidea GENDROT; FUČEK et al., pl. II: fig. 7 1991 Pseudocyclammina sphaeroidea GENDROT; FUČEK et al., pl. II: fig. 6 178 Geologia Croatica 56/2 179Korbar & Husinec: Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates... Material: Several specimens were observed in thin sections (samples CMA–5, CMA–6, CMA–7, and CMA–8; Fig. 2). The samples and thin sections are stored at the repository of the Institute of Geology in Zagreb (Croatia). Description: Test involutely enrolled, outer form infla- ted, almost sphaerical. Final coil with clear sutures slightly depressed. Endoskeleton with labyrinthic septa. Wall agglutinated. Cribrate aperture. Remarks: The specimens were observed in equatorial and oblique sections. Stratigraphic distribution: Turonian–Senonian (see text – section 4). Suborder MILIOLINA DELAGE & HÉROUARD, 1896 Superfamily Soritacea EHRENBERG, 1839 Family Soritidae EHRENBERG, 1839 Subfamily Praerhapydionininae HAMAUI & FOURCADE, 1973 Genus Scandonea DE CASTRO, 1971 Scandonea samnitica DE CASTRO, 1971 (Pl. II, Figs. 3, 4) 1971 Scandonea samnitica DE CASTRO, p. 5–6, 16– 65, text-figs. 1–10, 12–15, pls. I–XII, XV–XVII, 1988 Scandonea samnitica DE CASTRO; GUŠIĆ et al., pl. I: fig. 5 1990 Scandonea samnitica DE CASTRO; FUČEK et al., pl. II: figs. 3–6 Material: Several specimens were observed in thin sections (samples CMA–3, CMA–5, CMA–6, CMA–7, CMA–8, and CMA–10; Fig. 2). The samples and thin sections are stored at the repository of the Institute of Geology in Zagreb (Croatia). Description: Test enrolled, initially in various planes, later planispiral and involute. Final stage may be uncoiled and rectilinear. Endoskeleton with basal layer and rudimentary(?) subepidermal partitions in the adult chambers and in the chambers of adult stage. Wall calcareous, imperforate, porcellaneous, outer wall very thick. Cribrate aperture. Remarks: The specimens were observed in median and axial sections. Stratigraphic distribution: Turonian–Senonian (see text – section 4). 4. DISCUSSION The Hippuritid taxon Hippurites resectus DEFRANCE (including synonyms, see section 3.1.), that chara- cterizes the investigated area, is well known from numerous localities on the Adriatic Carbonate Platform and adjacent areas. This taxon has been commonly attributed to the Upper Turonian (POLŠAK, 1965; SLIŠKOVIĆ, 1968; POLŠAK & MAMUŽIĆ, 1969; MAMUŽIĆ et al., 1976; POLŠAK et al., 1982; GUŠIĆ & JELASKA, 1990; FUČEK et al., 1990; CESTARI & SARTORIO, 1995; CAFFAU, 1999) or an even wider range, e.g. Upper Turonian–?Coniacian (STEUBER, 1999a) and Upper Turonian–Lower Santonian (MORO, 1997; MORO & JELASKA, 1994). On the other hand, SIMONPIÉTRI (1999) revised the taxonomy and stratigraphy of a few “primitive” hippuritid species from Western Europe, including type specimens, and concluded that H. resectus is Middle– Late Turonian in age. Furthermore, recent results based on strontium iso- tope stratigraphy and morphometric analyses of the Hippuritidae from Central and Eastern Europe, imply that Vaccinites cornuvaccinum and V. inaequicostatus (see CESTARI et al., 1996; STEUBER, 1999a), traditio- nally considered as Santonian–Early Campanian in age (SÁNCHEZ, 1981; POLŠAK et al., 1982; STEUBER, 1999a), are no younger than Coniacian (STEUBER, 1999b; STEUBER & HÖFLING, 1999; STEUBER, 2001). However, the revised chronostratigraphy of these taxa should be confirmed for the Adriatic Car- bonate Platform domain analyzing the specimens from southern Istria (localities in POLŠAK, 1967b). Nevertheless, there is a need for biochronostratigraphic recalibration according to the new Cretaceous bio- chronostratigraphy (HARDENBOL et al., 1998). Finally, the association of hippuritids described in this paper suggests the Middle–Late Turonian age of the strata investigated. The microfossil association does not contain many stratigraphically relevant taxa. Moreover, the stra- tigraphic ranges of the only three “index” species are still disputed. The least debate surrounds the first appearance of Moncharmontia apenninica DE CAS- TRO, which is the Upper Turonian (e.g. DE CASTRO, 1966; GUŠIĆ & JELASKA, 1990; CHIOCCHINI et al., 1994). However, various authors have given very different data on the stratigraphic range of Scandonea samnitica DE CASTRO: Lower Senonian (CHIOCCHI- NI et al., 1994), Lower Santonian–Lower Campanian (HARDENBOL et al., 1998), Upper Santonian (BILOTTE, 1984, 1986), and Turonian–Santonian (DE CASTRO, 1971) – maybe even to Maastrichtian (FLE- URY, 1980; GUŠIĆ & JELASKA, 1990). This is also the case with Pseudocyclammina sphaeroidea GEN- DROT: Turonian–Santonian (FLEURY, 1980), Coni- acian–Santonian (BILOTTE, 1984; HARDENBOL et al., 1998), and Santonian (GENDROT, 1968). In central Croatia, the association of these three “index” species occurs in the Lower Senonian rudist limestones (VELIĆ, 1973; VELIĆ et al., 1980). FUČEK et al. (1991) reported on resedimented shallow-marine bio- 178 Geologia Croatica 56/2 179Korbar & Husinec: Biostratigraphy of Turonian to (?)Coniacian Platform Carbonates... clastic material containing the aforementioned forami- nifera, interbedded with deeper-water carbonates from Dugi otok Island. Undisturbed autochthonous layers of pelagic limestone contain planktonic foraminifera that clearly indicate the Middle to Late Turonian age of these deposits. However, there is one additional clue to narrow the stratigraphic range of the examined sequen- ce, namely, that foraminifera which appear in the Santonian on the Adriatic Carbonate Platform (Dicycli- na schlumbergeri MUNIER-CHALMAS, Accordiella conica FARINACCI, Keramospherina tergestina (STA- CHE), Scandonea mediterranea DE CASTRO, and Nummofallotia apula (LUPERTO SINNI) – e.g. GUŠIĆ et al., 1988; GUŠIĆ & JELASKA, 1990), were not found in the study area. Therefore, based on the microfossil association, and knowing that underlying deeper-water deposits are dated to the latest Cenoma- nian–earliest Turonian, the age of the investigated sequence on the island of Cres is likely to be (Middle) Turonian to (?)Coniacian. Additional investigations and correlations with regional and global stratigraphic charts and sequence stratigraphy, as well as possible strontium isotope dating are required. Neither rudists nor microfossil benthic assemblages allow (at least not according to our present knowledge) greater stratigraphic resolution within carbonate platform domains of this age. Acknowledgements This paper is a result of comprehensive geological investigations by the “Adriatic team” of the Institute of Geology in Zagreb, supported by the Ministry of Science and Technology of the Republic of Croatia through the project No. 0181–0101: Geological Map of the Republic of Croatia (scale 1:50.000). We wish to thank Ladislav FUČEK who introduced us to the geology of the island of Cres. The help in microfossil and rudist determinations by Ivo VELIĆ and Boško KOROLIJA is greatly appreciated. We acknowledge our colleagues Nenad OŠTRIĆ, Božo PRTOLJAN and Igor VLAHOVIĆ for their valuable suggestions and support during the fieldwork. Finally, we are grateful to Ivan GUŠIĆ, Josip TIŠLJAR and Peter W. SKELTON for very useful suggestions that greatly improved the manuscript. 5. 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Upper part of the Martinšćica section. Turonian to (?)Coniacian. 3 Hippurites cf. resectus DEFRANCE, sample CN–864c. Turonian to (?)Coniacian. 4 Radiolitid thicket (biostrome) at the top of a thick bed of peritidal limestone. Central part of the Martinšćica section. Turonian to (?)Coniacian. 5 Hippurites cf. resectus DEFRANCE, sample CN–864. Turonian to (?)Coniacian. 6 Hippurites cf. resectus DEFRANCE, sample CN–953. Turonian to (?)Coniacian. 7 Hippurites cf. resectus DEFRANCE, sample CN–864d. Turonian to (?)Coniacian. 8 Hippurites cf. resectus DEFRANCE, sample CL–1195. Turonian to (?)Coniacian. 182 Geologia Croatica 56/2 183 1 4 76 8 5 3 2 Korbar & Husinec PLATE I 184 Geologia Croatica 56/2 185 PLATE II Microfossils from the Martinšćica section (see Fig. 2). 1 Moncharmontia apenninica DE CASTRO, sample CMA–7, 70x. Turonian to (?)Coniacian. 2 Pseudocyclammina sphaeroidea GENDROT, sample CMA–5, 55x. Turonian to (?)Coniacian. 3, 4 Scandonea samnitica DE CASTRO, samples CMA–5 (3) and CMA–3 (4), 55x. Turonian to (?)Coniacian. 5, 6 Aeolisaccus kotori RADOIČIĆ – Thaumatoporella parvovesiculifera (RAINERI) wackestone, sample CMA–9, 55x. Turonian to (?)Coniacian. 184 Geologia Croatica 56/2 185 1 2 3 4 65 Korbar & Husinec PLATE II 186 Geologia Croatica 56/2