2016 | 69/2 | 187–194 | 4 Figs. | 1 Tab. | 1 Pl. | www.geologia-croatica Journal of the Croatian Geological Survey and the Croatian Geological Society 1. INTRODUCTION The Upper Cretaceous shallow-water limestones of the Periadri- atic Region (Adriatic, Apenninic, and Apulian carbonate plat- forms) contain a rich fauna of large-sized benthic foraminifera, many of them with special biostratigraphic importance (e.g., TORRE, 1966; LUPERTO SINNI, 1976; DE CASTRO, 1974; CVETKO TEŠOVIĆ et al., 2001; KORBAR & HUSINEC, 2003; VELIĆ, 2007; CHECCONI et al., 2008; FRIJIA et al., 2015). In the Croatian part of the Adriatic-Dinaridic carbonate platform, a shallow-water facies rich in benthic foraminifera known as the Pučišća Formation was originally described from the island of Brač (GUŠIĆ & JELASKA, 1990). The island of Brač is situated along the central part of the Adriatic-Dinaridic Carbonate Plat- form (ADCP; cf. JENKYNS, 1991; GUŠIĆ & JELASKA, 1990; PAMIĆ et al., 1998; JELASKA, 2002) or Adriatic Carbonate Plat- form (AdCP; cf. VLAHOVIĆ et al., 2005). During the Mesozoic, several long-lived isolated carbonate platforms existed in the Me- Cretaciclavulina gusici n. gen., n. sp. (?family Valvulinidae BERTHELIN, 1880), a new larger benthic foraminifer from the lower Campanian of Brač Island, Croatia Felix Schlagintweit1 and Blanka Cvetko Tešović2 1Lerchenauerstr. 167, D-80935 München, Germany; (corresponding author: felix.schlagintweit@gmx.de) 2University of Zagreb, Faculty of Science, Department of Geology, Horvatovac 102a, Zagreb, Croatia; (bcvetko@geol.pmf.hr) doi: 10.4154/gc.2016.17 Abstract The larger benthic foraminifera Cretaciclavulina gusici n. gen., n. sp. is described from the lower Campanian Pučišća Formation of the Island of Brač, Croatia. With its elongate test, trochospiral to uniserial coiling, simple chambers, paraporous wall structure, and areal aperture provided with a cribrate apertural plate, Cretaciclavulina is tentatively placed into the family Valvulinidae BERTHELIN, 1880. Besides Neobalkhania bignoti CHERCHI, RADOIČIĆ & SCHROEDER, 1991, Fleuryana adriatica DE CASTRO, DROBNE & GUŠIĆ, 1994, and Reticulinella fleuryi CVETKO, GUŠIĆ & SCHROEDER, 1997, Cretaciclavulina gusici represents the fourth benthic foraminifera newly described from the Upper Cretaceous shallow-water carbonates of Brač Island. Article history: Manuscript received August 19, 2015 Revised manuscript accepted March 30, 2016 Available online June 1, 2016 Keywords: Benthic foraminifera, Wall structure, Valvulinidae, Palaeotextulariidae, Upper Cretaceous, Croatia diterranean region (the former central Tethys; present-day peri- Adriatic area). The ADCP was the largest of these platforms with relatively well preserved, mainly shallow-marine successions oc- casionally interrupted by episodes of emersion or drowning. From the Pučišća Formation of Brač Island, three benthic for a- minifera have already been introduced from thin-section mate rial: Neobalkhania bignoti CHERCHI, RADOIČIĆ & SCHROEDER, 1991, Fleuryana adriatica DE CASTRO, DROBNE & GUŠIĆ, 1994, and Reticulinella fleuryi CVETKO, GUŠIĆ & SCHROEDER, 1997. Another new taxon is reported here is Cretaciclavulina gusici n. gen., n. sp. 2. GEOLOGICAL SETTING 2.1. Lithostratigraphy On the Island of Brač, situated along the central part of the Croa- tian Adriatic coast (Fig. 1), an almost complete, relatively undis- Figure 1. Map showing the location and geology of Brač Island, and type locality of Cretaciclavulina gusici n. gen., n. sp. (modified after GUŠIĆ & JELASKA, 1990, CVETKO TEŠOVIĆ et al., 2001 and STEUBER et al., 2005). G eo lo gi a C ro at ic a Geologia Croatica 69/2188 ŠIĆ & JELASKA, 1990), ranging in age from Cenomanian to Maastrichtian (Fig. 2): – The Milna Formation (Cenomanian) comprises bioclastic (including foraminifera, rudists and other mollusca) wackestones to grainstones alternate with microbial lami- nites, occasional slump features, and rare intraformational breccias (GUŠIĆ & JELASKA, 1990; KORBAR et al., 2012). – The Sveti Duh Formation (uppermost Cenomanian–Lower Turonian) comprises pelagic skeletal wackestones with planktonic foraminifera and calcispheres indicate drown- turbed, and well-exposed Upper Cretaceous succession of the ADCP is exposed. This succession has served as a representative example for the Upper Cretaceous shallow-water carbonate de- velopment of the ADCP (Figs. 1, 2). Palaeogene deposits are also present along the northwestern and, as scattered outcrops, along the southeastern coast of the island (Fig. 1). The Upper Cretaceous platform limestones represent a thick „layer-cake” sedimentary succession (up to 1500 m), consisting predominantly of small-scale shallowing-upward cycles (GUŠIĆ & JELASKA, 1990). The succession has been subdivided into six lithostratigraphic units (PEJOVIĆ & RADOIČIĆ, 1987; GU- Figure 2. Stratigraphic synthesis of the Upper Cretaceous deposits of Brač Island with detailed lithology and selected foraminiferal assemblage of Pučišća Forma- tion (adapted from GUŠIĆ & JELASKA, 1990, CVETKO TEŠOVIĆ et al., 2001 and STEUBER et al., 2005). G eologia C roatica Felix Schlagintweit and Blanka Cvetko Tešović: Cretaciclavulina gusici n. gen., n. sp. (?family Valvulinidae BERTHELIN, 1880) ... 189 ing of the ADCP (JENKYNS, 1991; GUŠIĆ & JELASKA, 1990; DAVEY & JENKYNS, 1999; KORBAR et al., 2012). – The Gornji Humac Formation (Upper Turonian–Lower Campanian) comprises oncoid-bearing beds in the lower part (e.g. the „Gračišće Oncolite” Member) during the Late Turonian–Early Coniacian, which cap the underlying pela- gic deposits and evidence a shallowing and reinstallation of carbonate platform environments, which were gradually less restrictive and more favourable for populations of shal- low-water benthic organisms. – The Dol Formation (Coniacian–Lower Campanian) com- prises micrites with abundant calcispheres and planktonic foraminifera indicating a second Late Cretaceous pelagic episode. – The Pučišća Formation (Santonian–Middle Campanian): platform sediments with rudists in parautochthonous posi- tion and shallow-water bioclastic limestones indicate the gradual infilling of the intraplatform trough, known as the Brač „Marble” Member. With the progradation of the plat- form, the protected back-margin environments gradually occupied larger areas until they completely overlaid the Brač „Marble” Member. These environments are repre- sented by the two superpositional-lateral subunits of the Rasotica member (rudist biostromes, bioclastic floatstones to rudstones and foraminiferal wackestones/packstones with rich and diverse assemblages of larger benthic imper- forate foraminifera) and the Lovrečina member (uppermost member characterized by regularly developed shallowing- upward sequences with features indicating emergence con- ditions with subaerial erosion at the top, probably reflecting a global drop of sea level in the Middle to Late Campanian). – The Sumartin Formation (Upper Campanian–Maastricht- ian) represents the regressive cycles of the Maastrichtian, above the Late Campanian emersion, which were deposited in peritidal environments. The new benthic foraminifer described in the present paper was observed in the Campanian deposits of the uppermost part of the Gornji Humac and are more frequent in the Pučišća For- mation (Rasotica and Lovrečina members). 2.2. Biostratigraphy PEJOVIĆ & RADOIČIĆ (1987) subdivided the Upper Creta- ceous deposits into six formations mainly based on benthic fora- minifera and rudists. Six formations were also recognized by GU ŠIĆ & JELASKA (1990), but their litho- and chronostratigra- phic interpretation differs from that of PEJOVIĆ & RADOIČIĆ (1987). They emphasized the diachronous character of some for- mation boundaries (Fig. 2) and subdivided some of them into smaller units. Rudist bivalves and benthic microfossils have been studied comprehensively as biostratigraphic markers for the up- per Cretaceous succession of Brač (POLŠAK et al., 1982; GUŠIĆ & JELASKA, 1990; CVETKO TEŠOVIĆ et al., 2001, KORBAR, 2003; STEUBER et al., 2005 and references therein) and the type localities of several taxa are located on the island. The Pučišća Formation contains especially rich assemblages of larger benthic foraminifera dominated by various imperforate taxa in the Rasotica and Lovrečina members and hyaline forami- nifera in the Brač „Marble” Member. These assemblages were used for the interpretation of stratigraphic and palaeoenviron- mental features (GUŠIĆ & JELASKA, 1990; CVETKO TE ŠO- VIĆ et al., 2001). CVETKO TEŠOVIĆ et al. (2001) described these assemblages in detail including taxonomic, phylogenetic, stratigraphic and palaeoecologic aspects. The Late (but not latest) Campanian age of the Pučišća Formation is largely based on the age determination of the Brač „Marble” Member. GUŠIĆ & JELASKA (1990) gave stratigraphic priority to the relevant and well-studied larger benthic foraminifera (orbitoidids and sidero- litids). Based on numeric ages derived from strontium-isotope stratigraphy (SIS) of low-Mg calcite of rudist shells, STEUBER et al. (2005) revised the chronostratigraphy of the Coniacian– Maastrichtian platform carbonates of the island of Brač. Accord- ing to the strontium-isotope stratigraphy, the Pučišća Formation is mid-Santonian to late Middle Campanian in age. Based on benthic foraminifera, especially Calveziconus lecalvezae CAUS & CORNELLA, the samples containing Cretaciclavulina gusici n. gen. n. sp. can be assigned to the lower Campanian (see revised ranges of FRIJIA et al., 2015). 3. MATERIAL AND REPOSITORY The micropalaeontological analysis of samples from the Pučišća Formation was performed on about 200 thin sections. Sections of Cretaciclavulina gusici n. gen, n. sp. were only observed in 15 of them. The investigated samples are the property of the Croa- tian Geological Survey and their repository (inventory numbers: 10807−10815) is currently in the Geological-Palaeontological De- partment of the Croatian Natural History Museum, Demetrova 1, Zagreb, Croatia. 4. MICROPALAEONTOLOGY 4.1. Description of the new taxon Phylum: Foraminifera D’ORBIGNY, 1826 Class: Globothalamea PAWLOWSKI et al., 2013 Order: Ataxophragmiina FURSENKO, 1958 Superfamily: Textulariacea EHRENBERG, 1838 Family:?Valvulinidae BERTHELIN, 1880 Remarks: With its elongate test, trochospiral later becom- ing uniserial, the simple chambers, a paraporous wall structure, and probable cribrate apertural plate, Cretaciclavulina is tenta- tively placed into the family Valvulinidae BERTHELIN, 1880. According to LOEBLICH & TAPPAN (1987, p. 181), the Valvuli- nidae range in age from the Palaeocene to the Holocene. Cretaciclavulina n. gen. Type species: Cretaciclavulina gusici n. gen., n. sp. Origin of the name: Composite name referring to the Cre- taceous and the genus Clavulina D’ORBIGNY. Diagnosis: Test elongate, trochospiral (most likely triserial) to uniserial, with a short intermediate biserial stage between these. Chambers simple, broad low, enlarging in the triserial stage and of nearly constant width in the uniserial stage. Wall thick ag- glutinating, and canaliculate (paraporous), possibly with an inner calcareous (?aragonitic) layer. Foramen single interiomarginal in the trochospiral and areal in the uniserial part. Aperture areal, provided with a cribrate apertural plate. Remarks: The wall structure combined with the elongate test and its trochospiral to uniserial chamber arrangement allow a comparison of Cretaciclavulina with some representatives of the family Palaeotextulariidae GALLOWAY, 1933, Valvulinidae BERTHELIN, 1880, and partly also the Ataxophragmiidae SCHWAGER, 1877, Verneuilinidae CUSHMAN, 1911 as well as Pseudogaudryinidae LOEBLICH & TAPPAN, 1985 (Fig. 3A). The wall of Cretaciclavulina displays closely spaced, fine and more or less parallel, more rarely bifurcating canaliculi or parapores that are not open to the exterior, but end blindly shortly G eo lo gi a C ro at ic a Geologia Croatica 69/2190 before the outer test surface (see BANNER et al., 1991; HOT- TINGER et al., 1990; HOTTINGER, 2006, for details) (Fig. 3A). This thin outer „pavement” is commonly eroded. Canaliculi ap- pear scarcer to absent in the septa. The phylogentic relationship concerned with the appearance of such „false keriothecae” (VA- CHARD et al., 2004) is still poorly understood and requires fur- ther study (see also RIGAUD et al., 2015). In the adult chambers of some Cretaciclavulina the outline of an inner calcareous layer, morphologically close to that of the Palaeotextulariidae (Fig. 3B), is preserved. In Palaeotextulariidae, however, the inner layer is clearly yellowish and fibrous whereas that observed in Cretaciclavulina is recrystallized into sparite (?originally aragonitic). It is worth mentioning here that a yellow- ish inner fibrous calcitic layer was reported recently from the Up- per Cretaceous (Coniacian) genus Siphodinarella (SCHLAGINT- WEIT et al., 2014). Axial sections (that usually do not allow bi se rial to be distinguished from the triserial forms) of Cretaci­ clavulina show morphological resemblance to large-sized pa- laeozoic Palaeotextulariid genera such as Climacammina BRADY (Fig. 4A), Deckerella CUSHMAN & WATERS (Fig. 4B), and Palaeobiginerina GALLOWAY. These taxa are biserial becom- ing uniserial in the adult part. The wall structure is originally described as „calcareous, microgranular, commonly with an in- ner radial fibrous layer” (LOEBLICH & TAPPAN, 1987, p. 218). This view was corrected by PILLER (1990) evidencing the ag- glutinating character of the outer layer. The uniserial stage in Cretaciclavulina does not abruptly fol- low the trochospiral (triserial) stage, but with a mediating short biserial stage. Examples of such triserial-biserial-uniserial tests are for example the agglutinated Lower Cretaceous Spiroplecti­ nata CUSHMAN, 1927 of the Verneuilinidae (TYSZKA & THIES, 2001; KAMINSKI et al., 2011) and Gerochella NEAGU, 1997 (Fig. 4C) of the Ataxophragmiidae, the Eocene to Holocene Goesella CUSHMAN, 1933 of the Valvulinidae (Fig. 4D), as well as the Late Cretaceous (Campanian) Rectogerochammina KA- MINSKI, CETEAN & NEAGU, 2010 of the family Prolixoplecti- dae LOEBLICH & TAPPAN, 1985. The four mentioned genera exhibit a solid (non-canaliculate) wall different from that of Cre­ ta ciclavulina. Forms with a serial and later uniserial test as well as a cana- liculate wall structure are reported from the various representa- tives of the family Valvulinidae BERTHELIN, with the genera Clavulina D´ORBIGNY, 1826, Cribrogoesella CUSHMAN, 1935, and Gyrovalvulina LOEBLICH & TAPPAN, 1985 as well as of the family Pseudogaudryinidae LOEBLICH & TAPPAN, 1985, with the genera Clavulinopsis BANNER & DESAI, 1985, and Pseudoclavulina CUSHMAN, 1936. The differences be- tween these genera and Cretaciclavulina can be roughly summa- rized as follows (only the main differences are stressed; ages and generic features acc. to LOEBLICH & TAPPAN, 1987): – Clavulina D’ORBIGNY, 1826 (Palaeocene to Holocene) (Fig. 4E): triangular early and uniserial adult stage (3-1 chamber arrangement opposed to 3-2-1 in Cretaciclavu­ Figure 3. Details of the wall structure of Cretaciclavulina gusici n. gen., n. sp. A) Detail from Pl. 1D showing rare distal pore bifurcations (arrows). Thin-section S2N124. B) Detail from the holotype specimen of Pl. 1A showing the inner recrystallized calcareous layer. Thin-section 514 K3V71/5. Figure 4. Foraminiferal genera that are compared with Cretaciclavulina n. gen. A) Climacammina antiqua (BRADY), early Carboniferous of Scotland (from LOEBLICH & TAPPAN, 1987, pl. 228, fig. 11). B) Deckerella clavata CUSHMAN & WATERS, late Carboniferous of Texas (from LOEBLICH & TAPPAN, 1987, pl. 229, fig. 3). ) Gerochella cylindrica NEAGU, Valanginian of Romania (from NEAGU, 1997, Fig. 1/40–41). D) Goesella rotundata (CUSHMAN), Holocene of Philippine Islands (from LOEBLICH & TAPPAN, 1987, pl. 200, fig. 6). E) Clavulina parisiensis d´ORBIGNY, Middle Eocene of France (from LOEBLICH & TAPPAN, 1987, pl. 200, fig. 3). F) Cribrogoesella robusta (BRADY), Holocene of Pernambuco, Atlantic (from LOEBLICH & TAPPAN, 1987, pl. 201, fig. 3), G) Clavulinopsis hofkeri BANNER & DESAI, Upper Cretaceous (Campanian) of Texas, USA (from LOEBLICH & TAPPAN, 1987, pl. 196, fig. 3). H) Bigenerina nodosaria D´ORBIGNY, Holocene of France (from LOEBLICH & TAPPAN, 1987, pl. 191, fig. 1). Scale bars = 0.3 mm. G eologia C roatica Felix Schlagintweit and Blanka Cvetko Tešović: Cretaciclavulina gusici n. gen., n. sp. (?family Valvulinidae BERTHELIN, 1880) ... 191 lina; see also the comparative table in WEIDICH, 1988); finely bifurcating pores are sealed internally by an organic lining (that may simply not be preserved in Cretacicla­ vulina?); aperture with an imperforate toothplate; tooth- plates of successive chambers oriented 120 degrees apart. – Cribrogoesella CUSHMAN, 1935 (Miocene to Holocene) (Fig. 4F): early trochospiral stage with up to five chambers; rapidly reducing to three, then biserial and finally unise- rial; both lateral walls and septa strongly canaliculate; ap- erture cribrate in the uniserial stage (opposed to single, and areal in Cretaciclavulina). – Gyrovalvulina LOEBLICH & TAPPAN, 1985 (Eocene): „triserial and triangular early stage and later chambers in a loose spiral, with progressively fewer chambers per whorl, until the final chamber nearly completely encircles the axis” (LOEBLICH & TAPPAN, 1985, p. 213). – Clavulinopsis BANNER & DESAI, 1985 (Campanian to Maastrichtian) (Fig. 4G): test triangular (throughout!); early stage triserial, later abruptly becoming uniserial (3-1 cham- ber arrangement opposed to 3-2-1 in Cretaciclavulina). – Pseudoclavulina CUSHMAN, 1936 (Upper Cretaceous to Lower Eocene): early stage triangular, then uniserial (3-1 chamber arrangement) thereby reducing abruptly test di- ameter; aperture terminal, but without a distinct tooth. Last but not least, the genus Bigenerina D’ORBIGNY, 1826 (Eocene to Holocene acc. to LOEBLICH & TAPPAN; 1987) shows an early biserial stage, later becoming abruptly uniserial, and an agglutinating, canaliculate wall (Fig. 4H). It is worth mentioning here that the Mesozoic-Cenozoic taxa that were compared with Cretaciclavulina were all described from isolated specimens recovered from deeper water marly litho logies. Cretaciclavulina instead is reported from typical shallow-water platform carbonates. Cretaciclavulina gusici n. sp. Fig. 3, Pl. 1 1990 Unidentified or unknown foraminifera – GUŠIĆ & JELSKA, pl. 15, figs. 8, 9. Origin of the name: Dedicated to Ivan Gušić (Zagreb) for his contributions to the taxonomy of benthic foraminifera. The new taxon was also illustrated for the first time by GUŠIĆ & JE- LASKA (1990) (see synonymy). Holotype: Subaxial section illustrated in Pl. 1, Fig. A, and details in Pl. 1, Fig. G, and Fig. 3B, thin-section inv. no. 10807 (514 K3V71/5). Paratypes: Specimens illustrated in Pl. 1, Figs. B–F, H–O (inv. no. 10808–10815). Type-locality: On the east side of the Otočac cove (northeast coast of the Brač island). Approximate coordinates: 43.352294oN, 16.796578o (Fig. 1). Type-level: Lower Campanian; the highest levels of the Gornji Humac Formation, (Upper Turonian–Lower Campanian), and the Rasotica and Lovrečina Members (Lower–Middle Cam- panian) in the Pučišća Formation) (Fig. 2). Diagnosis: Being monospecific see diagnosis of genus. Description: Test elongate, trochospiral to uniserial. The early stage, rounded triangular (with concave sides), is most likely triserial as visible in transverse sections (Pl. 1B) becoming in- creasingly rounded. In the specimen shown in Pl. 1A, this stage amounts about ~40 % of the total test. The rounded void at the Table 1. Benthic foraminifera (selection) co-occurring with Cretaciclavulina gusici. Taxa Thin-sections Ac or di el la co ni ca FA RI N AC CI An ta ly na ko ra yi FA RI N AC CI & K Ö YL Ü O G LU Ca lv ez ico nu s l ec al ve za e CA U S & CO RN EL LA Ca lv ez ico nu s? sp . Cu ne ol in a gr . p av on ia p ar va H EN SO N D ic yc lin a sp . D ic ty oc on us ? s p. Li tu on el la ? s p. Li tu ol ip or a? n . s p. m ili ol id s M in ou xi a sp . M on tc ha rm on tia a pe nn in ica (D E CA ST RO ) M ur ge lla la ta LU PE RT O S IN N I Ne zz az at in el la cf . a dh am i D AR M O IA N Re tic ul in el la fl eu ry i C VE TK O e t a l. Ro ta lis pi ra sc ar se lla i ( TO RR E) Sc an do ne a m ed ite rra ne a D E CA ST RO Sc an do ne a sa m ni tic a D E CA ST RO Vo lo sh in ov el la ? s p. 514 K3V71/5 X X X X X 251 5184 X X X X X 208 18/1S4 X X X X X X X X X X X X 223 187/1 S4 X X X X X X 1Kr11315 ? ? X X X S2N124 X ? X X 209 18/2S4 X X X X X 132 918 Ku3 X X X ? 21 42 1315KR1 X X X X X 212 728 S4 X X X X X X X X 528 K213 4615 X X X X Mu 3K 606/20 X X X X X X X X ? X X G eo lo gi a C ro at ic a Geologia Croatica 69/2192 Plate 1. Cretaciclavulina gusici from the early Campanian of Brač Island. A Subaxial section, holotype specimen. Thin-section inv. no. 10807 (514 K3V71/5). B Slightly oblique transverse section showing triangular outline with concave sides, lower part of the triserial stage. Thin-section inv. no. 10808 (223 187/1 S4). C Slightly oblique transverse section in the upper part of the trochospiral stage (see GUŠIĆ & JELASKA, 1990, Pl. XV, Fig. 9). Thin-section inv. no. 10809 (213 7218/2 S4). D Slightly oblique section of the biserial stage. Thin-section inv. no. 10810 (S2N124). E Oblique section of the triserial stage. Thin-section inv. no. 10811 (132 9184 Ku3). F Oblique section of the trochospiral stage. Thin-section inv. no. 10812 (209 18/2S4). G Detail from A, showing the transition of the triserial to the uniserial stage. Note the pseudo-keriothekal wall structure. Thin-section inv. no. 10807 (514 K3V71/5). H Slightly oblique transverse section of the uniserial stage. Thin-section inv. no. 10807 (514 K3V71/5). I Detail from O, showing the cribrate apertural plate. Thin-section inv. no. 10813 (1315/1Kr1). J Oblique section of the uniserial stage cutting two chambers. Thin-section inv. no 10808 (223 187/1 S4). K Subaxial section of a broken specimen cutting 8 chambers of the uniserial stage. Thin-section inv. no. 10808 (223 187/1 S4). L Broken fragment consisting of two chambers of the uniserial stage, axial section. Thin-section inv. no. 10814 (208 18/1S4). M Oblique or tangential section of a broken specimen cutting 4 chambers of the uniserial stage. Thin-section inv. no. 10813 (1315/1Kr1). N Oblique section. Thin-section inv. no. 10815 (21 42 1315KR1). O Longitudinal, non-centered section of the uniserial stage, notably 9 chambers, of a specimen. The apertural detail is shown in I. Thin-section inv. no. 10813 (1315/1Kr1). G eologia C roatica Felix Schlagintweit and Blanka Cvetko Tešović: Cretaciclavulina gusici n. gen., n. sp. (?family Valvulinidae BERTHELIN, 1880) ... 193 apex of the holotype specimen possibly refers to the proloculus (Fig. Pl. 1G). Altogether, the information on the initial stage is poor as most random sections are beyond the uniserial stage. Fur- ther towards the following uniserial stage, transverse sections of the test become more and more rounded in outline (Pl. 1B–E, G). A short biserial part occurs between the triserial and uniserial stages (Pl. 1D). The adult stage is represented by a series of at least six uni- serial chambers. This stage is roughly cylindrical, rectilinear to slightly bent, with chambers that only slightly increase in breadth and height. This accounts for the slender, sometimes slightly bent cylindroconical test morphology. Transverse sections are either circular or slightly elliptical in outline. The solid septa are almost planar (so that the chambers are not overlapping) and pierced by a single foramen in a central to slightly eccentric position. In ax- ial sections, the appressed chambers have a low rectangular shape with rounded margins. Wall agglutinating, with a large amount of microgranular or microagglutinated calcareous material, thick and canaliculate (or paraporous) with fine pores (or canaliculi) ending blindly shortly before the outer test surface (Fig. 3A). This thin outer layer (or „pavement”, see HOTTINGER, 2006) is most ly eroded. The pores are straight and more or less parallel (radial arrangement), but may branch in the outer part. In the adult uniserial chambers of the holotype specimen, remnants of an in- ner calcitic layer are discernible. The thickness of this layer is about 0.04 mm at the lateral walls and is decreasing/tapering upon the septa towards the foramina (Fig. 3B). Foramen single interiomarginal in the trochospiral and areal in the uniserial part. Aperture (last chamber) areal, provided with a cribrate apertural plate (Pl. 1I). Dimensions: Test length: up to 2 mm Test diameter: up to 0.7 mm Number of chambers last mm axial length: 5 Adult chamber height: ~0.18 to ~0.2 mm Wall thickness (without calcitic inner layer): ~0.065 to ~0.1 mm Diameter caniculi: ~7 µm Remarks: Cretaciclavulina gusici has been illustrated by GUŠIĆ & JELASKA (1990, pl. 15, figs. 8, 9) as an „unidentified or unknown foraminifera”. The two illustrations presented are a longitudinal section of the uniserial final part cutting nine cham- bers (op. cit., pl. 15, fig. 8, refigured here on Pl. 1A, and detail in G). The other one represents an oblique transverse section of the triserial early portion (op. cit. Pl. 15, fig. 9, refigured here on Pl. 1C). Based on these sections GUŠIĆ & JELASKA (1990) sum- marized the characteristics of this taxon comprising „a well-de- veloped keriothecal wall structure, in addition to a comparatively simple morphology and lack of endoskeleton”. In fact, this mate- rial was insufficient for recognizing the new character of the form based on the combination of the different coiling modes in the early and late test portions. Transverse sections of the chrysalidinid Praechrysalidina infracreatcea LUPERTO SINNI, 1979 (Aptian of south Italy) (e.g., LUPERTO SINNI, 1985, pl. 6, fig. 5–6) are very similar to those of Cretaciclavulina gusici. P. infracretacea differs from the latter mostly by having a triserially coiled test throughout. Moreover, the early part of the test with its foramina are said to be most likely simple with broad apertural flaps situated at the inner margin, later becoming pierced by numerous areal pores (cribrate) opposed to the single areal foramina in Cretacicla­ vulina (see also BANNER et al., 1991). The species Gerochella cylindrica NEAGU (Lower Val- anginian of Romania, Fig. 4C) can be considered homeomorphic to Cretaciclavulina gusici, but is more slender (test length up to 1.4 mm; width between 0.24 to 0.29 mm). As already remarked, the wall of G. cylindrical is compact, finely agglutinated, whereas in Cretaciclavulina the wall is canaliculate (paraporous). Microfacies: Cretaciclavulina gusici has been observed in packstones and grainstones containing a diverse association of benthic foraminifera: cuneolinids, orbitolinids, soritids and other miliolids, nezzazatids, coxitids, spirocyclinids, nautiloculinids, textulariaceans, rare rotaliids and others (Tab. 1). ACKNOWLEDGMENT The authors appreciate the very helpful and constructive com- ments of the two reviewers Sylvain RIGAUD (Singapore) and Mike SIMMONS (Oxford). This work has been supported by the Croatian Science Foundation under the project number IP-2014- 09-9541. Last but not least, we thank Julie ROBSON for the Eng- lish corrections. REFERENCES BANNER, F.T. & DESAI, D. (1985): The genus Clavulinoides Cushman emended and the new Cretaceous genus Clavulinopsis.– Journal of Foraminiferal Research, 15, 79–90. doi: 10.2113/gsjfr.15.2.79 BANNER, F.T., SIMMONS, M.D. & WHITTAKER, J.E. (1991): The Mesozoic Chry- salidinidae (Foraminifera, Textulariacea) of the Middle East: the Redmond (Ara- mco) taxa and their relatives.– Bulletin of the British Museum (Natural History) Geology, 47/2, 101–152. BERTHELIN, G. (1880): Mémoire sur les Foraminifères fossils de l´Etage Albien de Mon- cley (Doubs).– Mémoires de la Société Géologique de France, ser. 3, 1 (5), 1–84. CHECCONI, A., RETTORI, R. & SPALLUTO, L. (2008): Biostratigrapfia a foraminif- erei del Cretaceo Superiore della succession di Parco Priore (Calcare di Altamura, Piattaforma Apula, Italia Meridionale).– Annali dell’Universita degli Studi di Fer- rara Museologia Scientifica e Naturalistica, 4, 1–9. doi: 10.15160/1824-2707/4/1 CHERCHI, A., RADOIČIĆ, R., SCHROEDER, R., 1991. Neobalkhania bignoti n. gen., n. sp., grand Foraminifère du Maastrichtian supérieur du Sud-est de l´Europe.– Comptes Rendus de l´ Academie des Sciences, Série II, 313, 287–292. CUSHMAN, J.A. (1911): A Monograph of the Foraminifera of the North Pacific Ocean. Part II – Textulariidae.− United States National Museum Bulletin, 71, 1−108. doi: 10.5479/si.03629236.71.2 CUSHMAN, J.A. (1927): An outline of a re-classification of the foraminifera.– Contri- butions from the Cushman Laboratory for Foraminiferal Research, 3, 1–105. CUSHMAN, J.A. (1933): Some new foraminiferal genera.– Contributions from the Cushman Laboratory for Foraminiferal Research, 9, 32–38. CUSHMAN, J A. (1935): Fourteen new species of Foraminifera.– Smithonian Miscel- laneous Collections 91 (21), 181, 1–9. doi: 10088/23898/SMC_91 CUSHMAN, J.A. (1936): New genera and species of the families Verneuilinidae and Valvulinidae and of the subfamily Virgulininae.– Special Publications Cushman Laboratory for Foraminiferal Research, 6, 1–71. CVETKO, B., GUŠIĆ, I., SCHROEDER, R. (1997): Reticulinella fleuryi n. sp. (Fo- raminiferida) from the Upper Cretaceous (Upper Santonian–Middle Campanian of the Island of Brač, Croatia.– Revue de Micropaléontologie, 40/2, 131–139. doi:10.1016/S0035-1598(97)90530-4 CVETKO TEŠOVIĆ, B., GUŠIĆ, B., JELASKA, V., BUCKOVIĆ, D. (2001): Stra- tigraphy and microfacies of the Upper Cretaceous Pučišća Formation, Island of Brač, Croatia.– Cretaceous Research, 22, 591–613. doi: 10.1006/cres.2001.0279 DAVEY, S.D. & JENKYNS, H.C. (1999): Carbon-isotope stratigraphy of shallow-water limestones and implications for the timing of Late Cretaceous sea-level rise and anoxic events (Cenomanian-Turonian of the peri-Adriatic carbonate platform, Cro- a tia).– Eclogae Geologicae Helvetiae, 92, 163–170. doi: org/10.5169/seals-168658 DE CASTRO, P. (1974): Su alcune nuove miliolidi del Senoniano del Mediterraneo.– VI Instituto di Paleontologia dell´Università di Napoli Pubblicazione, 54, 1–19. DE CASTRO, P., DROBNE, K. & GUŠIĆ, I. (1994): Fleuryana adriatica n. gen., n. sp. (Foraminiferida) from the uppermost Maastrichtian of the Brač Island (Croatia) and some other localities on the Adriatic Carbonate Platform.– Razprave IV. Razre- da SAZU, 35/8, 129–149. D’ORBIGNY, A. (1826): Tableau méthodique de la classe des Céphalopodes.– Annales des Sciences Naturelles, 7, 245–314. FRIJIA, G., PARENTE, M., DI LUCIA, M. & MUTTI, M. (2015): Carbon and Stron- tium isotope stratigraphy of the Late Cretaceous (Cenomanian-Campanian) shal- low-water carbonates of southern Italy: chronostratigraphic calibration of larger G eo lo gi a C ro at ic a Geologia Croatica 69/2194 foraminifera biostratigraphy.– Cretaceous Research, 53, 110–139. doi: 10.1016/j. cretres.2014.11.002 GALLOWAY, J.J. (1933): A manual of Foraminifera. Bloomington, Principia Press. GUŠIĆ, I. & JELASKA, V. (1990): Upper Cretaceous stratigraphy of the Island of Brač.– Djela Jugoslavenska Akademija Znanosti i Umjetnosti Zagreb, 69, 1–160. HOTTINGER, L. (2006): Illustrated glossary of terms used in foraminiferal research. Car- nets de Géologie.– Notebooks on Geology Memoires 2006/02. doi: CG2006_M02 HOTTINGER, L., HALICZ, E. & REISS, Z. (1990): Partitions and fistulose chambers in Textulariina.– In: HEMLEBEN, C., KAMINSKI, M.A., KUHNT, W. & SCOTT, D.B. (eds.): Paleoecology, biostratigraphy, paleoceanography and taxonomy of agglutinated foraminifera. Dordrecht, Kluwer Academic Publisher, 37–49. doi: 10.1007/978-94-011-3350-0 JELASKA, V. (2002): Carbonate Platforms of the External Dinarides.– In: VLAHOVIĆ, I. & TIŠLJAR, J. (eds.): Evolution of Depositional Environments from the Pal- aeozoic to the Quaternary in the Karst Dinarides and Pannonian Basin.– 22nd IAS Meeting of Sedimentology, Opatija, Field Trip Guidebook, 67–71. JENKYNS, H.C. (1991): Impact of Cretaceous sea level rise and anoxic events on the Mesozoic carbonate platform of Yugoslavia.– American Association of Petroleum Geologists, Bulletin, 75/6, 1007–1017. KAMINSKI, M.A., CETEAN, C.G. & TYSZKA, J. (2011): Nomenclature to describe the transition from multiserial to uniserial chamber arrangement in benthic foraminif- era.– Journal of Micropalaeontology, 30, 7–10. doi: 10.1144/0262-821X10-016 KAMINSKI, M.A., CETEAN, C.G. & NEAGU, T. (2010): Rectogerochammina eu­ gubina nov. gen., nov. sp., a new agglutinated foraminifer from the Upper Creta- ceous of Gubbio, Italy.– Revue de Micropaléontologie, 53, 121–124. doi:10.1016/ jraminifera KORBAR, T. (2003): Stratigrafija, taksonomija i paleoekologija radiolitida gornje krede Jadranske karbonatne platforme (Stratigraphy, Taxonomy and Palaeoecology of Upper Cretaceous Radiolitidae of the Adriatic Carbonate Platform).– PhD Thesis, University of Zagreb, Croatia, 242 p. (in Croatian with English summary, unpu- blished). KORBAR, T., GLUMAC, B., CVETKO TEŠOVIĆ, B., CADIEUX, S. B. (2012): Re- sponse of a carbonate platform to the Cenomanian–Turonian drowning and OAE 2: a case study from the Adriatic Platform (Dalmatia, Croatia).− Journal of Sedi-Sedi-edi- mentary Research, 82, 163−176. doi:10.2110/jsr.2012/17 KORBAR, T. & HUSINEC, A. (2003): Biostratigraphy of Turonian to (?)Coniacian plat- form carbonates: A case study from the Island of Cres (Northern Adriatic, Cro- atia).– Geologia Croatica, 56, 173–185. doi: 10.4154/GC.2003.11 LOEBLICH, A.R., JR. & TAPPAN, H. (1985): Some new and redefined genera and fa- milies of agglutinated foraminifera II.– Journal of Foraminiferal Research, 15/3, 175–217. doi: 10.2113/gsjfr.15.3.175 LOEBLICH, A.R., JR. & TAPPAN, H. (1987): Foraminiferal genera and their classifica- tion. – 2 volumes, 1–970, (Van Nostrand Reinhold) New York. doi: 10.1007/978- 1-4899-5760-3 LUPERTO SINNI, E. (1976): Microfossili senoniani delle Murge.– Rivista Italiana di Paleontologia e Stratigrafia, 82/2, 293–416. LUPERTO SINNI, E. (1979): Praechrysalidina infracretacea n. gen., n. sp. (Foramini- ferida) del Cretaceo inferiore delle Murge Baresi.– Studi geologici e morfologici sulla Regione Pugliese, 5, 1–16. LUPERTO SINNI, E. (1985): Praechrysalidina infracretacea LUPERTO SINNI, 1979. – In: SCHROEDER, R. & NEUMANN, M. (coords.), Les grand foraminifères du Crétacé Moyen de la région Méditerranénne.– Géobios Mémoire spécial, 7, 22. NEAGU, T. (1997): Lower Cretaceous agglutinated foraminifera from southern Do- brogea, omania. Part 1, Verneuilinacea, Ataxophragmiacea.– Annales Societatis Geologorum Poloniae, 67, 307–323. PAMIĆ, J., GUŠIĆ, I. & JELASKA, V. (1998): Geodynamic evolution of the Central Dinarides.– Tectonophysics, 297, 251–268. doi: 10.1016/S0040-1951(98)00171-1 PEJOVIĆ, D. & RADOIČIĆ, R. (1987): Contribution to the study of Upper Cretaceous stratigraphy of Brač – Adriatic Carbonate Platform.– Geologija, 28/29, 121–150 (In Serbian, English summary). PILLER, W.E. (1990): Wall structures of palaeotextulariid foraminifers and discussion of microgranular test walls.– Paleoecology, Biostratigraphy and Taxonomy of ag- glutinated Foraminifera. NATO ASI Series, 327, 25–35. doi: 10.1007/978-94-011- 3350-0_4 POLŠAK, A., BAUER, V. & SLIŠKOVIĆ, T. (1982): Stratigraphie du Crétacé supérieur de la plate-forme carbonatée dans les Dinarides externs.– Cretaceous Research, 3, 125–133. doi: 10.1016/0195-6671(82)90013-1 RIGAUD, S., VACHARD, D. & MARTINI, R. (2015): Agglutinated versus microgran- ular foraminifers: end of a paradigm?– Journal of Systematic Palaeontology, 13/2, 75–95. doi:10.1080/14772019.2013.863232 SCHLAGINTWEIT, F., HUSINEC, A. & JEŽ, J. (2014): Siphodinarella costata n. gen., n. sp., a new benthic foraminifer from the Upper Cretaceous (Late Turonian-San- tonian) of the Karst Dinarides (Slovenia, Croatia).– Facies, 60, 133–145. doi: 10.1007/s10347-013-0365-1 SCHWAGER, C. (1877): Quadro del proposto sistema di classificazione dei foraminiferi con guscio.– Bolletino del R. Comitato Geologico d´Italia, 8, 18–27. STEUBER, T., KORBAR, T., JELASKA, V. & GUŠIĆ, I. (2005): Strontium-isotope strati- graphy of Upper Cretaceous platform carbonates of the island of Brač (Adriatic Sea, Croatia): implications for global correlation of platform evolution and bios- tratigraphy.– Cretaceous Research, 26, 741–756. doi: 10.1016/j.cretres.2005.04.004 TORRE, M. (1966): Alcuni foraminiferi del Cretacico superiore della Penisola Sorren- tina.– Bolletino della Società dei Naturalisti in Napoli, 75, 409–431. TYSZKA, J. & THIES, A. (2001): Spiroplectinata, key benthic foraminifera genus for palaeoceanographic reconstructions of the Albian Lower Saxony Basin.– Palaeo- geography, Palaeoclimatology, Palaeoecolgy, 174, 199–220. doi: 10.1016/S0031- 0182(01)00294-2 VACHARD, D., MUNNECKE, A. & SERVAIS, T. (2004): New SEM observations of keriothecal walls: implications for the evolution of the Fusulinida.– Journal of Fo- raminiferal Research, 34/3, 232–242. doi: 10.2113/34.3.232 VELIĆ, I., (2007): Stratigraphy and palaeobiogeography of Mesozoic benthic forami- nifera of the Karst Dinarides (SE Europe).– Geologia Croatica, 60, 1–113. doi: 10.4154/GC.2007.01a VLAHOVIĆ, I., TIŠLJAR, J., VELIĆ, I. & MATIČEC, D. (2005): Evolution of the Adri- atic Carbonate Platform: Palaeogeography, main events and depositional dynam- ics.– Palaeogeography, Palaeoclimatology, Palaeoecology, 220/3–4, 333–360. doi: 10.1016/j.palaeo.2005.01.011 WEIDICH, K.-F. (1988): On the variability of some Recent and fossil „Clavulina” spe- cies (Foraminifera). Abhandlungen der Geologischen Bundesanstalt, 41, 337–354.