- Research Article
- Open Access
Multiple Orbitoides d’Orbigny lineages in the Maastrichtian? Data from the Central Sakarya Basin (Turkey) and Arabian Platform successions (Southeastern Turkey and Oman)
Swiss Journal of Palaeontology volume 140, Article number: 8 (2021)
The standard reconstruction of species of Orbitoides d’Orbigny into a single lineage during the late Santonian to the end of the Maastrichtian is based upon morphometric data from Western Europe. An irreversible increase in the size of the embryonic apparatus, and the formation of a greater number of epi-embryonic chamberlets (EPC) with time, is regarded as the main evolutionary trends used in species discrimination. However, data from Maastrichtian Orbitoides assemblages from Central Turkey and the Arabian Platform margin (Southeastern Turkey and Oman) are not consistent with this record. The Maastrichtian Besni Formation of the Arabian Platform margin in Southeastern Turkey yields invariably biconvex specimens, with small, tri- to quadrilocular embryons and a small number of EPC, comparable to late Campanian Orbitoides medius (d’Archiac). The upper Maastrichtian Taraklı Formation from the Sakarya Basin of Central Turkey contains two distinct, yet closely associated forms of Orbitoides, easily differentiated by both external and internal features. Flat to biconcave specimens possess a small, tri- to quadrilocular embryonic apparatus of Orbitoides medius-type and a small number of EPC, whereas biconvex specimens possess a large, predominantly bilocular embryonic apparatus, and were assigned to Orbitoides ex. interc. gruenbachensis Papp–apiculatus Schlumberger based on morphometry. The flat to biconcave specimens belong to a long overlooked species Orbitoides pamiri Meriç, originally described from the late Maastrichtian of the Tauride Mountains in SW Turkey. This species is herein interpreted to be an offshoot from the main Orbitoides lineage during the Maastrichtian, as are forms that we term Orbitoides ‘medius’, since they recall this species, yet are younger than normal occurrence with the accepted morphometrically defined lineage. The consistent correlation between the external and internal test features in O. pamiri implies that the shape of the test is not an ecophenotypic variation, but appears to be biologically controlled. We, therefore, postulate that more than one lineage of Orbitoides exists during the Maastrichtian, with a lineage that includes O. ‘medius’ and O. pamiri displaying retrograde evolutionary features.
Orbitoides d’Orbigny is an orbitoidal larger foraminifer that thrived in the tropical and sub-tropical shallow marine carbonate platforms and ramps from Central America to Asia during the late Santonian to the end of the Maastrichtian (Goldbeck & Langer, 2009; Loeblich & Tappan, 1987; van Gorsel, 1978). The genus evolved from a simple test, consisting of solely an equatorial layer with a small embryonic apparatus and a few epi-embryonic chamberlets (EPC), to large tests with thick lateral layers on both sides of the equatorial layer, large embryons and many epi-embryonic chamberlets. A single evolutionary succession of species (from oldest to youngest: Orbitoides hottingeri van Hinte, Orbitoides douvillei (Silvestri), Orbitoides tissoti Schlumberger, Orbitoides medius (d’Archiac), Orbitoides megaloformis Papp and Küpper, Orbitoides gruenbachensis Papp, Orbitoides apiculatus Schlumberger, and Orbitoides gensacicus (Leymerie)) has been constructed, ranging from the late Santonian or early Campanian to the end of the Maastrichtian (Caus et al. 1996; Eggink & Baumfalk, 1983; van Gorsel, 1978; van Hinte, 1966a, 1968, 1976). Recently, Albrich et al. (2014) interpreted Orbitoides sanctaepelagiae (Astre) as a valid species and considered it as a transitional form between O. hottingeri and O. douvillei.
The Maastrichtian part of the Orbitoides lineage was constructed mainly from data gathered from the Maastrichtian type section in the Netherlands and some sections in SW France and Spain. It, therefore, more properly represents the evolution of the genus in Western Europe. The exact stratigraphic distribution of the species within this lineage is not yet precisely calibrated against the standard geologic time scale. In spite of these uncertainties, three species, O. gruenbachensis, O. apiculatus and O. gensacicus, have commonly been reported from Maastrichtian sediments. These species correspond to an advanced developmental stage of the presumed lineage and are characterised by a relatively large embryonic apparatus (the size of which is expressed by Li + li) and many epi-embryonic chamberlets (expressed by E, the total number of primary and accessory epi-embryonic chamberlets (EPC)).
It is noteworthy that specimens with rather small embryons and a small number of epi-embryonic chamberlets (morphometrically in the range of the Campanian species O. medius) have been reported associated with the ‘advanced’ members of the genus within Maastrichtian strata (Baumfalk, 1986; Baumfalk & Willemsen, 1986; Eggink & Baumfalk, 1983; Görmüş & Meriç, 2000; Özcan & Özkan-Altıner, 1997). Most of these studies do not consider typologically different specimens as separate species, but rather assume a single species is present, following the morphometric species concept where all specimens from one population receive the same species name. According to the morphometric approach, morphologic characters of the majority of the specimens in a population are also considered to be more important for species determination than the characters of the individual specimens (Drooger, 1993; van Gorsel, 1978; van Hinte, 1966b). This means that variations in test features such as shape, features of lateral layers, chamberlets and piles are explained by variations in environmental conditions, and are not considered to possess taxonomic value in species discrimination (see van Gorsel, 1978 for discussion).
Having recognised two morphologically distinct groups of tests of Orbitoides during outcrop-based studies of the upper Maastrichtian Taraklı Formation in Nallıhan region (Central Turkey), we carried out a detailed study to record embryonic-nepionic developmental stages, paying special attention to external test features. In addition to the well-known species O. ex. interc. gruenbachensis–apiculatus, we show that these late Maastrichtian populations include predominantly flat- to biconcave specimens, possessing small, tri- to quadrilocular embryonic apparatus of Orbitoides medius-type and a small number of EPC, previously recorded from southern Turkey as O. pamiri, but not known from Europe. We also present unpublished data of EÖ from the Maastrichtian Besni Formation from the Arabian Plate margin, previously assigned to Orbitoides ‘medius’ in the frame of his PhD studies (Özcan, 1994). For further context, Orbitoides from the upper Maastrichtian Beyobası Formation of the Haymana Basin (Central Turkey) and upper Campanian–Maastrichtian Qahlah and Simsima Formations of Oman are also discussed briefly, with the overall aim of testing the hypothesis that more than one evolutionary lineage of Orbitoides occurs within the Maastrichtian.
Geological setting, stratigraphy and larger foraminiferal assemblages
Central Sakarya Basin (Central Turkey)
The Jurassic–Cretaceous Central Sakarya Basin is located in the Sakarya Zone of the Pontides (Okay & Tüysüz, 1999). The sedimentary sequence begins with Lower Jurassic conglomerates, sandstone and shales, which unconformably overlie a Variscan and Cimmeride basement (Ocakoğlu et al. 2019; Saner, 1980). The Lower Jurassic siliciclastic rocks are overlain by Upper Jurassic to Lower Cretaceous limestones, no younger than Aptian (Altıner et al. 1991). The Albian to Santonian sequence is represented by sandstone, shale, pelagic limestone and marl. Siliciclastic turbidite deposition begins in the Campanian and extends into the Maastrichtian (Ocakoğlu et al. 2019). These turbidites, the Yenipazar Formation (Saner, 1980), have a thickness of more than 1000 m and form a regressive sequence. Turbidites pass up into massive marls, the Seben Formation (Saner, 1980), which grades into ‘neritic’ sandstones of the Taraklı Formation (the focus of our study), recording the final stage of extensive Cretaceous marine sedimentation in the Central Sakarya Basin (Saner, 1980) (Fig. 1a and b). The palaeogeographic position of the basin is shown in Fig. 2.
The Taraklı Formation is composed of a sandstone–siltstone succession, 100–300 m-thick, with larger foraminifera and bivalves present in some intervals. It is unconformably overlain by either continental clastic rocks of the Kızılçay Group or shallow marine carbonates of the Selvipınar Formation (Fig. 1b). The age of the Taraklı Formation was reported as Maastrichtian in the southern part of the Central Sakarya Basin (Saner, 1980), and Maastrichtian–Paleocene in the northern part (Ocakoğlu et al. 2019; Saner, 1980). Our data (including new nannofossil analyses) from the Epçeler Sections (Epçeler A and B) to the northwest of Nallıhan, and from Dereköy to the north of Nallıhan, indicate a late Maastrichtian age for the Taraklı Formation. The fauna present in the Epçeler and Dereköy sections is not diverse, and is predominantly composed of Orbitoides, very rare Lepidorbitoides, Siderolites, a few broken tests of Omphalocyclus and bivalve debris (Fig. 3).
Kahta, Adıyaman region (Southeastern Turkey)
The northern margin of the Arabian Platform in Southeastern Turkey is characterised by allochthonous and pre-and/ or post-emplacement autochthonous or parautochthonous units (Perinçek, 1980; Rigo de Righi & Cortesini, 1964; Yılmaz, 1993) (Fig. 4). The Kahta region of the Adıyaman province is one of the areas at the northern border of Arabian fold belt in which Late Cretaceous nappe emplacement and post-emplacement Late Cretaceous sedimentation are fully recorded (Meriç, 1965; Meriç et al. 1987; Özcan, 1993, 1994) (Fig. 4). The post-emplacement Terbüzek (also known as ‘Antak’) Formation is a thick-bedded to massive, friable and polygenetic coarse conglomerate unit with local sandstone intercalations (samples TF2 and 5). The formation is a continental to shallow marine clastic unit, which forms part of a new transgressive cycle following the Campanian– (?) early Maastrichtian nappe emplacement (Özcan, 1993, 1994). The fauna from the Terbüzek Formation consists of O. megaloformis Papp and Küpper, 1953, Lepidorbitoides bisambergensis (Jaeger, 1914), Omphalocyclus anatoliensis Özcan, 2007, Planorbulinella sp., Goupillaudina sp., and Marssonella sp., associated with rudists (Özcan, 1994, 1995, 2007; Özer, 1986). The Besni Formation is a clastic-carbonate unit, interpreted as a biohermal carbonate or beach deposit, conformably overlying the Terbüzek Formation (Meriç et al. 1987) (Fig. 4). The rapid proliferation and abundance of many larger benthic foraminiferal taxa such as Orbitoides, Siderolites, Omphalocyclus, Loftusia, Clypeorbis, Lepidorbitoides, Sirtina, Goupillaudina, together with the presence of rudists is a very characteristic feature of this formation (Özcan, 1993, 1994). Özcan (1994, 2007) assigned Orbitoides assemblages to O. ‘medius’ associated with Siderolites calcitrapoides Lamarck, 1801, Omphalocyclus anatoliensis Özcan, 2007, Sirtina cf. orbitoidiformis Brönnimann and Wirtz, 1962, and Clypeorbis aff. mamillatus (Schlumberger, 1902). An early Maastrichtian age for the Besni Formation was proposed by Özcan (1994). The overlying Germav Formation is predominantly composed of fine siliciclastic rocks with planktonic foraminifera. Two turbiditic beds (sample GA64 yielded an assemblage of O. ‘megaloformis’ and L. gr. minor-socialis associated with Siderolites calcitrapoides, Siderolites denticulatus Douvillé, 1906, Omphalocyclus. cf. macroporus (Lamarck, 1816), Pseudomphalocyclus blumenthali Meriç, 1980, S. cf. orbitoidiformis, and Loftusia spp. (Özcan, 1993, 1994). The age of the Germav Formation has been reported as early-middle/late Maastrichtian. Tertiary deposits unconformably overlie the Upper Cretaceous units and are represented by the continental red beds of the Gercüş Formation and carbonates of the Midyat Group.
Haymana Basin, Central Turkey
The Haymana Basin is a thick clastic depocentre of Late Cretaceous to Eocene age in central Anatolia (Özcan et al. 2020). The Beyobası Formation, the uppermost stratigraphic unit of the Cretaceous sequence, is a shallow marine-mixed carbonate-siliciclastic deposit consisting of siltstone-sandstone and bioclastic limestone beds. The Beyobası Formation contains O. apiculatus, O. ‘medius’, L. socialis, O. macroporus, Siderolites sp., Loftusia sp., Sirtina sp., Hellenocyclina sp. and Cideina sp., accompanied by Cyclolites sp., bivalves and gastropods indicating a late Maastrichtian age (Özcan & Özkan-Altıner, 1997).
Buraymi region, North Oman
The Qahlah and Simsima Formations are the first autochthonous sediments deposited on the obducted ophiolite complex in Oman. They are characterised by an abundance of benthic foraminifera and rudists, along with corals, calcareous algae, gastropods and echinoids (Abdelghany, 2003; Béchennec et al. 1993; Kayğılı et al. 2021; Nolan et al. 1990; Roger et al. 1993; Schlüter et al. 2008; Skelton et al. 1990). A road-cut section to the northeast of Buraymi in North Oman shows an expanded section of the marine part of the Qahlah Formation immediately below the Simsima Formation (Fig. 5) (Buraymi Section in Kayğılı et al. 2021). The upper Campanian Qahlah Formation here consists of massive mudstone/marl and siltstone beds with primitive Omphalocyclus (O. omanensis sp. nov. in Kayğılı et al. 2021), O. medius and calcareous nannofossils with a typical late Campanian assemblage (zones CC22b and CC23a). The marine siliciclastic beds in the upper part of the Qahlah Formation are overlain by a paleosol horizon and a conglomerate bed with predominantly chert pebbles, with a sharp contact with the overlying Simsima Formation.
The Simsima Formation is of variable thickness (2.5–200 m) and is a shallow marine bioclastic limestone. Foraminifera reported from previous studies include O. medius, O. apiculatus, O. macroporus, Pseudomphalocyclus blumenthali, L. cf. minor, Siderolites calcitrapoides, Loftusia morgani Douvillé, Sulcoperculina dickersoni (Palmer) (Abdelghany, 2003; Béchennec et al. 1993; Schlüter et al. 2008; Skelton et al. 1990). Rudists are common, with assemblages including Vaccinites, Hippurites, Durania, Biradiolites, Dictyoptychus, Torreites, Vautrinia, Bournonia, Pseudopolyconites, and Sabinia (Skelton et al. 1990). In the Buraymi region, the Simsima Formation begins with a succession of nodular, resistant calcarenitic beds, 9-m-thick, with clay partings (Fig. 5). This part is highly fossiliferous, dominated by O. gensacicus (Leymerie, 1851), Lepidorbitoides ex. interc. socialis (Leymerie, 1851)–minor (Schlumberger, 1902), Sirtina orbitoidiformis Brönnimann and Wirtz, 1962, Clypeorbis cf. mamillatus (Schlumberger, 1902), Ilgazina unilateralis Erdoğan, 1995, Siderolites sp., O. cf. macroporus, Pseudorotalia sp., Rotalispira sp., Fallotia sp., Planorbulina sp., Fissoelphidium sp., algae, miliolids, gastropods and agglutinated foraminifera (Özcan et al. 2021). The age of the studied populations is, thus, safely constrained to the Maastrichtian, most likely to the late (not latest) Maastrichtian by the co-occurrence of the primitive developmental stage of L. socialis and O. gensacicus, a ‘late Maastrichtian’ key species in Europe (Caus et al. 1996; Eggink & Baumfalk, 1983; Özcan & Özkan-Altıner, 1997). O. gensacicus, recorded for the first time from the Simsima Formation in Oman, is accepted as the youngest representative of the genus and thus, its presence in the Simsima Formation unequivocally suggests a late Maastrichtian age.
Materials and methods
Samples were collected at three localities (Localities A–C) in the southeastern part of the Central Sakarya Basin, near Nallıhan (province of Ankara), and from three localities at the Arabian Platform margin (Localities D–F) in SE Turkey (Figs. 1 and 4). Samples from the Haymana Basin (Locality G) in Central Turkey, and Buraymi region (Locality H) in north Oman (Fig. 5), are also incorporated to this study.
Locality A (Epçeler A Section, Central Sakarya Basin): 19 samples were collected to the south of Epçeler village near Nallıhan, Ankara province (Fig. 1b). Samples 1–12 are from the massive marly beds of the Seben Formation below the sandstones of the Taraklı Formation, and samples 13–19 (sample 13: 40° 14′ 6.64″ N, 31° 5′ 39.19″ E; sample 19: 40° 14′ 5.10″ N, 31° 5′ 39.72″ E) come from the middle and upper part of sandstone succession of the Taraklı Formation. The Taraklı Formation is unconformably overlain by coarse red beds of the Kızılçay Formation.
Locality B (Epçeler B Section, Central Sakarya Basin): Samples EPB 1–9 were taken from the Taraklı Formation near Epçeler village, approximately 700 m east of Locality A, to the southeast of Epçeler village (sample 1: 40° 14′ 15.01″ N, 31° 5′ 56.51″ E; 40° 14′ 6.19″ N, sample 9: 40° 14′ 6.19″ N, 31° 6′ 1.83″ E).
Locality C (Dereköy Section, Central Sakarya Basin): Samples DE 6 and 7 were taken from the upper part of the Taraklı Formation near Dereköy village to the northwest of Nallıhan, Ankara province (sample 6: 40° 15′ 51.45″ N, 31° 20′ 9.55″ E, sample 7: 40° 15′ 51.71″ N, 31° 20′ 9.43″ E).
Locality D (SE Turkey). Samples TF2 and TF5 come from the middle part of the Terbüzek Formation to the west of Alidamı, Kahta, Adıyaman province (37° 55′ 38.12″ N, 38° 54′ 8.70″ E and 37° 55′ 35.54″ N, 38° 54′ 7.74″ E) (Özcan, 1994).
Locality E (SE Turkey). Samples TC6-10 and 13 were collected from the Besni Formation to the north of Alidamı, Kahta, Adıyaman province (37° 56′ 6.26″ N, 38° 58′ 16.36″ E) (Özcan, 1994).
Locality F (SE Turkey). Sample GA64 was taken from a turbiditic bed of the Germav Formation to the southeast of Karadut, Kahta, Adıyaman province (37° 55′ 15.99″ N, 38° 47′ 46.44″ E) (Özcan, 1994).
Locality G (Haymana Basin, Central Turkey). Samples DEG16-20B were collected just below the Cretaceous–Cenozoic boundary near the village of Sarıdeğirmen (39° 30′ 37.21″ N; 32° 26′ 53.24″ E) (Özcan & Özkan-Altıner, 1997).
Locality H (Buraymi region, North Oman). The samples B6, B8 and B9 were collected from the upper part of the Campanian Qahlah Formation near Buraymi (24° 16′ 48.57″ N; 55° 49′ 26.96″ E; 24° 16′ 49.84″ N; 55° 49′ 24.68″ E). A detailed description of the Buraymi section is given by Kayğılı et al. (2021).
The material from the Taraklı Formation consists of 359 isolated Orbitoides specimens studied in equatorial sections and about 50 specimens studied in axial sections, and a single Lepidorbitoides specimen, investigated through its equatorial section, supplemented by random thin sections. The material from the Terbüzek and Besni Formations consists of 261 Orbitoides specimens studied in their equatorial sections and 14 specimens studied in axial sections. Equatorial, axial and tangential sections, essential for taxonomy, require the grinding of the isolated test on preferred orientations by a fine grinding paper. The measurements and counts used in the morphometry of these taxa are shown in Tables 1 and 2. All specimens are deposited in the palaeontological collections of the Geological Engineering Department of İstanbul Technical University and prefixed EO/. For calcareous nannofossils, eleven samples from Epçeler A Section and one sample from Epçeler B Section, and five from Dereköy Section were collected. They were prepared as simple smear slides following standard procedures (Bown & Young, 1998) and analysed through a polarised light microscope at × 1250 magnification.
Species concept and evolutionary trends in Orbitoides
The definition of species in palaeontology is fraught with difficulty. On one hand, we may seek to attempt to determine that a fossil species has equivalent meaning to that of a biological species—a grouping of organisms that can interbreed and are reproductively isolated from other groups. Our recognition of species may attempt to allude to this unknowable goal. More practically, we may try to define species as distinct forms within the process of evolution, capturing the progressive stages of the evolution of a genus or related group of genera. Very often, species are defined because they seem distinct enough to a palaeontologist to merit separation. This can be very subjective, especially if the evolutionary context of the new species being described is not well understood.
The concept of species definition in larger benthic foraminifera (LBF) is a case in point. Differences in the complex internal structure of many LBF are the basis for species definition, with external morphology often a secondary consideration, as it is often viewed as being controlled by localised environmental factors. In several LBF groups, including Orbitoides, two approaches to species definition have arisen. The first is a typological approach, following long palaeontological tradition. A grouping of the size and shape of internal features, and perhaps external features, collectively define a species with reference to type specimens. This method has been described as “the intuitive appraisal of differences recognised by the specialist on the basis of his ‘experience’ ” (Drooger, 1993), in other words, the entire process of empirical pattern recognition (Less & Kovacs, 2009). The second is a morphometric approach, where a statistical analysis of morphological characters (such as diameter of the embryon, and size and number of peri-embryonic chambers) in an adequate number of samples from successive populations can be used to define the evolutionary stages of each character to form a bioseries. Both methods have advantages and disadvantages (Less & Kovacs, 2009; Pignatti, 1998). A potential pitfall of morphometric methods is that they consider a population of generally similar forms to be a single species, and thus, representative of the range within that species. This means that co-existing parallel lineages can be overlooked.
Since the first description of Orbitoides by d’Orbigny, many species have been described based on various criteria (see van Gorsel, 1978 for a historical account). Classification follows either typological (based on overall test features; shape of the test, features of piles and lateral layers, type of embryonic apparatus) or morphometric species concepts. The latter approach, based on the study of the embryonic apparatus and the surrounding nepionic chamberlets, results in a single evolutionary series consisting of quantitatively defined ‘chronospecies’ the boundaries of which are arbitrary (Figs. 6, 7). According to this approach, all specimens from a population are assigned to a single species.
The morphological changes recorded in the equatorial layer of Late Cretaceous orbitoidal foraminifera (e.g. Orbitoides, Lepidorbitoides) are expressed by the concept of nepionic–embryonic acceleration (Drooger, 1983, 1993; van Hinte, 1966b, 1976). This is based on a progression resulting in fewer steps of chambers until the individuals attain the ontogenetic stage of cyclical development, and a tendency for an increase in the size of the embryon. In this approach to species definition, other test features, specifically shape of the test and piles, are interpreted as environmentally controlled and not used in species characterisation (van Gorsel, 1978). In contrast, Neumann (1972, 1987) concluded that primitive species of the genus (e.g. O. dordoniensis) actually belong to Planorbulina or Planorbulinella, and considered O. tissoti, O. medius and O. apiculatus as the only valid species of Orbitoides. Research on Orbitoides populations from the (upper) Campanian type section at Aubeterre (SW France) (Figs. 2, 8a), (upper) Maastrichtian type sections at ENCI quarry (St. Pietersberg, Netherland) (Figs. 2, 8b) and adjacent regions form the backbone of the morphometric studies and phylogenetic interpretations (Baumfalk, 1986; Baumfalk & Willemsen, 1986; Caus et al. 1996; Eggink & Baumfalk, 1983; van Hinte, 1966b) (Figs. 6, 7).
Key biometric features being considered as definitive include embryonic apparatus size (expressed as Li + li) and number of epi-embryonic chamberlets (EPC) (expressed by E, total number of primary and accessory EPC). Size and number of EPC has typically been assumed to increase with time, providing biostratigraphic utility through the definition of a series of biozones (Caus et al. 1996). Whilst this lineage is not perfectly calibrated to the standard stages of the Late Cretaceous (and bearing in mind calibration issues caused by the definition of the base Maastrichtian GSSP (Odin & Lamaurelle, 2001)), O. gruenbachensis Papp, O. apiculatus, and O. gensacicus, with relatively large apparatus and many epi-embryonic chamberlets (Fig. 7) are typically considered as Maastrichtian (Caus et al. 1996). It is important to note that this lineage has been defined based mostly on material from the Campanian and Maastrichtian stratotypes and allied sections in Western Europe. Can the concept of a simple single lineage be challenged by data from other Tethyan margins where Orbitoides proliferated (e.g. Turkey, Arabia) and from the Caribbean?
Previous studies have considered that O. medius and O. megaloformis are typical late Campanian species and the evolution from O. medius to O. megaloformis is not gradual but involves a relatively short interval of transition in which former is replaced by the latter (Baumfalk, 1986). Similarly, the evolution of O. apiculatus within the Maastrichtian type section involves a general increase in the embryon size and number of epi-embryonic chamberlets although more ‘advanced’ populations were recorded from the debris layers over the hardgrounds present, and the intervals between the hardgrounds contain specimens with rather smaller embryons, a phenomenon ascribed to the specific environmental conditions (Baumfalk & Willemsen, 1986).
O. gensacicus with a very large embryon, which is composed of a great number of embryonic chambers, was suggested to be a direct descendent of O. apiculatus stock in the late Maastrichtian (Eggink & Baumfalk, 1983). Thus, in spite of the uncertainties in the definition of the Campanian–Maastrichtian boundary in the shallow marine Tethyan realm, the Maastrichtian Orbitoides are characterised by large, tri-to quadrilocular (O. gruenbachensis-type), bilocular (O. apiculatus-type) and giant multilocular embryons (O. gensacicus-type).
In spite of the overall evolutionary trend in the increase of embryon size and formation of a greater number of epi-auxiliary chamberlets from the Campanian to the end of the Maastrichtian (Fig. 7), the occurrence of Orbitoides specimens consisting of small embryons with only a few epi-embryonic chamberlets has been frequently been reported associated with the phylogenetically advanced species such as O. gruenbachensis, O. apiculatus and O. gensacicus during the Maastrichtian (Baumfalk, 1986; Eggink & Baumfalk, 1983; Meriç, 1965; Özcan & Özkan-Altıner, 1997, 1999; Özer et al. 2009). These specimens were either assigned to O. ‘medius’ as a separate species or were considered a part of the population that receives the species name based on morphometry. Meriç (1965) and Özcan (1994) thus reported O. medius from the Maastrichtian sequence in the Arabian Platform margin. Baumfalk (1986) has pointed out that in a purely typological sense specimens with O. medius-type embryons may also be found in O. apiculatus populations at the Maastrichtian stratotype.
The upper Maastrichtian beds, immediately below the Maastrichtian–Paleocene boundary in the Haymana Basin (Central Turkey), yield Orbitoides with predominantly large bilocular embryons, but also rare small tri- to quadrilocular embryons (Özcan & Özkan-Altıner, 1997, 1999) (Figs. 2, 8c). Similarly, O. ‘medius’ was reported as co-occurring with O. apiculatus and O. gensacicus in upper Maastrichtian deposits from the Gensac–St. Marcet region in Southern France (Eggink & Baumfalk, 1983). Furthermore, Meriç (1974) reported some flat to biconcave Orbitoides specimens from the upper Maastrichtian of the Taurus Mountains (SW Turkey) and assigned them to O. apiculatus pamiri n. ssp., assuming a relationship to O. apiculatus. These specimens have small tri- to quadrilocular embryons and their embryonic parameters are within the limits of O. medius (Fig. 7). The tests of these specimens, however, are quite different from the biconvex test of O. medius, and the number of lateral chamberlet layers in this subspecies is much less than in O. medius.
Calcareous nannofossils and age of the Taraklı Formation in the Nallıhan region
Calcareous nannofossils were studied from the Taraklı Formation to provide independent biostratigraphic calibration of age. Samples from the Epçeler A and B sections contain calcareous nannofossil assemblages characterised by low abundance and poorly preserved forms (Fig. 9). However, it was possible to recognise a certain number of taxa occurring in reasonable numbers. The most abundant genus is Micula, mainly represented by Micula staurophora (Gardet) Stradner, with minor occurrences of Micula concava (Stradner) Verbeek and Micula swastica Stradner and Steinmetz (gathered under Micula spp.) and very rare specimens of Micula praemurus (Bukry) Stradner and Steinmetz. The other well-represented genus is Watznaueria, including Watznaueria barnesiae (Black) Perch-Nielsen and subordinately Watznaueria fossacinta (Black) Bown. Another component of the assemblages is the genus Prediscosphaera, well represented by Prediscosphaera cretacea (Arkhangelsky) Gartner and in minor amounts by Prediscosphaera ponticula (Bukry) Perch-Nielsen. Lithraphidites occurs with the presence of the marker species Lithraphidites quadratus Bramlette and Martini and Lithraphidites praequadratus Roth. Arkhangelskiella cymbiformis Vekshina occurs continuously with significant numbers of medium and large specimens. Also present are Biscutum constans (Górka) Black and Biscutum ellipticum (Górka) Grün, Retecapsa angustiforata Black and Retecapsa crenulata (Bramlette and Martini) Grün. Other components are Cribrosphaerella ehrenbergii (Arkhangelsky) Deflandre, Eiffellithus turriseiffelii (Deflandre) Reinhardt, Microrhabdulus decoratus Deflandre, and in minor amounts Ceratolithoides aculeus (Stradner) Prins and Sissingh, Chiatozygus sp., Cribrocorona gallica (Stradner) Perch-Nielsen, Cyclagelosphaera sp., Russellia bukryi Risatti and Zeugrhabdotus sp. The occurrence of L. quadratus allows for the Epçeler Section to be attributed to the late Maastrichtian UC20a Zone of Burnett, 1998 (corresponding to the CN22 Zone of Roth, 1978 and the CC25c zones of Sissingh, 1977 and Perch-Nielsen, 1985).
Samples from Dereköy Section are characterised by low diversity calcareous nannofossil assemblages, with rare occurrences of very poorly preserved forms (Fig. 9). The main taxa are A. cymbiformis, C. ehrenbergii, Micula (M. staurophora, M. concava and M. swastica), P. cretacea and Watznaueria (W. barnesiae and W. fossacinta). Specimens occurring in minor amounts are referable to Biscutum, Chiastozygus, Retecapsa, and to the species C. reinhardtii, E. turriseiffelii, M. decoratus and R. bukryi. It was not possible to recognise marker species, but the occurrence of large specimens of A. cymbiformis, in significant amounts, and the unusual presence of the rare holococcolith R. bukryi, also recognised in the Epçeler Section, allows for the correlation between the two sections and the attribution of the Dereköy Section to the same late Maastrichtian age.
Orbitoides from the Taraklı Formation
Orbitoides from the Taraklı Formation in Epçeler and Dereköy (localities A-C) is represented by two morphologically distinct types; lenticular, symmetrical biconvex, rarely asymmetrical tests, assigned to O. ex. interc. gruenbachensis Papp–apiculatus Schlumberger, and biconcave- to flat ones, assigned to O. pamiri Meriç (Fig. 10). A comparison of the test diameter versus thickness of these species, and also that of O. ‘medius’ from the Maastrichtian of Arabian Plate, is shown in Fig. 11. Although both species have similar test dimensions, O. pamiri appears to be much thinner than O. ex. interc. gruenbachensis–apiculatus, with a high test diameter-thickness ratio compared to any species discussed here. A comparison of the axial sections of both species is given in Figs. 12 and 13, where the development of lateral chamberlets, thickness of the equatorial layer and stolon system are well observed. The measurements are tabulated in Table 2.
Orbitoides ex. interc. gruenbachensis Papp–apiculatus Schlumberger
In Epçeler A section, based on 21 specimens, test diameter of O. ex. interc. gruenbachensis–apiculatus varies between 2.95 and 6.8 mm, with sample averages ranging between 3.7 and 5.10 mm (Fig. 11; Table 2). Test thickness varies between 0.65 mm and 1.95 mm, with sample averages ranging between 0.96 and 1.41 mm. Test diameter to thickness ratio varies between 2.74 and 5.36 with a sample average of 3.83. The thickness of the equatorial layer (excluding the chamber wall) near its centre and periphery ranges between 75 and 165 µm and 105.0 and 245 µm with sample averages of 132.5 and 160.0 µm, respectively. Stolons connecting the equatorial chamberlets are about 20–25 µm in diameter in the early stage of development and 35–40 µm in the later stages. Orbitoides ex. interc. gruenbachensis–apiculatus possess predominantly large bilocular embryonic apparatus, a characteristic embryonic chamber arrangement commonly observed in O. apiculatus (Figs. 14a–e and 15). The average size of the embryonic apparatus (Li + li) in seven samples from both stratigraphic sections varies between 854.8 and 935.0 µm (Table 1). The average number of E varies between 13.0 and 14.30. These populations are assigned to a transitional development stage between O. gruenbachensis Papp and O. apiculatus Schlumberger according to the biometric species limits proposed by van Hinte (1976), which is designated as O. ex. interc. gruenbachensis–apiculatus (Fig. 16).
Orbitoides pamiri Meriç
Orbitoides from the Epçeler B section is only represented by O. pamiri. Based on 19 specimens, test diameter varies between 2.9 and 6.17 mm, with an average of 4.61 mm (Fig. 11; Table 2). Test thickness varies between 0.45 mm and 0.92 mm, with an average of 0.69 mm in sample EPB5. Test diameter to thickness ratio varies between 4.33 and 10.2 with a sample average of 6.09. The thickness of the equatorial layer (excluding the chamber wall) near its centre and periphery ranges between 85 and 150 µm and 170.0 and 440 µm, respectively, with a sample average of 238.1 µm in sample EPB5. Stolons connecting the equatorial chamberlets are about 35–40 µm in diameter in the late ontogenetic stages.
O. pamiri from Epçeler A, B and Dereköy sections possess invariably small tri- to quadrilocular embryonic apparatus commonly observed in O. tissoti and O. medius (Figs. 14f–k, 16, 17, and 18). The average size of the embryonic apparatus (Li + li) in nine samples from Epçeler A and B sections varies between 421.18 and 516.43 µm (Table 1). The average number of E varies between 3.95 and 4.13. It is interesting to note that some specimen of O. pamiri yielded embryonic apparatus with 3 epi-embryonic chamberlets (Fig. 16i and l).
Orbitoides from Terbüzek, Besni and Germav Formations
Orbitoides specimens from the Terbüzek, Besni and Germav Formations (localities D–F) are represented by symmetrical biconvex, rarely asymmetrical tests with notably large central piles in the central part of the test. These specimens were assigned to O. megaloformis in Terbüzek and Germav Formations and to O. ‘medius’ in the Besni Formation.
Orbitoides megaloformis Papp and Küpper
Orbitoides specimens from the Terbüzek Formation (Locality D; samples TF2 and 5) yielded tri- to quadrilocular embryons. The size of the embryon in both samples varies between 415.0 and 1155 µm, and 315.0 and 1050 µm, with sample averages of 700.3 and 698.4 µm, respectively (Fig. 19; Table 1). The average number of epi-embryonic chamberlets are 9.13 and 8.6, respectively. This population is assigned to O. megaloformis, although, typologically, some specimens with small embryons and a few epi-embryonic chamberlets (e.g. TF2–18, TF2–33 in Fig. 19) are within the limits of O. medius. Lepidorbitoides from both samples invariably possess quadriserial nepionts, with a few adauxiliary chamberlets (adc) only in some several specimens (Fig. 19). In sample TF2, out of 52 specimens, only three with one and one specimen with two adauxiliary chamberlets were found. In sample TF5, only three specimens, out of 35, with one adauxiliary chamberlets were found. These specimens with mean P, D, D/P and adc values of 98.65 µm, 147.12 µm, 1.5 and 0.1 in sample TF2 and 96.0 µm, 145.71 µm, 1.52 and 0.09 in sample TF5, respectively, were assigned to Lepidorbitoides bisambergensis (Jaeger) (Fig. 19).
Most Orbitoides specimens in the Germav Formation (Locality F; sample GA64) possess predominantly tri- to quadrilocular embryons. One single specimen yielded a bilocular embryon, typical for O. apiculatus (specimen GA64-84 in Fig. 19). Embryon size ranges between 410 and 910 µm, with the sample average of 596.4 µm. The mean E value varies between 4 and 13, with an average of 7.75. This population is assigned to O. ‘megaloformis’, although, in a typological sense, specimen with a bilocular embryon may be assigned to O. apiculatus.
Orbitoides ‘medius’ (d’Archiac)
Orbitoides specimens from the Besni Formation (Locality E; samples TC6, 7, 8, 9, 10 and 13) are characterised by having strongly biconvex tests with large piles in their central parts (Fig. 20). The asymmetrical tests occur rarely. Based on 14 specimens from samples TC7 and 13, test diameter varies between 2.25 and 4.41 mm, with samples averages of 3.88 and 3.3 mm, respectively (Table 2). Test thickness varies between 0.97 and 2.12 mm, with sample averages of 1.72 and 1.77 mm. Test diameter to thickness ratio varies between 2.02 and 2.49 and 1.73 and 2.3 with a sample average of 2.27 and 1.89. A comparison of the test diameter versus thickness of these specimens and those of O. medius from the Campanian of Oman, and O. pamiri and O. ex. interc. gruenbachensis–apiculatus from the Taraklı Formation is shown in Fig. 11. The thickness of the equatorial layer (excluding the chamber wall) near its centre and periphery ranges between 140 and 190 µm and 130 and 165 220 µm and 220 and 285 µm and 215 and 290 µm, respectively, with sample averages of 160.0 and 146.6 µm and 252.5 and 249.1 µm (Table 2). Stolons connecting the equatorial chamberlets are about 30–40 µm in diameter in the late stage of ontogenetic development. The embryonic apparatus consist of small tri- to quadrilocular embryons, within the biometric limits of O. medius, surprisingly much smaller than those from the underlying Terbüzek Formation (Fig. 19; Table 1). The size of the embryonic apparatus based on 144 specimens in 6 samples (TC6, 7, 8, 9, 10 and 13) varies between 345.0 and 950 µm, with sample averages ranging between 461.7 and 554.4 µm. The average number of epi-embryonic chamberlets ranges between 4.4 and 5.41. This population is assigned to O. ‘medius’, although, typologically, some specimens with larger embryons (e.g. TC8-47, TC6-33 in Fig. 19) are within the limits of O. megaloformis).
Orbitoides from the Beyobası Formation (Haymana Basin, Central Turkey)
Most of the specimens (34 out of 36) yielded bilocular and two yielded tri- to quadrilocular embryons (Fig. 8c, specimen DEG19-38). The size of the embryonic apparatus in bilocular specimens ranges between 665 and 1380 µm, with the sample average of 1023.4 µm (Figs. 8c and 16, Table 1). The mean E value varies between 11 and 20, with an average of 14.94. This population is assigned to O. apiculatus, although, in a typological sense, 2 specimens with small embryons may be assigned to O. ‘medius’.
Orbitoides from the Qahlah and Simsima Formations (Oman)
Orbitoides from the upper Campanian Qahlah Formation (locality G) is represented lenticular, symmetrical biconvex, rarely asymmetrical tests (Figs. 11, 21). These specimens are within the biometric limits of O. tissoti and O. medius and are assigned to O. medius considering the presence of well-developed lateral chamberlets and the number of epi-embryonic chamberlets (Table 2). A comparison of the test diameter versus thickness of this species with O. ‘medius’ from the Maastrichtian of Arabian plate and O. ex. interc. gruenbachensis–apiculatus from the Taraklı Formation is shown in Fig. 11. A comparison of the axial sections of O. medius and O. pamiri, which have a similar embryonic apparatus, is presented in Fig. 21. In sample BC6, the thickness of the equatorial layer near test centre and periphery ranges between 85 and 140 µm and 130 and 205 µm, with sample averages of 113.8 and 157.1 µm, respectively (Table 2). The stolons at the peripheral equatorial chamberlets are about 25–30 µm in diameter. The embryonic apparatus in all specimens is tri- to quadrilocular and shows a range of size between 260 and 690 µm, with sample averages ranging between 440 and 450 µm (Fig. 21; Table 1). The average number of epi-embryonic chamberlets ranges between 4.2 and 4.36.
The rare Orbitoides from the lower part of the Simsima Formation at Jabal Huwayyah (samples B28 and B32) yielded two types of embryons: a large, multilocular embryons and small ones with typical tri- to quadrilocular appearance in equatorial sections. In sample B28, the large multilocular embryon with Li + li value of 1710.0 µm is assigned to O. gensacicus, and two specimens possessing small, tri- to quadrilocular embryons with an average Li + li value of 477.5 µm are assigned to O. ‘medius’ (Fig. 22). These specimens have only 4 epi-embryonic chamberlets. In sample B32, two Orbitoides specimens are characterised by a large embryon with an average size of 1660 µm (Fig. 21). The number of epi-embryonic chambers could not be counted. These specimens are assigned to O. gensacicus. Two specimens characterised by trilocular embryons, with an average Li + li value of 527.5 µm are assigned to O. ‘medius’ (Fig. 22).
The new data presented herein permit us to interpret the Maastrichtian Orbitoides from the Central Sakarya Basin and Arabian Platform in a broader Tethyan context for the first time and allow us a comparison with the records from Western Europe. In general, our data from various Maastrichtian localities in the Arabian Platform (Turkey and Oman) and Central Turkey show the predominance of ‘O. medius’-like specimens with small tri- to quadrilocular embryons and fewer epi-embryonic chamberlets, previously considered characteristic for the Campanian (Fig. 6). These specimens are characterised by two morphological types: biconvex tests (O. ‘medius’), and flat to biconcave tests (O. pamiri) and do not show any sign of reworking in terms of test features and composition of the associated foraminifera. Orbitoides are intact and well preserved without any sign of abrasion or decortication. No older foraminifera (e.g. Campanian foraminifera) were found in association with this species. In our material, O. pamiri is very abundant in the Taraklı Formation and all specimens are flat and/or biconcave in shape.
The Arabian Platform sequence in Southeastern Turkey yields O. megaloformis–L. bisambergensis assemblages in its lower part (Terbüzek Formation) and an O. ‘megaloformis’ –L. gr. minor-socialis assemblage in its upper part (Germav Formation) (Özcan, 1994; Fig. 17). The Maastrichtian Orbitoides present in this succession are characterised by biconvex tests with similar features to those recorded in some localities in Iran and Oman (Abdelghany, 2003; Payandeh et al. 2019). Considering the mean values of embryon size (Li + li) and number of epi-embryonic chamberlets (E), an evolutionary trend is not observed. Contrary to the principle of nepionic-embryonic acceleration, the most ‘evolved’ populations occur in the Terbüzek Formation and ‘primitive’ ones in the overlying beds of the Besni Formation which contains biconvex tests with predominantly O. medius-type embryonic apparatus, associated with S. calcitrapoides, O. anatoliensis, S. cf. orbitoidiformis, and C. cf. mamillatus, Loftusia spp. (Özcan, 1993, 2007). The Germav Formation contains an O. ‘megaloformis’ assemblage with few specimens possessing O. apiculatus-type bilocular embryonic apparatus (Fig. 19).
In addition to the advanced specimens of the main Orbitoides lineage, which are here assigned to a transitional stage from O. gruenbachensis to O. apiculatus, the Maastrichtian Taraklı Formation yielded invariably flat to biconcave tests possessing very small embryonic apparatus (in the range of O. tissoti and O. medius) and a low number of epi-embryonic chambers (with predominantly 4 chamberlets), thus, very much resembling the Campanian species O. tissoti and O. medius in equatorial sections. These specimens, however, have well-developed lateral layers, making them distinct from O. tissoti, a very thick equatorial layer, almost twice as thick as that those of the biconvex specimens, and numerous large stolons connecting the equatorial chamberlets. Moreover, the number of lateral chamberlet cycles is much less than the biconvex Orbitoides specimens (compare the specimens in Figs. 12 and 13). In previous studies with well-documented morphometric data from Europe and Turkey, Orbitoides tests were invariably reported to be symmetric to asymmetrical in outline, with rare occurrences of plano-convex tests (Baumfalk & Willemsen, 1986; Caus et al. 1996; Eggink & Baumfalk, 1983; Meriç, 1965; Özcan, 1993). These variations were always interpreted as ecophenotypic, linked with prevailing environmental conditions (Eggink & Baumfalk, 1983; van Gorsel, 1978). The flat to biconcave specimens with small embryons from the Taraklı Formation strongly resemble to O. apiculata pamiri first described by Meriç (1974) from the upper Maastrichtian beds from SW Turkey. Meriç (1974) reported the associated foraminifera as O. apiculatus, O. medius, L. minor, O. macroporus, S. calcitrapoides, L. anatolica and H. beotica. A comparison of the axial sections of our flat to biconcave specimens (O. pamiri) with O. medius from the upper Campanian of Oman (Kayğılı et al. 2021) is given in Fig. 21. Both species have similar morphometric values for the size of the embryon and number of epi-embryonic chamberlets (Table 1). O. medius differs from O. pamiri in having biconvex tests, numerous lateral chamberlets and a thinner equatorial layer.
Based on the above data, we assert that biconvex and flat to biconcave Orbitoides populations from the upper Maastrichtian of Central Sakarya Basin and Taurides do not belong to the main Orbitoides evolutionary lineage. We think that O. ‘medius’ and O. pamiri represent offshoots from the main lineage in the Maastrichtian (Fig. 23), forming side-lines to the main lineage. These offshoots probably took place at levels corresponding to L. minor and/or L. socialis in the Maastrichtian since the record of the genus until the level with L. bisambergensis appears to be consistent with the species succession of O. medius–O. megaloformis–O. gruenbachensis in the Tethys. Well-dated Campanian deposits in two localities in Turkey yielded data consistent with this scheme. Helicorbitoides voigti van Gorsel and Pseudosiderolites vidali (Douvillé) recorded from the Tonya Formation in NE Turkey are associated with O. medius (Özcan et al. 2019), and O. megaloformis (Erdem et al. 2021), consistent with the record at the Campanian type section at Aubeterre. Caus et al. (1996) reported an O. gruenbachensis population from Maurens (Spain) associated with L. bisambergensis. This population does not contain O. medius-type embryons. We think that these inconsistent variations and widespread and common occurrence of flat to biconcave tests in at least two geographically separate regions in Turkey cannot simply be explained by environmentally induced morphological changes.
The principle of nepionic–embryonic acceleration demonstrated in many orbitoidal groups (Drooger, 1993) is also applicable in Orbitoides as recorded from single and separate sections from the late Santonian–Maastrichtian time interval in Western Europe. Nonetheless, our data also imply the significance of test features not only related with the equatorial layer but also lateral layers and overall test morphology in general. The biconvex specimens from the upper Maastrichtian of the Haymana Basin in Central Turkey were provisionally assigned to O. ‘medius’ because of their great resemblance to this species on the morphometric grounds (Özcan & Özkan-Altıner, 1997) and their distinction as a separate species from O. pamiri requires a detailed study.
The hypothesis that a distinct separate lineage of Maastrichtian Orbitoides occurs in addition to the classic lineage formed by progressive evolution of key biometric characteristics (notable E and Li + li) is supported by:
In Maastrichtian-aged sediments of the Besni Formation of Southeastern Turkey, Orbitoides biometrically similar to O. medius occur, overlying the Terbüzek Formation with O. megaloformis, and underlying the Germav Formation with O. megaloformis and possible O. apiculatus. We refer to such forms with the informal name O. ‘medius’, to indicate that whilst they are very similar to O. medius in morphometric terms they represent a distinctively young retrograde or perhaps long-lived lineage that requires further study.
Within the Taraklı Formation of the Central Sakarya Basin, large biconvex specimens, with relatively large, complex embryons, referable to O. ex. interc. gruenbachensis–apiculatus, occur alongside flat-biconcave Orbitoides, with relatively small simple embryons in the biometric range of O. medius. We refer these to the overlooked species O. pamiri on the distinctive combination of morphology and embryon size and complexity.
Limited records of probable O. ‘medius’ occurring alongside O. apiculatus are also known from the Maastrichtian sediments of the Haymana Basin of Central Turkey.
O. medius is known from the Campanian Qahalah Formation of Oman, whilst the overlying Maastrichtian Simsima Formation yields O. ‘medius’.
The recognition of O. ‘medius’ in undoubtedly Maastrichtian strata invites investigation of past records of O. medius. For example, this species has often been reported from Maastrichtian strata in the Middle East (e.g. Payandeh et al. 2019; Rahaghi, 1976; Schlagintweit et al. 2016) and Italy (Chiocchini et al. 2012). These records need to be re-examined to assess whether (i) these occurrences can be verified as O. medius; and (ii) if they are genuine Maastrichtian records.
Retrograde evolution within Orbitoides has been reported previously from the Caribbean bioprovince. There Mitchell (2005) reports the occurrence in uppermost Maastrichtian strata of a form he terms “Orbitoides cf. megaloformis”. Biometrically, this taxon would appear very similar to O. megaloformis from typically upper Campanian strata (Fig. 7). This could be a further example of parallel lineages of Orbitoides occurring in the Maastrichtian, although it should be noted that the Caribbean is a separate bioprovince from the Mediterranean and Arabian Tethys (Goldbeck, 2007).
The recognition of multiple lineages of Maastrichtian Orbitoides requires the integration of both morphometric analysis of embryon features coupled with consideration of external morphologies, that can be demonstrated not be simply ecophenotypic. Hence, a combination of morphometric and typological approaches can be beneficial for recognising the speciation of Late Cretaceous Orbitoides and identifying parallel evolutionary lineages.
Availability of data and materials
All thin sections and oriented sections are deposited in the Palaeontology Section of the Department of Geological Engineering (İstanbul Technical University).
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Material from the Taraklı Formation in Central Turkey was collected within the context of a TUBITAK (Turkish Research Council) Project (no: 116Y127). Fieldwork in Oman for EÖ and İAA was supported by Sultan Qaboos University (Project No: IG/SCI/ETHS/18/03). We thank Lorenzo Consorti (Trieste) and Esmeralda Caus (Barcelona) for their reviews that helped to improve this contribution. Aral Okay acknowledges support from Turkish Academy of Sciences (TÜBA). Mike Bidgood provided useful critical comments. This paper is dedicated to Dr. Engin Meriç (İstanbul), the author of many important contributions on the Late Cretaceous benthic foraminifera of Turkey.
This work was supported by TUBITAK (Turkish Research Council) Project (no: 116Y127) and by Sultan Qaboos University (Oman) (Project No: IG/SCI/ETHS/18/03).
We report no potential conflict of interest.
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Taxonomic list of the calcareous nannofossils recognised in the samples from Epçeler and Dereköy sections. All the references below are reported in http://www.mikrotax.org/Nannotax3
Arkhangelskiella cymbiformis Vekshina, 1959.
Biscutum constans (Górka, 1957) Black in Black and Barnes, 1959.
Biscutum ellipticum (Górka, 1957) Grün in Grün and Allemann, 1975.
Ceratolithoides aculeus (Stradner, 1961) Prins and Sissingh in Sissingh, 1977
Chiastozygus Gartner, 1968.
Cribrocorona gallica (Stradner, 1963) Perch-Nielsen, 1973.
Cribrosphaerella ehrenbergii (Arkhangelsky, 1912) Deflandre in Piveteau, 1952.
Cyclagelosphaera reinhardtii (Perch-Nielsen, 1968) Romein, 1977.
Eiffellithus gorkae Reinhardt, 1965.
Eiffellithus turriseiffelii (Deflandre in Deflandre and Fert, 1954) Reinhardt, 1965.
Lithraphidites quadratus Bramlette and Martini, 1964.
Lithraphidites praequadratus Roth, 1978
Markalius inversus (Deflandre in Deflandre and Fert, 1954) Bramlette and Martini, 1964.
Microrhabdulus decoratus Deflandre, 1959.
Micula concava (Stradner in Martini and Stradner, 1960) Verbeek, 1976.
Micula praemurus (Bukry, 1973) Stradner and Steinmetz, 1984.
Micula staurophora (Gardet, 1955) Stradner, 1963.
Micula swastica Stradner and Steinmetz, 1984.
Prediscosphaera cretacea (Arkhangelsky, 1912) Gartner, 1968.
Prediscosphaera ponticula (Bukry, 1969) Perch-Nielsen, 1984.
Retecapsa angustiforata Black, 1971.
Retecapsa crenulata (Bramlette and Martini, 1964) Grün in Grün and Allemann, 1975.
Russellia bukryi Risatti, 1973.
Zeugrhabdotus Reinhardt, 1965.
Watznaueria barnesiae (Black in Black and Barnes, 1959) Perch-Nielsen, 1968.
Watznaueria fossacincta (Black, 1971) Bown in Bown and Cooper, 1989.
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Özcan, E., Yücel, A.O., Catanzariti, R. et al. Multiple Orbitoides d’Orbigny lineages in the Maastrichtian? Data from the Central Sakarya Basin (Turkey) and Arabian Platform successions (Southeastern Turkey and Oman). Swiss J Palaeontol 140, 8 (2021). https://doi.org/10.1186/s13358-021-00219-x
- Central Sakarya Basin
- Arabian Platform margin