The Shillong Plateau in NE India consists of a Precambrian basement and is covered by Cretaceous and Cenozoic sedimentary deposits in the south, which form a raised topography in the foreland of the Himalayas (Fig. 1) (Biswas et al., 2007; Najman et al., 2016). The southern fringes of the Shillong Plateau, commonly referred to as the southern Shillong Plateau, form the Khasi–Jaintia Hills. The Paleogene succession exposed in the southern Shillong Plateau is represented by the Paleocene fluvio-deltaic Langpar and Therria formations, consisting of fine calcareous shales with occasional limestone bands and a thick sandstone succession, and the overlying Sylhet Limestone Group subdivided into several units: the Lakadong, Umlatdoh, and Prang formations intercalated with two mainly sandstone units (Lakadong Sandstone and Narpuh Sandstone) (Wilson and Metre, 1953). These units are interpreted to record three marine transgressions in the late Paleocene, the early Eocene, and the middle Eocene and are overlain by the upper Eocene Kopili Formation (Jauhri, 1994, 1998). The Lakadong Formation consists of the Lakadong Limestone Member, comprising shallow marine algal–foraminiferal facies, extensively developed in the Khasi and Jaintia Hills, and the Lakadong Sandstone Member, a sandstone–shale unit with coal seams (Jauhri, 1994; Garg and Khowaja-Ateequzzaman, 2000; Srivastava and Prasad, 2015). In the Lakadong Formation, LBF occur only in the Lakadong Limestone Member and this unit has been extensively studied for red algae and LBF (Jauhri, 1994, 1998; Jauhri and Agarwal, 2001; Matsumaru and Jauhri, 2003; Jauhri et al., 2006; Gogoi et al., 2009; Tewari et al., 2010; Matsumaru and Sarma, 2010). The age of the unit has been reported either as late Paleocene or to range from the late Paleocene to the early Eocene at different outcrops in Meghalaya based on LBF, most commonly alveolinids and miscellaneids. The unit contains diverse assemblages, including miscellaneids, alveolinids, rotaliids, orthophragminids, textulariids, miliolids, encrusting foraminifera, coralline and dasycladalean algae, gastropods, echinoids, bivalves, and scarce coral fragments.

Figure 2The Lakadong Limestone in MQS, position of the samples and simplified stratigraphic column of the quarry. The position of the boundary between SBZ 3 and 4 is tentative. The position of the lower samples (C1–5) from the first bench (B1), are not seen here. B: benches in the limestone.

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Figure 3Records of orthophragminids in the Paleocene and across the Paleocene–Eocene boundary in Tethys and SE India. The Shallow Benthic Zones (SBZ) are after Serra-Kiel et al. (1998), modified by Drobne et al. (2014) and Papazzoni et al. (2017) with respect to the Paleocene–Eocene boundary. The orthophragminid zones (OZ) are from Less et al. (2007) and their boundaries with respect to SBZ zones are after Papazzoni et al. (2017). The alveolinid zones are after Hottinger (1960) and Drobne (1977).

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The Lakadong Limestone was logged in the Mawmluh Quarry section (MQS), located near the Mawmluh cement factory, ca. 2.5 km southwest of Cherrapunji on the southern Shillong Plateau (base of the section: 25^∘15^′26.72${}^{\prime \prime }$ N, 91^∘42^′47.01${}^{\prime \prime }$ E; top of the section: 25^∘15^′23.39${}^{\prime \prime }$ N, 91^∘42^′52.03${}^{\prime \prime }$ E) (Fig. 1). Here, the outcropping succession is about 36 m thick and consists of dolomite, dolomitic limestone, limestone with intervening levels of shale, siltstone, and sandstone (Fig. 2). Although the bottom of the section is largely obliterated by alluvium, nearby exposures of the unit reveal that in the MQS the exposed lower part of the Lakadong Limestone is very close to the contact with the underlying Therria Formation.

A total of 31 samples from the indurated limestone–dolomitic limestone, and some loose orthophragminid specimens from levels C5, 9, 24, 25, 27, and 28, were collected (Fig. 2). Specimens extracted from the shale, marl, and limestone beds were studied for their external and internal features in equatorial and axial sections. Oriented equatorial sections of megalospheric and partly microspherical specimens (A and B forms, respectively) were prepared because the most important taxonomic and evolutionary parameters are observed in this part of the test (Less, 1987; Ferràndez-Cañadell, 1998). Biometric measurements and counts were carried out on equatorial sections of the megalospheric specimens (Less, 1987, 1998). Finally, axial and subaxial sections of megalospheric forms were prepared and photographed in order to facilitate specific recognition in rock thin sections.

The late Paleocene phylogeny of Tethyan orthophragminids was reconstructed from localities in Europe and the peri-Mediterranean region, a part of the western Tethyan bioprovince (Schlumberger, 1903; Douvillé, 1922; Neumann, 1958; Samuel et al., 1972; Less, 1987; Zakrevskaya, 2007; Less et al., 2007; Özcan et al., 2014), whereas a systematic study from the eastern Tethys is lacking. In the western Tethys, Paleocene orthophragminids are represented by several species (lineages) of Discocyclina Gümbel and Orbitoclypeus Silvestri, enabling us to characterize the Thanetian by two orthophragminid zones (OZ), 1a, b and a part of OZ 2 crossing the Paleocene–Eocene boundary (Less et al., 2007). These zones correspond to the Tethyan Shallow Benthic Zones (SBZ) 3, 4, and in part 5 (sensu Papazzoni et al., 2017) (Fig. 3).

The Paleocene orthophragminids from eastern Tethys, however, are little known either because of the absence of the group in some Paleocene key outcrops in Tibet and Pakistan or because of the difficulty in obtaining free specimens for detailed taxonomic study as in the case of MQS. The Paleocene deposits in Pakistan (e.g., the Lockhart Limestone in the Salt Range) and the Tethyan Himalayas (e.g., the Zhepure Shan and Zongpu formations in Tingri and Gamba regions in Tibet, China) did not yield orthophragminids but only orbitoidiform foraminifers such as Orbitosiphon Rao and Lakadongia Matsumaru and Jauhri (= Setia Ferràndez-Cañadell, see below), in addition to other LBF (Nagappa, 1959; Hu et al., 1976; Wan, 1991; Ferràndez-Cañadell, 2002; Wan et al., 2010; Zhang et al., 2013) (Fig. 3). The earliest orthophragminids in the Salt Range are known after the Paleocene–Eocene boundary in the Alveolina vredenburgi Zone (SBZ 5) (Ferràndez-Cañadell, 2002). From the Tethyan Himalayas of Tibet they have been first recorded in the mid–late Ypresian (SBZ 9/10) (Zhang et al., 2013); their first occurrence from the Asian plate (Zhongba area) in Tibet has been recorded much earlier, in the late Thanetian (SBZ 4) (BouDagher-Fadel et al., 2015). In the eastern Tethys, to the southeast of Tingri and Gamba, Paleocene orthophragminids, associated with Glomalveolina primaeva Reichel, Orbitosiphon punjabensis (Davies), Lakadongia tibetica (Douvillé), miscellaneids, and rotaliids, have been reported only from the Lakadong Limestone in the Shillong Plateau in the Meghalaya region (e.g., Mawmluh Quarry section) (Dutta and Jain, 1980; Jauhri, 1994, 1998; Jauhri et al., 2006; Matsumaru and Jauhri, 2003; Matsumaru and Sarma, 2010; Tewari et al., 2010). These orthophragminids were previously mainly described from axial and tangential sections in rock thin sections and were assigned to either Discocyclina or Orbitoclypeus with contrasting species-level identifications. Jauhri (1998) first mentioned the occurrence of Orbitoclypeus ramaraoi (O. schopeni ramaraoi of Less, 1987) in the Lakadong Limestone from the Um Sohryngkew River section near the Therria village in the southern Shillong Plateau, without any illustration and discussion. The orthophragminids from the same section, however, were assigned to Discocyclina by Jauhri et al. (2006) without any reference to Orbitoclypeus previously reported by Jauhri (1998). Matsumaru and Sarma (2010) recorded Orbitoclypeus ramaraoi in oblique sections, although these authors also incorrectly assigned some sections of Orbitoclypeus to Orbitosiphon tibetica.

Further southward along the Indian subcontinent, Paleocene orthophragminids have been recorded only from the Cauvery Basin (Pondicherry area) in SE India (Samanta, 1967). Here, the orthophragminids are represented only by Orbitoclypeus schopeni ramaraoi, the most primitive member of the O. schopeni lineage. The associated LBF assemblages of this area are poorly characterized (Govindan, 2013) and the identification of Ranikothalia by Samanta (1980) should be revised: his figured specimens do not show a marginal chord and appear to be rotaliids (Daviesina), not nummulitids. The assemblages do not permit the assignment of a precise SBZ age to these shallow-marine deposits consisting of strongly burrowed, several-meter-thick argillaceous carbonates. Records of late Paleocene orthophragminids from the Andaman Islands are similarly based on loosely dated assemblages yielding Ranikothalia (Koley and Wanjarwadkar, 2013).

Figure 4Thin-section photomicrographs of foraminiferal and algal assemblages in the Lakadong Limestone. 1: miscellaneid foraminifer–red algal wackestone–packstone with miscellaneids (mi); 2–3, 7–8: Glomalveolina-dasycladalean algae–miliolid wackestone–packstone with Glomalveolina cf. sireli (gs), Glomalveolina primaeva (gp), Ranikothalia sp. (ra), Elazigella altineri (el), and miliolids (mil); 4, 6, 9–10: miscellaneid foraminifera-Glomalveolina wackestone–packstone with Lockhartia sp. (lo), miscellaneids (mi), Bakalovaella sp. (ba), Glomalveolina levis (gl); 5: Aberisphaera-red algal wackestone–packstone with Aberisphaera sp. (ab), Orbitoclypeus schopeni (os) and Orbitosiphon pubjabensis (or); 11–12: orthophragminid-red algal- Distichoplax packstone–grainstone with Ranikothalia sp. (ra), Orbitoclypeus schopeni (os), Distichoplax biserialis (db) and red algae (ra). 1: sample C2; 2: sample C6; 3: sample C8; 4: sample C10; 5: sample C12; 6: sample C12A; 7: sample C15; 8: sample C16; 9: sample C17; 10: sample C19; 11: sample C22; 12: sample C23.

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Figure 5Lithostratigraphic column of the Lakadong Limestone in MQS, facies, and distribution of LBF and other fossil groups with inferred SBZ zones by Serra-Kiel et al. (1998). Facies explanation: 1: miscellaneids-red algal wackestone–packstone, 2: Glomalveolina-dasycladalean algae-miliolid wackestone–packstone, 3: Aberisphaera-red algal wackestone–packstone, 4: miscellaneids-Glomalveolina wackestone–packstone, 5: Lakadongia-Glomalveolina wackestone–packstone, 6: dasycladalean algal wackestone, 7; orthophragminid-red algal- Distichoplax packstone–grainstone.

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Figure 6Distribution of algae in MQS. See Fig. 5 for facies explanation.

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The Lakadong Limestone contains a diverse association of benthic foraminifera of such groups as the miscellaneids, alveolinids, orthophragminids, rotaliids, miliolids, and textulariids, accompanied by dasycladalean and coralline algae, rare corals, bryozoans, echinoids, bivalves, and gastropods (Figs. 4–6). The foraminifera are represented by the following genera: Orbitoclypeus Silvestri, Lakadongia Matsumaru and Jauhri (= Setia Ferràndez-Cañadell, see below for detailed explanation); Orbitosiphon Rao; Ornatanomalina Haque; Lockhartia Davies; Miscellanea Pfender; Carterella Sirel; Ranikothalia Caudri; Elazigella Sirel; Rotalia Lamarck; Aberisphaera Wan; Glomalveolina Hottinger; Rotorbinella Bandy; Idalina Munier-Chalmas and Schlumberger; Valvulina d'Orbigny; Orduella Sirel; Globotextularia Eimer and Fickert; Mardinella Meriç and Çoruh (= Azzarolina Vicedo and Serra-Kiel); Periloculina Munier-Chalmas and Schlumberger; Cincoriola Haque; Kathina Smout; and Pachyrotalia Hottinger (Fig. 5). The unit consists of wackestones–packstones dominated by LBF and coralline–dasycladacean algae, which are characteristic of inner- to middle and middle to outer shelf environments (Nebelsick et al., 2005) (Figs. 4 and 5). Most of the section, between samples 1 and 20, yielding alveolinids, miscellaneids, and rotaliids, was deposited in an inner to middle shelf setting, whereas the upper part (samples 21–28), with orthophragminids and less abundant rotaliids and miscellaneids, was deposited in a middle to outer shelf depositional setting. This suggests a general deepening upsection. Among the alveolinids, the occurrence of Glomalveolina cf. sireli and also G. primaeva in the lower and middle part of the section is significant for the assignment of SBZ 3. The first appearance of Glomalveolina cf. levis in sample C17 is used to place the boundary between SBZ 3 and SBZ 4, which corresponds tentatively to 22 m in the section.

Orthophragminids are scarce in the interval from the first sample of the section up to sample C20, where Distichoplax biserialis becomes abundant. The occurrence of Lakadongia, abundant in the middle part of the section below sample C21, declines sharply upward in the section, with a single record in the last sample (C28). The orthophragminids are subdivided into two lineages of the genus Orbitoclypeus Silvestri, the lineages of O. schopeni (Checchia-Rispoli) and O. multiplicatus (Gümbel). In the lower part of the section (SBZ 3 and lower part of SBZ 4), the specimens belonging to Orbitoclypeus schopeni are identified as O. schopeni ramaraoi based on morphometry (with an average D_mean value of 188.3 µm for sample C21), whereas those in the upper part (SBZ 4) represent a transitional development stage between O. schopeni ramaraoi and O. schopeni neumannae (with average D_mean values ranging between 192.9 and 198.3 µm). The embryon diameter of O. multiplicatus, recorded only in SBZ 4, ranges between 300.0 and 318.3 µm on average, corresponding to the transitional development stages of O. multiplicatus haymanaensis and O. multiplicatus multiplicatus.

Algae are essentially represented by red and green algae, among which Distichoplax biserialis (Dietrich) Pia is the most common in MQS (Fig. 6). Fragments of other corallinaceans also occur through the section, while  crustose thalli of Lithoporella sp. are only recorded from sample C15 up to sample C28. Polystrata alba (Pfender) Denizot is occasionally found. Among green algae, dasycladales are predominant. Thyrsoporellids are rather common throughout the section and include Thyrsoporella turgidipora Radoičić, Belzungia pfenderae Radoičić, and Özgen-Erdem, Belzungia cf. terquemi Morellet and Morellet, Dissocladella gracilis Radoičić and Furcoporella diplopora Pia, the latter species being found only in the middle and upper part of the section. Among neomerids, Indopolia cf. satyavanti Pia and Cymopolia aff. sirmiensis Radoičić are recorded. Acetabulariaceans are characterized by Clypeina rotella Wang, Acicularia tavnae Radoičić, and Orioporella malaviae Pia. Apart from Ovulites morelleti Elliott commonly occurring in the lower-middle part of the section, other green algae bryopsidales are found in the upper part and consist of disc-like segments of Halimeda cf. tuna Lamouroux and a large specimen tentatively identified as Arabicodium sp. Dasycladaleans inhabit shallow warm waters (Valet, 1979) in particular thyrsoporellids are interpreted to prefer mid-ramp environments (Barattolo, 2002). Many taxa recognized in the MQS are characteristic for European and North African Thanetian–Ypresian successions. Indopolia satyavanti, Orioporella malaviae, and Clypeina rotella are recognized here for the first time from the NE Indian area. The latter species, recorded only at its type locality in Tibet, is poorly known.

Figure 7(a) General test features in Tethyan orthophragminid genera (after Less, 1987; Ferràndez-Cañadell, 1997; Özcan et al., 2016b). (b) Qualitative parameters: 1: types of embryon configurations; 2: types of adauxiliary chamberlets, 3: different growth patterns of the equatorial annuli; 4: types of granules and lateral chamberlets on the test surface; and (c) parameters used in the morphometric description of orthophragminids as illustrated in Orbitoclypeus schopeni ramaraoi-neumannae from MQS.

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Table 1Statistical data for the orthophragminids from the Lakadong Limestone. For the illustration and explanation of the parameters, see Fig. 7c. N denotes the number of specimens studied in each sample. Asterisks indicate the measurements from random thin sections.

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Figure 81–2, 9–13, 22–24: Orbitoclypeus schopeni ramaraoi-neumannae; 1–2: external views, 9–13: axial sections, 22–24: equatorial sections of B forms. 1: C28–42, 2: C28–43, 9: C24–43, 10: C25–30, 11: C27–30, 12: C22–19, 13: C21, 22: C24–3, 23: C24–39, 24: C24–38. 3–8: Orbitoclypeus schopeni cf. ramaraoi; 3–4: equatorial sections, 3: C5–1, 4: C9–1. 5: slightly oblique equatorial section, C3–1. 6: axial section, C18, 7–8: off-center axial sections, 7: C2A, a microspherical form, 8: C12. 14–21: Orbitoclypeus multiplicatus haymanaensis-multiplicatus; axial to slightly off-center axial sections, 14: C21, 15: C21, 16: C21, 17: C21, 18: C21,19: C21, 20: C28, 21: C28.

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Figure 91–9: Orbitoclypeus schopeni ramaraoi-neumannae; equatorial sections, 1: C24–7, 2: C24–4, 3: C24–20, 4: C24–12, 5: C25–9, 6: C24–20, 7: C24–36, 8: C25–1, 9: C25–26. 10–13: Orbitoclypeus multiplicatus haymanaensis-multiplicatus; equatorial sections, 10: C24–6, 11: C24–41, 12: C24–45, 13: C27–31.

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Figure 10Embryon and equatorial chambers in Orbitoclypeus schopeni ramaraoi-neumannae. Note that the embryon is of eulepidine type, some equatorial chambers are incomplete and slightly wavy in pattern, and the distal sides of the chamberlets are arcuate to wedge shaped.

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Figure 11Embryon and equatorial chambers in Orbitoclypeus multiplicatus haymanaensis-multiplicatus. Note that the embryon is of excentrilepidine, umbilicolepidine, and trybliolepidine type, the equatorial chambers are incomplete, the distal sides of the chamberlets are arcuate to wedge shaped, and the peripheral chambers are radially elongated. The holotype of Orbitoclypeus multiplicatus haymanaensis from the Thanetian of Haymana Basin (central Turkey), sample KAR.8, is illustrated for comparison (Özcan et al., 2001).

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Figure 12Variation in the embryon and configuration of the embryonic chambers in Orbitoclypeus schopeni ramaraoi-neumannae in samples C24, 25, 27, and 28.

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Figure 131–3: Orbitoclypeus multiplicatus haymanaensis-multiplicatus; equatorial sections, 1: C28–20, 2: C28–19, 3: C27–1. 4–13: Orbitoclypeus schopeni ramaraoi-neumannae; equatorial sections, 4: C28–23, 5: C28–27, 6: C28–42, 7: C28–34, 8: C28–5, 9: C28–18, 10: C28–17, 11: C28–1, 12: C28–25, 13: C28–30.

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Figure 14Orbitoidiform foraminifers from the Lakadong Limestone. 1–5: Lakadongia sp.; 1, 3–5; off-center axial sections, 1: C2–23, 3: C2A-1, 4: C2A-13, 5: C2A-18, 2: section showing equatorial chambers, C2–39. 6–17: Lakadongia tibetica; 6–11; off-center axial sections, 6: C10–1, 7: C11–6, 8: C11–10, 9: C12–25, 10: C18–8, 11: C18A-4. 12–13: axial sections, 12: C18–3, 13: C16–62. 14–17: incomplete equatorial sections. 14: C12–9, 15: C12–7, 16: C16A–1, 17: C16. 18–21: Orbitosiphon punjabensis; off-center axial sections, 18: C10–4, 19: C12–1, 20: C12–20, 21: C8–4.

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We follow the taxonomic concept adopted for western Tethyan Paleocene orthophragminids by Less (1987) and Less et al. (2007). The details of morphometric discrimination of subspecies in orthophragminids are explained in Less and Kovács (2008). Eight test measurements (in micrometers) and counts and some qualitative data (e.g., types of embryon configurations and adauxiliary chamberlets) were used to characterize the taxa (Fig. 7 and Table 1). These measurements and counts are P and D, outer diameter of the protoconch and deuteroconch perpendicular to their common axis; A, number of adauxiliary chamberlets; H and W, height and width of the adauxiliary chamberlets; n_0.5, number of annuli within a 0.5 mm distance measured from the deuteroconch along the axis of the embryon; and h and w, height and width of the equatorial chamberlets around the peripheral part of the equatorial layer.

Order Foraminiferida Eichwald

Family Orbitoclypeidae Brönnimann

Genus Orbitoclypeus Silvestri

Orbitoclypeus schopeni (Checchia-Rispoli, 1908)

Diagnosis: Orbitoclypeus schopeni is an unribbed species with a “marthae” type rosette, a small to relatively large, eu-, tryblio-, and excentrilepidine embryon; narrow or medium wide, low or medium high “varians” type adauxiliary chamberlets; and also narrow or medium wide equatorial chamberlets arranged into circular or slightly undulated annuli usually with varians type growth pattern. The distal margins of the annular chamberlets are typically arched or wedge shaped. It commonly occurs in the orthophragminid assemblages from SW France to India, especially in the Thanetian and Ypresian. The earliest appearance is known from the lower Thanetian beds from India and SW France, with its reported highest occurrence from the late Lutetian (OZ 11) of Padragkút (Hungary) and San Pancrazio (OZ 12) (Italy). This species includes five subspecies in western Tethys: O. s. ramaraoi Samanta (D_mean<195 µm), O. s. neumannae Toumarkine (D_mean=195–240 µm), O. s. suvlukayensis Less (D_mean=240–300 µm), O. s. crimensis Less (D_mean=300–500 µm), and O. s. schopeni Checchia-Rispoli (D_mean>500 µm).

Orbitoclypeus schopeni (Checchia-Rispoli, 1908) ramaraoi (Samanta, 1967)-neumannae (Toumarkine, 1967): figs. 8.1–2, 9–13, 9.1–9, 10, 12, 13.4–13.

1967 Discocyclina ramaraoi n. sp. – Samanta: pp. 239–240, pl. 1, figs. 1–20, text-figs. 2–5.

1967 Discocyclina neumannae n. sp. – Toumarkine: pp. 210–212, pl. 1, figs. 1–8.

1987 Orbitoclypeus ramaraoi ramaraoi (Samanta) – Less: pp. 197–198, text-fig. 30b.

1987 Orbitoclypeus ramaraoi (Samanta) neumannae (Toumarkine) – Less: pp. 198–199, pl. 26, figs. 1, 2, text-fig. 30c.

2001 Orbitoclypeus neumannae (Toumarkine) – Özcan et al.: pp. 347, 348, 350, pl. 1, figs. 14–16, pl. 2, figs. 1–8, text-fig. 3C.

2007 Orbitoclypeus schopeni (Checchia-Rispoli) ramaraoi (Samanta) – Less et al.: pp. 441–442, pl. 3, figs. 20–22, Fig. 14.

2007 Orbitoclypeus schopeni (Checchia-Rispoli) neumannae (Toumarkine) – Less et al.: pp. 441–442, pl. 3, figs. 19, 23–29, Fig. 14.

2010 Orbitoclypeus ramaraoi (Samanta) – Matsumaru and Sarma: pl. 6, fig. 8.

2010 Orbitosiphon tibetica (Douvillé) – Matsumaru and Sarma: pl. 1, fig. 3.

2014 Orbitoclypeus schopeni (Checchia-Rispoli) ramaraoi (Samanta) – Özcan et al.: pp. 224–225, fig. 12.10–14, fig. 13–14, fig. 15.13–16.

Both the megalospheric (A forms) and microspherical (B forms) specimens have been studied, though the microspherical generation is rare and only five specimens were found among 143. The test is of medium size, circular in outline, mostly symmetrical with regard to the equatorial layer, and lenticular discoidal. The test diameter and thickness in A forms range between 1050 and 2800 and between 350 and 780 µm, respectively (Fig. 8.7–13). In the lower part of the section (e.g., samples C3, 5, 9), the specimens (O. schopeni cf. ramaraoi) have smaller tests, varying in diameter from 600 to 1200 µm (Fig. 8.3–6). The surface is smooth with uniformly distributed piles, coarser at the central part of the test (70–90 µm in diameter) and finer towards the periphery (20–50 µm in diameter). A large pile, 100–110 µm in diameter, is usually observed at the center of the test. The equatorial layer is about 35–60 µm high in axial sections. The average diameters of protoconch and deuteroconch range between 115.7–119.5 µm and 192.9–198.3 µm, respectively (Table 1). Both chambers invariably exhibit a eulepidine-type embryonic configuration. The number of adauxiliary chamberlets counted in 132 specimens varies between 13 and 23. The equatorial chamberlets are low and narrow in the early chambers and become radially elongated in the outer chambers. These chambers are slightly wavy in the equatorial sections and they usually form incomplete cycles (Fig. 10). The microspherical generation possesses a typical orbitoclypeid juvenarium, as shown in Fig. 8.22–24.

Remarks: Specimens from the lower part of the Lakadong Limestone (samples C3, 5, 9), as well as upper samples below sample C21 (Fig. 8.3–8), were assigned to Orbitoclypeus schopeni cf. ramaraoi due to sparse morphometric data from these levels. Specimens from the upper part (SBZ 4) represent transitional development stages between O. schopeni ramaraoi and O. schopeni neumannae with average D_mean values ranging between 192.9 and 198.3 µm (Table 1). Orbitoclypeus schopeni is differentiated from O. multiplicatus in having (a) a smaller embryon, (b) a different type of embryonic configuration (eulepidine in O. schopeni and excentrilepidine to umbilicolepidine type in O. multiplicatus), (c) a smaller number of adauxiliary chamberlets, and (d) smaller equatorial chambers/chamberlets, as recorded in parameter N_0.5. The average deuteroconch size of this species from SBZ 4 in MQS is slightly above the morphometric limit between O. s. ramaraoi, which stratigraphically extends to the early Eocene in the western Tethys, and O. s. neumannae. These records suggest that the average deuteroconch size of O. schopeni might be slightly larger than that in the western Tethys (Table 2).

Table 2Statistical data for O. schopeni ramaraoi from western Tethys. “No.” denotes the number of specimens studied in the samples.

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In previous works, Orbitoclypeus from the Lakadong Limestone has been apparently confused with the genera Discocyclina and Lakadongia. Matsumaru and Sarma (2010) illustrated several embryons in equatorial and uncentered equatorial sections as Orbitosiphon tibetica (Douvillé) from the Lakadong Limestone in Meghalaya. In fact, these specimens with different embryonic configurations and different features of equatorial chamberlets represent three different genera. The biloculine specimens illustrated in Plate 1, figs. 1 and 2 in Matsumaru and Sarma (2010) were correctly assigned to Orbitosiphon tibetica by the authors. The uncentered specimen with eulepidine embryon (fig. 3) represents an Orbitoclypeus schopeni ramaraoi and the specimen with isolepidine embryon and hexagonal peripheral chamberlets illustrated in fig. 4 represents a Nemkovella stockari Less & Özcan (see Özcan et al., 2016a). We think that the stratigraphic position of Nemkovella stockari, an early Eocene species as recorded in several localities (e.g., Turkey, Tunisia, Egypt, and Oman) in the western Tethys, has also been confused by the authors. The alleged occurrence of Discocyclina in the Lakadong Limestone (e.g., Jauhri et al., 2006) is not confirmed by the present study. Previous records of orthophragminids from Pondicherry (SE India), the Salt Range (Pakistan), Gamba and Tingri (Tibet) (Samanta, 1967; Hu et al., 1976; Wan, 1991; Ferràndez-Cañadell, 2002; Wan et al., 2010; Zhang et al., 2013), and the late Paleocene and early Eocene assemblages from the Indian subcontinent (Özcan et al., 2015, and this study) suggest that the genera Discocyclina and Orbitoclypeus do not co-occur in the Paleocene of the eastern Tethys. The co-occurrence of both genera is known from the Alveolina vredenburgi beds (SBZ 5) in the Salt Range and lower Eocene Patala Formation in Thal in Pakistan (Özcan et al., 2015; Ercan Özcan, unpublished data, 2015).

Orbitoclypeus multiplicatus (Gümbel, 1870)

Diagnosis: Average-sized, inflate, unribbed forms with marthae type rosette. The medium-sized to moderately large embryon is in most cases excentrilepidine, rarely eulepidine. The numerous varians type adauxiliary chamberlets as well as the equatorial chamberlets are rather wide and of average height. The annuli are usually moderately undulated; the growth pattern is of the varians type. This species includes four subspecies in the western Tethys: O. m. haymanaensis Özcan, Sirel, Özkan-Altıner and Çolakoğlu (D_mean <310 µm); O. m. multiplicatus Gümbel (D_mean=310–420 µm); O. m. kastamonuensis Less and Özcan (D_mean=420–550 µm), and O. m. gmundenensis Less (D_mean>550 µm).

Orbitoclypeus multiplicatus (Gümbel, 1870) haymanaensis Özcan et al., 2001 -multiplicatus (Gümbel, 1870): Figs. 8.14–21, 9.10–13, 11, 13.1–3.

2001 Orbitoclypeus haymanaensis n. sp. – Özcan et al.: pp. 344–345, 347, pl. 1, figs. 1–13, text-fig. 3A.

2007 Orbitoclypeus multiplicatus (Gümbel, 1870) haymanaensis Özcan, Sirel, Özkan-Altıner and Çolakoğlu, 2001 – Less et al.: pp. 439, pl. 3, figs. 1–3; Fig. 14.

2007 Orbitoclypeus multiplicatus multiplicatus (Gümbel, 1870) – Less et al.: pp. 439, pl. 3, figs. 5–9, 11–13; Fig. 14.

2014 Orbitoclypeus multiplicatus (Gümbel, 1870) haymanaensis Özcan, Sirel, Özkan-Altıner and Çolakoğlu, 2001 – Özcan et al.: pp. 223, figs. 12, 15–19, 21–25, Figs. 13–14, 19.

Only megalospheric (A forms) specimens have been found. The test is of medium size, circular in outline, mostly symmetrical with regard to the equatorial layer, and lenticular discoidal with a lobate periphery. The external test features are similar to those of O. schopeni and a clear distinction based on these features between these two species is not possible. The test diameter and thickness in A forms range between 1780 and 2050 and between 650 and 800 µm, respectively (Fig. 8.14–21). The surface is smooth with uniformly distributed piles, coarser in the central part of the test (50–100 µm in diameter) and finer towards the periphery (30–50 µm in diameter). A large pile is usually present at the center of the test. The equatorial layer is about 50–55 µm high in axial sections. The average diameters of the protoconch and deuteroconch range between 150.0–189.0 and 300.0–318.3 µm, respectively (Table 1). Both chambers exhibit excentrilepidine to umblicolepidine embryonic configuration (Fig. 11). The number of adauxiliary chamberlets counted in 27 specimens varies between 24 and 32. The equatorial chamberlets are relatively high and wide in the early chambers and may become radially elongated in the outer chambers. These chambers are slightly wavy in the equatorial sections and they usually form incomplete cycles (Fig. 11).

Remarks: O. multiplicatus, identified only in the upper part of the MQS, is much less abundant than O. schopeni. A distinction between O. multiplicatus and O. schopeni based on external characters is unfeasible because of the same test features; these species can be differentiated only in equatorial and axial sections. Less et al. (2007) indicated that the morphology and the evolutionary track of Orbitoclypeus multiplicatus and O. schopeni and O. varians are very similar. Therefore, the assignment of a given population to any of these three species is based mainly on the accompanying fossils. Moreover, they all gave rise to coeval lineages with ribs such as O. bayani, O. munieri, and O. furcatus, respectively, that are also very similar to each other.

The orbitoidiform foraminifers in MQS include two genera, Lakadongia Matsumaru and Jauhri, 2003, very common in SBZ 3 and rare in SBZ 4, and sparse Orbitosiphon Rao in SBZ 4 (Figs. 5 and 14). The orbitoidiform genus Setia, with type species Lepidorbitoides tibetica Douvillé from the Thanetian of Tibet, was introduced by Ferràndez-Cañadell (2002), who demonstrated that its architecture differs from that of the related and largely coeval genus Orbitosiphon Rao; both genera are restricted to Tibet, Pakistan, and India. Unfortunately, the name Setia was preoccupied by Setia Adams and Adams (Gastropoda: Rissoidae), a circumstance of which its author was not aware at that time (Carles Ferràndez-Cañadell, personal communication, 2010). Later, Matsumaru and Jauhri (2003) established the orbitoidiform foraminiferal genus Lakadongia from the Thanetian of Meghalaya, with type species Lakadongia indica Matsumaru and Jauhri. In turn, Ferràndez-Cañadell (2004) demonstrated L. indica to be a junior synonym of “Setia” tibetica Douvillé. Finally, unaware of Matsumaru and Jauhri (2003) and Ferràndez-Cañadell (2004), Özdikmen (2009) recognized that the name Setia Ferràndez-Cañadell, 2002 is preoccupied by Setia Adams and Adams and proposed the replacement name Novosetia. Notwithstanding the issue of the nomenclatural unavailability of the electronic publication in which it was published (Huber, 2007; ICZN, 2012), the genus-group name Novosetia Özdikmen is also invalid because there is an earlier available senior synonym, i.e., Lakadongia Matsumaru and Jauhri. This is in accordance with the Principle of Priority, as set forth by the ICZN (1999: Art. 23): if a scientific name is found to be unavailable or invalid, it must be replaced by the next oldest available name among its synonyms. Thus, the valid name for Setia Ferràndez-Cañadell is Lakadongia Matsumaru and Jauhri. The genus Lakadongia therefore includes two species, L. primitiva (Ferràndez-Cañadell, 2002) from the Hangu Formation, and the stratigraphically higher Lakadongia tibetica Douvillé from the Lockhart Limestone in the Salt Range in Pakistan. As of yet, this is the only locality where these Paleocene orbitoidiform foraminifers were studied in detail and the evolution of both genera has been recorded (Ferràndez-Cañadell, 2002). The Lockhart Limestone is generally considered upper Paleocene, although a firm shallow benthic zonation of the formation has not been proposed yet. Thus, the stratigraphic distribution of Lakadongia and Orbitosiphon and their species in the Lockhart Limestone are not well constrained in terms of SBZ. Our data from the Lakadong Limestone suggest that Lakadongia extends from SBZ 3 to 4, although it is rare in SBZ 4. This, however, may be due to facies change recorded by the prevalence of orthophragminids in the upper part of MQS. Due to lack of information for the embryonic stage of the genus, no species attribution was made for the specimens in the lower part of the section. Specimens of Lakadongia from the middle part of the MQS with two “first embryonic chambers” are confidently assigned to L. tibetica (Fig. 14.14–17). Orbitosiphon is poorly known from the MQS and only a few tangential sections are available (Fig. 14.18–21); thus its stratigraphic range cannot be precisely established.

Figure 15Stratigraphic columns of selected areas showing the correlation of Paleocene–early Eocene shallow marine sections in the Himalayan foreland basin in China, India, and Pakistan. A break in the sedimentation across the Paleocene–Eocene boundary is marked by an arrow. The map of Himalaya orogeny is from Jiang et al. (2015).

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Figure 16Distribution of Tethyan late Paleocene orthophragminids on late Paleocene–early Eocene paleogeographic base map (updated from Özcan et al., 2014). 1: Aquitaine Basin (France): Schlumberger (1903), Douvillé (1922), Neumann (1958), and Less (1998). 2: Adriatic Carbonate Platform (Slovenia): Drobne et al. (2012). 3: western Carpathians (Slovakia): Samuel et al. (1972). 4: central and eastern Crimea: Zernetskii (1977), and Zakrevskaya (2007). 5: Bulgaria: Less et al. (2007). 6: Armenia: Grigoryan (1986). 7: Haymana Basin (Turkey): Özcan et al. (2001). 8: Galala (Egypt): Özcan et al. (2014). 9: southern India: Samanta (1967). 10: Meghalaya (NE India).

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The late Paleocene to early Eocene corresponds to widespread shallow-marine sedimentation (mainly carbonates) along the northern margin of the Indian plate. Apart from other geological tools, stratigraphic development of the Paleogene sequences on the Indian craton was used as a tool to pinpoint the onset of the collision of the Indian and Asian plates (see Hu et al., 2016, for a synthesis and references therein). These deposits were investigated from Tethyan Himalayas, e.g., the Dibling and Zongpu formations (Garzanti et al., 1987; Green et al., 2008; Zhang et al., 2013; Jiang et al., 2015; Hu et al., 2016), and from the foreland basins in the sub-Himalayas, e.g., the Lockhart Limestone and Dungan Formation in the Salt Range and Sulaiman Range in Pakistan, and the Subathu and Dibling formations in northwest India (Najman et al., 2004; Afzal et al., 2011; Zhang et al., 2012) (Fig. 15). The cessation of the (shallow) marine sedimentation in the shelf and transition to continental setting, deposition of a laterally widespread conglomerate bed within the shallow-marine carbonates marking a break in sedimentation, and shoaling of the outer shelf deposits at or close to the Paleocene–Eocene boundary were commonly linked to the flexural uplift of the passive margin, marking the onset of the collision of the Indian and Eurasian plates (Garzanti et al., 1987; Zhang et al., 2012). In addition, thrusting of accretionary prism and trench complex over the Paleocene passive margin deposits was interpreted to hint the early sign for the onset of a collision (Beck et al., 1995). Nevertheless, a variety of ages ranging from Late Cretaceous to Oligocene–Miocene were assigned to the India–Asia collision based upon the various other criteria and hypotheses (see Hu et al., 2016, and references therein). The Paleocene–Eocene sections from the Shillong Plateau, which corresponds to the most eastern part of the foreland, however, were not taken into consideration in these reconstructions. Our data from Mawmluh show a sharp facies change from shallow-marine carbonates (Lakadong Limestone) to coal-bearing continental sandstones (the Lakadong sandstone) within SBZ 4. This corresponds to the oldest record for the cessation of marine carbonate sedimentation among the reported passive continental margin deposits (Fig. 15). Lakadong sandstone, ca. 25–250 m thick, consists of arkosic sandstone with thin carbonaceous shale and coal seams and is interpreted to have deposited in estuarine and lagoonal environments (Singh and Singh, 2000). Prasad et al. (2006) recorded the Paleocene–Eocene Thermal Maximum within the Lakadong sandstone and considered a significant part of the unit to be of Thanetian age. Our interpretation is that the drastic facies change in the MQS from a marine to continental setting within SBZ 4 corresponds to the oldest record for the cessation of the carbonate deposition along the passive margin. This was previously reported to be SBZ 6, which corresponds to a conglomerate horizon within the carbonates in the Gamba section in the Tethyan Himalayas (Zhang et al., 2012; Li et al., 2017).

The material can be accessed at the Geology Department of İstanbul Technical University.

The authors declare that they have no conflict of interest.