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Biostratigraphy of large benthic foraminifera from Hole U1468A (Maldives): a CT-scan taxonomic approach
Swiss Journal of Geosciences volume 111, pages 523–536 (2018)
Large benthic foraminifera are important components of tropical shallow water carbonates. Their structure, developed to host algal symbionts, can be extremely elaborate and presents stratigraphically-significant evolutionary patterns. Therefore their distribution is important in biostratigraphy, especially in the Indo-Pacific area. To provide a reliable age model for two intervals of IODP Hole U1468A from the Maldives Inner-Sea, large benthic foraminifera have been studied with computed tomography. This technique provided 3D models ideal for biometric-based identifications, allowing the upper interval to be placed in the late middle-Miocene and the lower interval in the late Oligocene.
Large Benthic Foraminifera (LBF) are important component in tropical carbonate platforms, major sediment producers and powerful tools for stratigraphic and environmental studies (Hottinger 1977; 1983; Schaub 1981; Lee and Hallock 1987; Pignatti et al. 1998; Serra-Kiel et al. 1998; Beavington-Penney and Racey 2004; Boudagher-Fadel 2008). Their tests present complex internal architectures, related to the presence of algal symbionts, that coupled with their external morphology, are fundamental for their taxonomy (Tan 1932; Loeblich and Tappan 1964; Haynes 1965; Hottinger 1977). Their distribution is controlled by temperature, light intensity, water energy, substrate type, nutrient availability and detrital input (Hohenegger 1994, 2000; Langer and Hottinger 2000; Renema et al. 2001; Beavington-Penney and Racey 2004; Renema 2007, 2018). LBF are particularly common and diverse in the Indo-Pacific, where, from the Paleogene to present-day, they massively contributed to carbonate production (Hallock 1981; Tudhope and Scoffin 1988; Renema et al. 2001; Renema 2006). Because of their high abundance, stratigraphy based on LBF represents a powerful dating tool (Van der Vlerk and Umbgrove 1927; Adams 1970; Chaproniere 1984; Boudagher-Fadel and Banner 1999; Boudagher-Fadel and Lokier 2005; Renema 2007). However, the correlation between carbonate platforms and the adjacent basin is challenging when independent age-controls are not available. LBF lineages can be regional, leading to further problems (Renema 2015). Specimen preparation is problematic in itself since perfectly oriented thin sections are necessary for reliable identifications (Briguglio et al. 2014). This approach is time consuming and destructive, making it impossible to obtain axial and equatorial sections of the same specimen (Briguglio et al. 2013). Computed tomographic scanner (CT-scan) overcomes these limitations, giving 3D representations of both external and internal structures along every possible section (e.g., Benedetti and Briguglio 2012; Hohenegger and Briguglio 2014; Briguglio and Hohenegger 2014; Briguglio et al. 2016).
Aim of this study is to provide a preliminary biostratigraphy for two intervals from Hole U1468A, drilled by the International Ocean Discovery Program (IODP) in the Inner Maldivian Sea, using LBF assemblages. Species identification follows a morphometric approach based on the results of the CT-scanning. Obtained ages are correlated with planktonic foraminifera and nannofossil distributions to provide independent age controls.
The Maldivian archipelago is a pure carbonate depositional system composed of two rows of atolls, separated by channels and surrounding the Inner Sea (Fig. 1; Aubert and Droxler 1996). Carbonate platforms surround the atolls, while periplatform ooze sedimentation, locally accumulating as drift deposits, occur in the Inner Sea (Droxler et al. 1990; Betzler et al. 2013). The sedimentation started between the early Eocene and Oligocene. At first it was restricted to narrow bands on the oceanward areas, leading to the formation of a double row of atolls. Subsequently, platform margins prograded toward the Inner Sea and current-related, clinoform bodies characterized the region from the late middle-Miocene (Betzler et al. 2017). In one of the channels connecting the Inner Sea to the ocean, IODP Expedition 359 drilled Hole U1468A (4°55.98′N, 73°4.28′E, water depth of 521 m; Fig. 1). The recovered succession features eight units, among them Units II, VII and VIII are characterized by shallow-water carbonates and a rich LBF fauna (Unit II, 45.7–192.5 mbsf, 6H–30F; Unit VII, 817.5–854.7 mbsf, 106X–109X; Unit VIII, 854.7–865 mbsf, 110X–111X; Betzler et al. 2017).
The first analyzed interval includes four regularly spaced samples spanning Unit II: 29F-CC; 22F-CC; 15F-CC and 7H-CC. The second interval consists of four samples covering Units VII-VIII: 110X-CC; 109X-CC; 108X-CC and 107X-CC. Samples were soaked in water, then washed through a 32 µm sieve and dried. In each sample LBF were selected, based on their external morphology, to represent the entire assemblage. 160 specimens were mounted with standard clear nail polish at distinct levels, 5 mm apart, around cylindrical Polyether ether ketone (PEEK) sample holders (Distrelec stock no. 148-21-756). Sample holders, manufactured in-house, were 6 cm in length, comprising a 5 cm length shaft (4 mm of diameter) and a 1 cm length base (6.4 mm of diameter; Fig. 2). The base serves for easy mounting into the Bruker SP-1212 and SP-1213 CT stage extenders. The shaft allowed the fixation of 5–8 specimens at each level, depending on size (Fig. 2). Similarly sized individuals were mounted at each level (Fig. 2). Specimens were scanned with a multi-scaled Bruker X-ray nano-computer tomographic scanner SkyScan 2211, using an open X-ray source with a diamond-window target at energies of 60 kV and currents of 350 µA. Images were acquired on a 11Mp cooled CCD detector resulting in a voxel resolution of 2 µm. 180° scans were taken with a rotation step of 1° (25′ of acquisition time for each level). Images were subsequently reconstructed with InstaRecon applying Gaussian smoothing, beam hardening and ring artifact corrections. Reconstructed images were analyzed with CTAn, CTVox and Avizo (FEI). After scanning, LBF specimens were removed from the PEEK sample holders with acetone.
The biometric study focused on equatorial sections integrating different procedures proposed in literature (Fig. 3; Tan 1932; Van der Vlerk 1959, 1963; O’Herne 1972; Matteucci and Schiavinotto 1977; Van Vessem 1978; Schiavinotto 1978; Chaproniere 1980; Hohenegger et al. 2000; Less et al. 2008; Özcan et al. 2009; Hohenegger 2011; Renema 2015; Benedetti et al. 2017; Torres-Silva et al. 2017). Species identifications were mostly based on biometric parameters. Following Özcan et al. (2009), the notation exemplum intercentrale (ex. interc.) was used whenever the mean value of the identifying parameter of a group of specimens fell very close to the limits of two contiguous species of the same lineage. The complete biometric dataset is provided online (Online resources 1–4).
Family Lepidocyclinidae Scheffen 1932
Genus Nephrolepidina Douville 1911
Test discoidal, biconvex with a distinct layer of equatorial chambers and lateral chambers on each side. Megalospheric stage with a protoconch only partially embrached by the deuteroconch.
Nephrolepidina ex. interc. rutteni Van der Vlerk 1924 -martinii Schlumberger 1900; Fig. 4a–n; Online resource 1.
Test biconvex, symmetrical and rounded. Surface with common, randomly distributed pustules representing the outer termination of thick pillars. Remnants of a collar can be observed along the equatorial plane. Embryo of megalospheric specimens small (PW = 105 μm; DW = 185 μm), with a rounded to slightly rectangular protoconch which is largely embraced by the deuteroconch (Ai = 61%). The wall enclosing the embryo is thick, while the wall dividing the two initial chambers is thin. No ACI observed on the protoconch, NPAC = 2. External surface of the deuteroconch almost completely covered by ACII (NACII = 6.3). Chambers on the equatorial plane disposed in a wavy concentric pattern (F = 4).
The average number of ACII observed in the examined specimens suggests a positioning between N. martini (6.5 > NACII>4.5) and N. rutteni (NACII > 6.5; Van Vessem 1978). No remarkable variability observed among the samples, B∑ACII is rather constant.
Nephrolepidina transiens Umbgrove 1929; Fig. 4o.
Test biconvex, symmetrical and rounded. Surface with common, randomly distributed pustules. Remnants of a collar can be observed along the equatorial plane. Embryo of megalospheric specimens large (PW > 250 μm; DW > 350 μm), with an irregularly shaped deuteroconch. Wall of the embryo thick and surrounded by a large number of irregularly-shaped auxiliary chambers. Equatorial chambers disposed in a wavy concentric pattern (F = 4).
Nephrolepidina ex. interc. isolepidinoides Van der Vlerk 1929 -sumatrensis Brady 1875; Fig. 4 p–x; Online resource 1.
Test biconvex, symmetrical and rounded. Surface characterized by common pustules. Remnants of a collar can be observed along the outer surface of the equatorial plane. Embryo small (PW = 130 μm; DW = 200 μm), composed of a rounded protoconch and a kidney-shaped deuteroconch, the latter only slightly encloses the protoconch (Ai = 43%). Wall enclosing the embryo as thick as the wall separating the first and second chambers. NPAC = 2 and NACII = 1.8, no ACI observed. Chambers on the equatorial plane disposed with an intersecting curve pattern (F = 1).
The low NACII observed in this population, coupled with the low Ai value, places these specimens between N. isolepidinoides and N. sumatrensis. The former is characterized by an Ai < 40% and NACII < 2.25, while the latter has an Ai > 40% and NACII > 2.25 (Van Vessem 1978). Both Ai and NACII are higher in the specimens from 107X-CC and lower in those from 108X-CC.
Family Nummulitidae De Blainville 1827
Genus Cycloclypeus Carpenter 1856
Test large, circular, with a central umbo and a narrow periphery. Megalospheric stage has a central embryo composed of two chambers followed by a short nepionic spire composed at first by undivided chambers and then by chambers divided into chamberlets by secondary septula. This nepionic spire is followed by annular chambers divided into chamberlets.
Cycloclypeus annulatus Martin 1880; Fig. 5a–i; Online resource 2.
Test large and flat, with a central area surrounded by annular inflations as thick as the umbo (the test between the annuli is thin and fragile). Outer surface lacking evident ornamentations. Embryo consisting of a circular protoconch and a large kidney-shaped deuteroconch (PW = 195 μm; DW = 245 μm). The first two chambers are followed by a third undivided chamber (X = 3) and this entire structure is surrounded by a thick wall. The wall separating the three chambers from each other is thin. Specimens generally characterized by 7 to 8 precyclical chambers (PC = 7.8; S4 + 5= 10.7).
Cycloclypeus eidae Tan 1930; Fig. 5j–n.
Specimens poorly preserved, broken and bioturbated. Test large and flat thicker at the center and thinner towards the edges. Outer surface granulated. Embryo composed of a small and rounded protoconch (PW 70 to 90 μm) and a hemispherical deuteroconch. One or two undivided chambers (X ≈ 3–4) and two whorls of nepionic chambers follow the embryo, after which annular growth starts.
Genus Heterostegina D’Orbigny 1826
Subgenus Vlerkina Eames, Clarke, Banner, Smout and Blow 1968 emended Banner and Hodgkinson 1991.
Test lenticular, biconvex, planispiral and involute. Embryo of megalospheric specimens composed of two chambers, followed by a variable number of undivided chambers. Later chambers are divided into chamberlets by secondary septula. Alar prolongations generally subdivided into lateral chamberlets. In axial section it present a single layer of lateral chamberlets is present for each whorl of the spire.
Heterostegina (Vlerkina) borneensis Van der Vlerk 1930; Fig. 5o–x; Online resource 3.
Test, involute, planispiral, flat and thicker at the center. Some specimens seems to have pillars in the central part of the test, but the external surface is generally abraded and bioturbated, therefore, it is unclear whether or not ornamentations were present. Alar prolongations are narrow and divide into a single layer of lateral chamberlets. Embryo large and composed of a rounded protoconch followed and a kidney-shaped deuteroconch (PW = 210 μm; DW = 250 μm). This structure is followed by one undivided chamber (X = 3; S3 + 4= 3.9; S4 + 5= 7; S10 = 7).
Heterostegina (Vlerkina) sp. 1; Fig. 6a–g; Online resource 3.
Test large, planispiral, involute and thick. Outer surface unornamented. Alar prolongations narrow and divided into lateral chamberlets. A single layer of lateral chamberlets is present for each whorl. Protoconch and deuteroconch small; two to three undivided chambers follow them (PW = 105 μm; DW = 110 μm; X = 5.5). Compared to H. (V.) borneensis the subsequent chambers have less subdivisions (S3 + 4= 2; S4 + 5= 2.8; S10 = 3.3).
This species differs from H. (V.) borneensis by its smaller protoconch, more undivided chambers after the embryo, and less chamberlets in the first divided chambers. It also differs from other coeval Heterostegina (Vlerkina) species of the Indo-Pacific. The protoconch is smaller than both Heterostegina (Vlerkina) pleurocentralis and Heterostegina (Vlerkina) assilinoides, it has more undivided chambers and less chamberelets in the 3rd, 4th, 5th and 10th chambers of the spire (Banner and Hodgkinson 1991).
Genus Operculina D’Orbigny 1826
Test lenticular, planispiral, from evolute to almost completely involute, with a lax spire. Septa can be regular or folded and can present partially developed septula.
Operculina complanata (De France In Blainville 1822); Fig. 6i–q; Online resource 4.
Test planispiral, entirely evolute and very flat, with a granulated surface. Alar prolongations absent. Protoconch small and rounded (PW = 42 μm). Deuteroconch small and kidney-shaped (PW = 23 μm). Septa are quite regular and they do not have septula.
Operculina cf. heterosteginoides; Fig. 6h–k; Online resource 4.
Test planispiral, entirely evolute, very flat, with a smooth outer surface. Alar prolongations absent. Embryo small and composed of a rounded protoconch and a hemispherical deuteroconch (PW = 60 μm; DW = 60 μm). Subsequent chambers partially divided by incomplete septula.
This species has a lax spire and fewer incomplete septula than the extant Operculina heterosteginoides. Evolute nummulitids with incomplete chamber divisions are have a complex taxonomic history (Renema 2018). Since their revision is beyond the purpose of this paper we simply compare this species with the extant O. heterosteginoides, the most similar living representative of the group.
Operculina sp.1; Fig. 6r–x; Online resource 4.
Test planispiral, moderately thick and involute with a smooth outer surface. Alar prolongations long and narrow. Embryo composed of a small rounded protoconch and kidney-shaped deuteroconch (PW = 35 μm; DW = 29 μm). Septa often bent and irregular as the main wall of the spire.
Nummulitidae sp. 1; Fig. 7a–f; Online resource 4.
Test planispiral, thick, lenticular and completely involute. Alar prolongation long and narrow, not extending over the center of the test. Embryo characterized by a small protoconch and a narrow, kidney-shaped, deuteroconch (PW = 48 μm; DW = 39 μm). Septa starting straight and slightly bending backwards close to the intersection with the wall of the subsequent whorl (BBA = 19).
Nummulites and Operculinella are both involute nummilitids. They are distinguished mainly by shape of the last whorl (Hohenegger et al. 2000; Renema 2018). The presence of trabeculae on the surface is also considered important by some authors (Hohenegger et al. 2000), as well as the number of chambers in each whorl and the BBA (Hohenegger et al. 2000; Renema 2018). Since the examined specimens were always broken and abraded, estimate the number of chambers per whorl, studying the last whorl and the superficial features was unfeasible. Thus, straightforward species identification was impossible.
Family Amphisteginidae Cushman 1927
Genus Amphistegina D’Orbigny 1926
Test low trochospiral, involute to partially evolute and unevenly to almost uniformly biconvex. Chambers of the spire strongly curved backward at the periphery.
Amphistegina lessonii D’Orbigny 1926; Fig. 7h–m; Online resource 4.
Test trochospiral, involute, lenticular, slightly asymmetrical and thick, with a smooth surface. Alar prolongations long and narrow. Protoconch and deuteroconch very small (PW = 30 μm; DW = 22 μm). Chambers subdivided by strongly backward bending septa (BBA = 41). Coiling with a low expansion rate and few chambers per whorl.
Amphistegina mammilla (Fichtel and Moll 1798); Fig. 7n–u; Online resource 4.
Test trochospiral, involute, slightly to remarkably asymmetrical, moderately thick, with a smooth surface. Dorsal side more convex than the ventral side. Alar prolongations long and narrow. Protoconch spherical and small, deuteroconch small and hemispherical (PW = 42 μm; DW = 45 μm). Septa of the chambers strongly bending backwards (BBA= 55).
Family Acervulinidae Schultze 1854
Genus Sphaerogypsina Galloway 1933
Test globular to somewhat irregular. Constructed of numerous layers of polygonal to squared chambers arranged in column and radiating from the center. Outer surface characterized by a chessboard pattern of raised and depressed chambers. Embryo located at the center of the test, surrounded by an area of unordered chambers.
Sphaerogypsina sp. 1; Fig. 7v.
Test small and spherical, with a mean diameter of 800 μm. Outer surface displaying the characteristic chessboard pattern. Embryo small and trochospiral. Embryonic area followed by a few rings of unordered chambers, which in turn are surrounded by chambers arranged in a more or less regular pattern of radial columns.
It is indistinguishable from Sphaerogypsina globula. The lack of clear characteristics to separate the species within this genus prevents an accurate identification.
Sphaerogypsina sp.2; Fig. 7w–x.
Test small and almost spherical (diameter of 750 μm). Outer surface exhibiting the characteristic chessboard pattern. Embryo bilocular, composed of a small elliptical protoconch and kidney-shaped deuteroconch. Embryonic area followed by a few rings of unordered chambers, which in turn are surrounded by chambers arranged in a regular pattern of radial columns.
In contrast from Sphaerogypsina sp.1, it exhibits a bilocular embryo. Additionally, the radial column of chambers are more regularly arranged. Such a major differences clearly suggests that they are separated species and has substantial taxonomic implications. Since the taxonomy of Sphaerogypsina is beyond the purpose of this biostratigraphic paper the subject is not further investigated. Sphaerogypsina sp.2 also fits perfectly within the broad definition of S. globula, but the lack of clear characteristics for species separation prevents an accurate identification.
In the first interval (Unit II, Samples 7H-CC to 29F-CC), LBF specimens are poorly preserved with evidence of abrasion and fragmentation. The assemblage is quite uniform with N. ex. interc. ruttenii-martinii and C. annulatus occurring in all examined samples (the latter is particularly poorly preserved and many specimens only possess the central part of the test; Table 1). Nephrolepidina. ex. interc martini-ruttenii suggests at late middle-Miocene to early late-Miocene age (Adams 1970; Van Vessem 1978; Boudagher-Fadel 2002; Sharaf et al. 2005). Van Vessem’s (1978) regards N. ruttenii as a more evolved species developing within the same lineage of N. martini and places this transition within Zone M11 (Wade et al. 2011). Chaproniere (1984) places these two species within the same lineage and their transition between Zones M9 and M10. Adams (1970) and Sharaf et al. (2005) consider N. martini and N. ruttenii two separate species, with overlapping stratigraphic ranges. For Adams (1970) N. martini is restricted to the middle Miocene while the range of N. ruttenii extends into the late Miocene. Sharaf et al. (2005) suggest a middle Miocene range for N. martini and an early to late Miocene range for N. ruttenii. The arrangement of equatorial chambers, which is stratigraphycally significant, supports a middle Miocene age (Chaproniere 1980; Betzler and Chaproniere 1993). Since the majority of the literature supports a M9 to M11 age for the examined Nephrolepidina, we will follow this line. Cycloclypeus annulatus ranges from the Burdigalian to the end of the Serravallian (Boudagher-Fadel and Lokier 2005; Sharaf et al. 2005; Hallock et al 2006; Renema 2015). Its presence restricts the possible age of the interval to zones M9 to M10 (Fig. 8). However, according to Renema (2015), the morphology of the examined C. annulatus is quite primitive and closer to those of Burdigalian and Langhian specimens. Nonetheless, planktonic foraminifera and calcareous nannofossil distributions support the M9 to M10 hypothesis. The interval from Sample 8HCC to 71X-CC should span between the Zones M9 and M11 as defined by the First Occurrence (FO) of Fohsella fohsi and Last Occurrence (LO) of Paragloborotalia mayeri (Fig. 8; Betzler et al. 2017; Spezzaferri et al. in prep.). Nannofossils distribution indicates a M5 to M12 age (Zones NN6 to NN15) for the interval 6H though 66X (Fig. 8; Betzler et al. 2017).
In the second interval (Units VII and VIII; Samples 107X-CC to 110X-CC) the majority of LBF are poorly preserved and fragmented, with extensive borings and authigenic mineral fillings. Sample 108X-CC, in particular, is dominated by fragments of lepidocyclinids, probably produced by the breakage of individuals with a prominent equatorial flange (the observed fragments have equatorial chambers arranged in an intersecting curved pattern similar to that of N. ex. Interc. isolepidinoides-sumatrensis). The LBF assemblage is more varied and diverse than in the first interval (Table 1). Sample 107X-CC is characterized by Nephrolepidina ex. interc. isolepidinoides-sumatrensis (closer to the N. sumatrensis-type), Heterostegina (Vlerkina) borneensis, and Cyclocypeus eidae (Table 1; Fig. 8). This assemblage suggests a late Oligocene age, equivalent to Zone O7 (Fig. 8; Adams 1970; Van Vessem 1978; Chaproniere 1984; Boudagher-Fadel and Lord 2000; Hallock et al. 2006; Sharaf et al. 2005; Lunt and Renema 2014). In Sample 108X-CC N. ex. interc. isolepidinoides-sumatrensis is closer to the N. isolepidinoides type. The assemblage includes also H. (V.) borneensis, while C. eidae is no longer present (Table 1; Fig. 8). This association is suggestive of an older age than Sample 107X-CC, ranging from Zones O4 to O7 (Chaproniere 1984; Van Vessem 1978; Boudagher-Fadel and Lord 2000; Sharaf et al. 2005; Lunt and Renema 2014). The only biostratigraphic marker in Sample 109X-CC is H. (V.) borneensis (Table 1; Fig. 8). The specimens still present alar prolongations divided into chamberlets, pointing toward a late Oligocene age (Lunt and Renema 2014). The presence of Heterostegina (V.) sp. 1 (more primitive than H. (V.) borneensis because of its higher X value and lower S4+5 value) suggests this sample may be older than both 107X-CC and 108X-CC. No age-diagnostic LBF were recognized in the lowermost sample, making its placement uncertain (Table 1).
Planktonic foraminifera and calcareous nannofossil distributions are in agreement with the LBF stratigraphy. Sample 107X-CC can be allocated to Zone O7 due to the FO of Paragloborotalia pseudokugleri, while an older age is suggested for 108X-CC and 109X-CC due to the presence of Chilogumbelina cubensis and Paragloborotalia opima (Fig. 8; Spezzaferri et al. in prep.). Nannofossils indicate that Sample 107X is younger than 27.27 Ma and, therefore, younger than Zone O6 (Fig. 8; Betzler et al. 2017).
CT-scan and LBF biostratigraphy
By providing a large number of 3D models in short time, X-ray tomography proved to be an useful tool for LBF stratigraphy (especially in a context where samples are limited and destroying them is not an option). Approximately 12 h for scanning and 72 h for processing the raw data were necessary to produce all 160 models (the measurements entailed an additional 48 h of work). The major limitation to this approach seems to be the preservation of the specimens. Since CT-scan imaging is based on density contrast, secondary infilling of the chambers (e.g., sediment, cement or authigenic minerals), may jeopardize the results, in this instances traditional thin sections are probably more effective. Actually, due to the poor preservation of the material it was often impossible to resolve most of the chambers, especially for the nummulitids. However, exquisite results were obtained with lepidocyclinids which were well preserved. Since this group includes some of the most reliable age-diagnostic LBF, fast CT-scanning could significantly improve the knowledge on lepidocyclinids distribution, by mass-producing high-quality data and allowing non-destructive examination of the holotypes. Although our technique is fast and very good for the study of large chambers along the equatorial plane, it may not be perfect to investigate the fine structure of alar prolongations or the volume and the 3D shape of the chambers, which are potentially crucial for nummulitids evolutionary history (e.g., Cotton et al. 2015; Renema and Cotton 2015). These elements, coupled with the study of growth-invariant parameters, are key elements for improving LBF taxonomy, phylogenesis and evolution (Hohenegger 2011; Renema and Cotton 2015). Nevertheless, our fast approach produced a reliable LBF-based stratigraphy that fits well with the available information on the distribution of both planktonic foraminifera and calcareous nannofossils. More detailed analyses of the lepidocyclinids, which are by far the most useful taxa in Hole U1468A, may refine the model and provide a powerful instrument for correlations. In this framework the use of independent age control systems, such as Strontium Isotope Stratigraphy, is crucial since planktonic foraminifera and calcareous nannofossils are rare in LBF-dominated intervals.
Large benthic foraminifera provided a reliable biostratigraphy for two shallow-water intervals in Hole U1468A. A late middle-Miocene age is suggested for Unit II and a late Oligocene age for Unit VII–VIII. These results are in agreement with the preliminary ages from planktonic foraminifera and calcareous nannofossils.
The evolution of the embryonic apparatus of Nephrolepidina appears to be an accurate biostratigraphic tool for this area. Further analyses focused on this genus will provide a powerful instrument to date these shallow-water deposits. The use of CT-scan proved to be valuable by producing non-destructive data in short time. This approach has the potential to advance biostratigraphy in shallow-water environments, opening new possibilities for paleontologists.
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We are grateful to the IODP for providing the samples used in this study. Christoph Neururer (Fribourg) is acknowledged for assistance during the CT scanning. Warm thanks to A. Collareta, W. Renema and J. Hohenegger for their useful suggestions. This study was supported by the Swiss National Science Foundation (200021_165852/1).
Editorial handling: D. Marty.
Electronic supplementary material
Online resource 1: Biometric values for Nephrolepidina. The number of analyzed specimens includes only those, which were sufficiently preserved.
Online resource 2: Biometric values for Cycloclypeus. The number of analyzed specimens includes only those, which were sufficiently preserved.
Online resource 3: Biometric values for Heterostegina. The number of analyzed specimens includes only those, which were sufficiently preserved.
Online resource 4: Biometric values for nummulitids and amphisteginids. The number of analyzed specimens includes only those, which were sufficiently preserved.
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Coletti, G., Stainbank, S., Fabbrini, A. et al. Biostratigraphy of large benthic foraminifera from Hole U1468A (Maldives): a CT-scan taxonomic approach. Swiss J Geosci 111, 523–536 (2018). https://doi.org/10.1007/s00015-018-0306-7