A refined foraminiferal biostratigraphy for the Late Campanian–Early Maastrichtian succession of northeast Iraq

The Shiranish Formation is the most geographically widespread lithostratigraphic unit of the Late Campanian–Early Maastrichtian succession in Iraq and contains rich and diverse benthonic and planktonic foraminiferal assemblages, including species of the benthonic foraminiferal genus Bolivinoides that can be used for high-resolution biostratigraphy. The Dokan and Azmer localities of the Kurdistan region, NE Iraq, have been selected for this study because they provide nearly complete successions through the Shiranish Formation (Figure 1). The lithostratigraphy and planktonic foraminiferal biostratigraphy of the Shiranish Formation have been described by several authors, most recently by Al-Banna (2010) and Hammoudi (2011). None of these studies have identified the biostratigraphic significance of Bolivinoides species in the Shiranish Formation.

Here we identify stratigraphically important Bolivinoides species, establish a biozonation that is useful for regional and interregional correlation, and more precisely define the Campanian–Maastrichtian boundary in NE Iraq. The newly refined biostratigraphy provides temporal constraint on the shallowing marine trend identified in NE Iraq, and enables regional comparisons with sea-level change on the Arabian Plate and globally.

Two stratigraphic rock successions, one at Dokan (latitude 35° 56′ 15″N and longitude 44° 57′ 21″E) and the other at Azmer (latitude 35° 37′ 30″N and longitude 45° 31′ 45″E; see Figure 1) have been chosen for analysis. These sections present near-complete Late Cretaceous successions of the Shiranish Formation that contain rich and diverse planktonic and benthonic foraminifer assemblages, especially of Bolivinoides. Samples were taken at a spacing ranging from 0.5 m in the soft marlstones to 2 m in the indurated marlstones and marly limestones. For indurated rock samples, thin-section analysis was used for planktonic foraminiferal identifications. For friable samples, a freeze-thaw method of processing was used (Mogaddam, 2002). Approximately 200–300 g of each friable sample was repeatedly frozen and thawed in a supersaturated solution of sodium sulphate until the rock disaggregated. Disaggregated sediments were then washed thoroughly through a 63 µm sieve and the residues separated by filtration and dried overnight with an oven temperature of 50ºC. Dried residues were sorted using sieves from 500 µm down to 63 µm. Foraminifera were picked and studied from the residue in the 63–300 µm size fractions. The foraminifera were studied using a Hitachi S-3600N Scanning Electron Microscope (SEM) at the University of Leicester, UK.

The Shiranish Formation represents marine shelf-deposited carbonates and mudstones that are rich in microfossil and macrofossil taxa (van Bellen et al., 1959-2005; Buday, 1980; Jassim and Goff, 2006). The Shiranish Formation unconformably overlies the marine limestones of the Kometan Formation (Mid Turonian–Early Campanian), and is succeeded conformably by marine clastic deposits of the Tanjero Formation (Late Maastrichtian) (Figure 2). van Bellen et al. (1959-2005) informally subdivided the Shiranish Formation into a ‘lower unit’, characterised by alternating foraminifer-rich marly limestone and calcareous marlstone, and an ‘upper unit’ that is dominated by blue marlstone in which the abundance of foraminifera decreases. The Shiranish Formation in the Dokan and Azmer areas is about 260 m and 144 m thick respectively. There is a glauconitic pebbly sandstone bed of about 0.5 m at the base of the Shiranish Formation (base of the ‘lower unit’) in the Dokan area (Figure 3) that may indicate a very slow rate of deposition or period of non-deposition. In the Dokan area the uppermost part of the ‘upper unit’ of the Shiranish Formation includes a massive bed of marly limestone that is about 1 m thick, bearing a mass of rudist bivalves near the contact with the overlying Tanjero Formation: this rudist bed is only locally developed and hence is not differentiated as a separate member in the Shiranish Formation.

Bolivinoides species provide one of the most highly resolved biostratigraphic subdivisions of Late Cretaceous strata globally (e.g. El-Nady, 2006). In order to place the Kurdistan assemblages into the context of this global stratigraphy, a total of 118 specimens of Bolivinoides have been collected from the Azmer and Dokan sections. Dimensions of the test and the number of lobes on the final chamber on the 114 complete specimens are shown in Table 1. We have not identified any intraspecific temporal trends in individual Bolivinoides species from our morphological analyses that would enable sub-division of zonal intervals. Nevertheless, the temporal succession in discrete Bolivinoides species can be used to establish three biozones and two subzones in the Shiranish Formation (Figure 3).

In NE Iraq this biozone is defined as the interval from the first to the last appearance datum of the nominate species and it is therefore a total range zone. It is identified in the ‘lower unit’ of the Shiranish Formation through a thickness of 158.5 m in the Dokan section and nearly 65 m in the Azmer section (Figure 3). Bolivinoides decoratus (Jones) is common at both localities and is restricted to Late Campanian strata (Figures 4 and 5). It was previously recorded with the same stratigraphical range in Europe (Hiltermann and Koch, 1950, 1955, 1962; Hofker, 1958; Hiltermann, 1963; Barr, 1966a, b; van Hinte, 1967), Atlantic Coastal Plain of New Jersey (Petters, 1977) and North Africa (Barr, 1970; Khalil, 1998; El-Nady, 2006). The first appearance datum of B. laevigatus Marie within the B. decoratus Biozone of NE Iraq enables subdivision of this interval into a lower B. decoratus Subzone and an upper B. laevigatus Subzone (see Figure 5). Based on co-occurring planktonic foraminifera in the Shiranish Formation (see Figure 6), the B. decoratus Biozone represents an equivalent stratigraphical interval to the Globotruncana aegyptiaca and lower part of the Gansserina gansseri planktonic foraminiferal biozones (see Robaszynski, 1998; Premoli Silva and Sliter, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004; Sari, 2006, 2009). The combined benthonic and planktonic foraminiferal biostratigraphy for the B. decoratus Biozone also enables the informal recognition of lower and upper Globotruncanaaegyptiaca and lower Gansserina gansseri intervals that may be important for more refined inter-regional correlation in the Middle East and North Africa (see Figures 5 and 6).

The lower boundary of the B. miliaris Biozone has been defined in Egypt (Khalil, 1998; see also El-Nady, 2006) by the last appearance datum (LAD) of B. decoratus, while the upper boundary of the zone is identified by the last appearance of B. miliaris (Hiltermann and Koch). In Egypt, B. miliaris and B. decoratus have overlapping ranges through much of the upper decoratus Biozone as recognised there (El-Nady, 2006), through an interval assigned to the Late Campanian (El-Nady op cit., Figure 3). Therefore, the base of the miliaris Biozone as it is recognised in Egypt is also identified by the FADs of Bolivinoides draco giganteus (Hiltermann and Koch) and B. draco draco (Marsson). However, El-Nady (2006, p. 685) stated, in contradiction to his range chart, that B. miliaris is an excellent marker for the Campanian/Maastrichtian boundary. In this paper we define the B. miliaris Biozone as a total range zone, with no overlap with B. decoratus. We believe that the decoratus-miliaris biozonal boundary equates to the Campanian/Maastrichtian boundary, as this level is also associated with the FAD of Bolivinoides draco in Iraq, and with the FADs (Figure 6) of the planktonic foraminifera Rugoglobigerina hexacamerata Bronnimann, R. pennyi Bronnimann and Planoglobulina acervulinoides (Egger), which are regarded as markers for the basal Maastrichtian in other regions (Zepeda, 1998; Li et al., 1999; Guray, 2006; Beiranvand and Ghasemi-Nejad, 2013; see Figure 6). The B. miliaris Biozone is identified in the uppermost part of the ‘lower unit’ and the lower part of the ‘upper unit’ of the Shiranish Formation (Figure 3), in the Dokan succession occupying a stratigraphic thickness of 39 m. However, in the Azmer section, the biozone is confirmed only through 26 m of strata: this is due to the rapid disappearance of foraminiferal assemblages upwards in the rock succession at Azmer (Figure 3). Bolivinoides miliaris occurs rarely in Iraq and is restricted to the earliest Maastrichtian. B. miliaris is recorded from the same stratigraphical range in Europe (Hiltermann and Koch, 1950), Atlantic Coastal Plain of New Jersey (Petters, 1977), North Africa (Le Roy, 1953; Said and Kenawy, 1956; Barr, 1970; Khalil, 1998; El-Nady, 2006), and the Caribbean (Beckmann and Koch, 1964). In NE Iraq the B. miliaris Biozone represents an equivalent stratigraphical interval to the middle part of the Gansserina gansseri planktonic foraminiferal Biozone (for which, see Robaszynski, 1998; Premoli Silva and Sliter 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004; Sari, 2006, 2009): this is based on the co-occurrence of B. miliaris with G. gansseri, and on its stratigraphic position above the B. decoratus Biozone. Combining the benthonic and planktonic foraminifer occurrences allows the informal recognition of an upper Gansserina gansseri interval in the Iraqi succession (see Figure 6).

In Iraq, the B. draco (Marsson) Biozone is a partial range zone that is defined as the interval from the last appearance datum of B. miliaris to the last appearance datum of B. draco. B. draco is rare in its lowermost range in Iraq, where it overlaps with B. miliaris, and becomes abundant after the extinction of B. miliaris. The B. draco Biozone is identified in the upper part of the ‘upper unit’ of the Shiranish Formation in the Dokan section through nearly 37 m of strata. A succeeding biozone is not recognised in the Dokan section, while the B. draco Biozone is absent at Azmer (Figure 3), probably as a consequence of environmental change caused by the rapid shallowing-up succession and the concomitant disappearance of foraminifera. In Egypt, El-Nady (2006) recognised the incoming of Bolivinoides paleocenicus (Brotzen) and B. peterssoni Brotzen at the base of the B. draco Biozone as he defined it, though we have not identified these taxa in Iraq. El-Nady (2006) also recorded B.miliaris as rare in the lowermost B. draco Biozone. Therefore, the base of the B.draco Biozone as we define it in Iraq most likely lies at a lower stratigraphic level than in Egypt (see Figure 4).

The associated planktonic species within the B. draco Biozone of Iraq are Contusotruncana contusa, C. patelliformis, C. walfischensis and Gansserina gansseri, which also signal the Early Maastrichtian and, in the case of C. contusa, the late Early Maastrichtian (Figure 6). These foraminifera indicate that the B. draco Biozone represents an equivalent stratigraphical interval to the upper part of the Gansserina gansseri and the lower part of the Contusotruncana contusa (Cushman) planktonic foraminiferal Biozone (for which, see Robaszynski, 1998; Premoli Silva and Sliter, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004; Sari, 2006; 2009).

At the Global Stratotype Section and Point (GSSP) at Tercis, southwestern France, the first appearance of the ammonite Pachydiscus neubergicus is taken as the marker of the Campanian/Maastrichtian (C-boundary, and this level also coincides with the first occurrences of the planktonic foraminifera Rugoglobigerina scotti and Contusotruncana contusa (Odin, 1996; Odin and Lamaurelle, 2001). At the GSSP the evolutionary lineages of the genus Bolivinoides have also been used to recognise the C-M boundary, the base of the Maastrichtian coinciding with the FAD of Bolivinoides specimens with 5 lobes on the last chamber (Odin and Lamaurelle, 2001). Bolivinoides with 5 lobes on the final chamber also characterise the base of the Maastrichtian in NE Iraq, but the first occurrences of R. scotti and C. contusa appear later in the Iraqi succession (see Figure 6), a situation apparently repeated in Iran (Darvishzad and Abdolalipour, 2009), Tunisia (Li and Keller, 1998a, b; Li et al., 1999) and NE Iraq (Sharbazheri, 2010; Ismael et al., 2011). The relative ranges, therefore, of the key planktonic and benthonic foraminifer species differ between the type section at Tercis and Iraq. Thus, the planktonic species R. scotti, C. contusa and the benthonic 5-lobed Bolivinoides species appear simultaneously at Tercis, but in Iraq the first occurrence of the planktonic species post-dates the appearance of 5-lobed Bolivinoides. Here, based on the total succession of foraminifera in our assemblages, we take the appearance of 5-lobed Bolivinoides as the more reliable marker for the C-M boundary and infer that the appearances of R. scotti and C. contusa are diachronous globally.

Before the selection of the GSSP, the extinction of the planktonic foraminifer Radotruncana calcarata had long been used to define the C-M boundary (van Hinte, 1965; Postuma, 1971; Wonders, 1980; Robaszynski et al., 1984; Olsson and Nyong, 1984; Caron, 1985; Sliter, 1989): however, several subsequent studies have shown that the LAD of R. calcarata significantly pre-dates the FAD of the boreal belemnite species Belemnella lanceolata (Burnett et al., 1992; Hancock et al., 1992) which has been regarded as another index for the C-M boundary. Based on these findings, Hancock et al. (1992) suggested that the position of the C-M boundary in Tethyan sections was best placed at the FAD of the planktonic foraminifera Gansserina gansseri. However, recent studies show that the FAD of Gansserina gansseri also pre-dates the C-M boundary (Robaszynski, 1998; Premoli Silva and Sliter, 1999; Robaszynski et al., 2000; Premoli Silva and Verga, 2004; Sari, 2006, 2009; also Figures 5 and 6).

Li et al. (1999) informally used the FAD of the planktonic foraminifer Rugoglobigerina hexacamerata for the C-M boundary based on biostratigraphic correlation with the geomagnetic time scale at Deep Sea Drilling Project (DSDP) site 525 in northwest Tunisia. Zepeda (1998) used the FAD of Rugoglobigerinapennyi for defining the C-M boundary in the Exmouth Plateau, northwest Australia and eastern Indian Ocean. In NE Iraq we use the first occurrences of the planktonic foraminifera Planoglobulinaacervulinoides, R. pennyi and R. hexacamerata within the Gansserina gansseri Biozone (Li and Keller, 1998a, b; Li et al., 1999; Zepeda, 1998; Robaszynski, 1998; Guray, 2006; Esmeray, 2008; Beiranvand and Ghasemi-Nejad, 2013) as additional evidence to identify the C-M boundary. These first occurrences coincide with the FAD of Bolivinoides with 5 lobes, especially B. miliaris.

Foraminifer assemblages in the Shiranish Formation indicate a gradual decrease in marine shelf water depth through the succession. High diversity foraminiferal assemblages characterise the ‘lower unit’ of the Shiranish Formation and include agglutinated species. These assemblages comprise species of the benthonic foraminifera Ammodiscus, Allomorphina, Clavulinoides, Glomospira, Pleurostomella, Praebulimina, Pullenia, Osangularia and Quadrimorphina, and in particular the taxa Bathysiphon, Dorothia and Gaudryina that suggest a middle slope environment with water depths of at least 600 m (Sliter and Baker, 1972; Sliter, 1973). This ‘lower unit’ of the Shiranish Formation also contains the benthonic foraminifera Clavulinoides trilatera (Cushman), Marginulina bullata Reuss, Nuttallides truempyi (Nuttall), Gyroidinoides globosus (Hagenow) and Praebulimina kickapooensis (Cole) that are useful indicators for middle slope environments (Sliter and Baker, 1972; Olsson and Nyong, 1984; Alegret and Thomas, 2001): the ‘lower unit’ is also characterised by rich planktonic assemblages of Globotruncana species. Towards the top of the B. decoratus Biozone the benthonic foraminifer assemblages are dominated by species of Gavelinella, Gyroidinoides, Gaudryina, Lenticulina, Marginulinopsis, Neoflabellina, Osangularia, Praebulimina and Spiroplectammina species, which suggest an upper slope environment with water depths ranging between 400 to 300 m (Sliter, 1972; Sliter and Baker, 1972). The top of the B. decoratus Biozone of the Shiranish Formation contains Bathysiphon vitta Nauss, Gaudryina pyramidata Cushman, Marssonella oxycona (Reuss), Nuttallinella florealis (White) and Osangularia cordieriana (d’Orbigny) that are useful indicators for upper slope environments (Sliter and Baker, 1972; Olsson and Nyong, 1984; Alegret and Thomas, 2001).

Foraminiferal assemblages in the topmost part of the ‘lower unit’ in the Azmer section and the ‘upper unit’ in the Dokan section of the Shiranish Formation suggest shallower marine conditions. The benthonic foraminifer assemblages at the level of the B. miliaris and B. draco biozones are species of Bolivina, Dentalina, Fissurina, Gyroidinoides, Nodosaria and Oolina which indicate an outer neritic shelf environment of about 200 m water depth (Sliter, 1972; Sliter and Baker, 1972). This unit also includes Bolivina incrassata gigantea Wicher and Praebulimina carseyae (Plummer) that are useful indicators for outer neritic shelf environments (Sliter and Baker, 1972; Olsson and Nyong, 1984). Planktonic foraminifer assemblages are characterised by Rugoglobigerina, Globigerinelloides, Hedbergella and Heterohelix species; according to Sliter (1972) and Hart (1980) species of these genera most likely characterised shallow marine depths.

The intra-Campanian unconformity recognised across the Arabian Plate is represented in the Dokan and Azmer sections at the cessation of deposition of pelagic limestones of the Kometan Formation (Early Campanian) followed by deposition of glauconitic pebbly sandstone at the base of the overlying Shiranish Formation (see van Bellen et al., 1959-2005; Jassim and Goff, 2006; Aqrawi et al., 2010; Lawa et al., 2013). The marine erosional surface represents a gap of the mid to early Late Campanian in which the biostratigraphically useful species Globotruncana ventricosa, Rodotruncana calcarata and Globotruncanella havanensis are not recorded.

The lithofacies of the Shiranish Formation suggest the combined influence of eustasy and local subsidence on sea-level change, the latter resulting from structural loading of the Arabian Plate by obducted Neo-Tethyan margin rocks (Jassim and Goff, 2006). The lower part of the ‘lower unit’ of the Shiranish Formation (within the Bolivinoides decoratus Subzone) represents a major deepening upwards succession indicated by an increasing planktonic to benthonic foraminifer ratio. The middle part of the ‘lower unit’ of the Shiranish Formation (that part assignable to the Bolivinoides laevigatus Subzone) is marked by a maximum flooding surface with palaeodepths of at least 600 m (Figure 7) and is characterised by marl beds associated with the predominance of a planktonic lime-mudstone facies. Thereafter, in the upper part of the ‘lower unit’, foraminiferal evidence suggest that sea level begins to fall (see Figure 7).

In the B. miliaris Biozone the Shiranish Formation is characterised by continued sea-level fall that is identified by increasing dominance of benthonic foraminifera, a sudden drop in the abundance of globotruncanids, and an increase in the heterohelicid population associated with the presence of Pseudotextularia and Planoglobulina species. Collectively these suggest decreasing marine shelf depths to some 200 m (Sliter, 1972; Abdel-Kireem, 1983; Darvishzad and Abdolalipour, 2009; see Figure 7).

Haq et al. (1987) and Hardenbol et al. (1998) proposed a major marine regression in the Early Maastrichtian that coincided with major global cooling phases at 71.2–69.2 Ma (Figure 7). Moreover, Barrera (1994) noted that the Early Maastrichtian was the coolest interval of the Cretaceous following the peak warmth of the earlier Late Cretaceous. Therefore, sea-level change in the Iraq succession might relate to Late Cretaceous climate change, as indicated by correlation from the Bolivinoides biozonation.

The same period of sea-level regression is also recorded in Iran (Darvishzad and Abdolalipour, 2009), Turkey (Sari, 2006, 2009) and in other parts of Iraq (El-Anbaawy and Sadek, 1979; Abdel-Kireem, 1983; Al-Banna, 2010; Fayyadh, 2010). In this study the sea-level curve for NE Iraq is generally consistent with the Haq et al. (1987) global sea-level curve, but it is substantially different from the Arabian Plate sea-level curve of Sharland et al. (2001), suggesting strong regional (tectonic?) controls on relative sea level on the Arabian Plate during the Late Cretaceous.

Here we highlight key morphological characters that we have used to diagnose Bolivinoides species in the Shiranish Formation, comparing our material with the original descriptions of the species. Specimens figured in Plates 1 to 3 are deposited in the collections of the British Geological Survey, Keyworth, Nottingham, UK and are identified by the prefix MPK.

Bolivinoides australis Edgell (Plate 1, Figs 1 and 2) was originally described from the Late Cretaceous succession of NW Australia (Edgell, 1954). Our material is conspecific with that of Edgell (op. cit.) based on its pyriform lateral shape and ovate cross-section; its smooth initial chambers, while later chambers are pustulate; and in possessing a final chamber that typically has between 5 and 6 thick, closely spaced lobes. The length/breadth ratio of the Iraqi material is between 1.4 and 1.6, thereby differentiating B. australis from B. decoratus, which has a smaller length/breadth ratio, a different shape, and more closely spaced lobes on the final chambers.

Bolivinoides decoratus (Jones) (Plate 1, Figs 3–9; Plate 2, Figs 1–5) was originally described and illustrated in Wright (1886) from the Chalk Group at Keady Hill, County Derry, Northern Ireland. However, the name had been used before by Jones in unpublished work and for that reason, Wright graciously attributed Jones with authorship of Bolivina [= Bolivinoides] decorata. The Iraqi material is typical of this species in being kite-shaped in lateral view, with an elliptical cross-section. The earliest chambers are smooth or weakly lobed; ornamentation on later chambers is more prominent, with 3 to 4 thick, distinct lobes on the final chambers. The length/breadth ratio is between 1.5 and 2.1, most commonly between 1.7 and 1.9.

Marsson (1878) described Bolivina [=Bolivinoides] draco (Plate 1, Figs 10–12; Plate 2, Figs 6 and 7) from the Maastrichtian of Rügen Island in the Baltic Sea, Germany. The material from the Shiranish Formation possesses the typical diamond-shaped lateral morphology of this species and the test also has a compressed cross-section. The ornament comprises two, species-diagnostic, centrally positioned

parallel ribs extending along the entire length of the test, separated by a central depression. In larger forms, the ribs are intersected by overlapping side-ribs at an angle of about 35° to 40° in the later part of the test. The length/breadth ratio of the test is generally between 1.3 and 1.5.

The type material of Bolivinoides laevigatus Marie (Plate 1, Figs 13 and 14; Plate 2, Fig. 8) is from the Late Campanian of the Paris Basin (Marie, 1941). Iraqi specimens have the characteristic narrow, slowly expanding test and elliptical cross-section of Marie’s material. Earlier chambers are smooth or with up to two lobes, later chambers become weakly lobate, and there are three lobes on the final chambers. Lobation weakens towards the periphery. The length/breadth ratio is between 1.9 and 2.0. Bolivinoides laevigatus can be distinguished from B. decoratus by its smaller test and more weakly developed ornamentation.

Bolivinoides miliaris Hiltermann and Koch (Plate 1, Figs 15 and 16; Plate 2, Figs 9 and 10) is a distinctive taxon with its broad rhomboidal lateral shape and elliptical to ovate cross-section. The ornament comprises long irregular lobes, numbering five on the last pair of chambers. The maximum breadth of B. miliaris is near the mid-point of the test. The length/breadth ratio is between 1.0 and 1.2, most commonly 1.2. Bolivinoides miliaris is most similar to B. draco, but is distinguishable by its long, irregular, discontinuous lobes, the absence of central ribs, and by its broader rhomboidal shape. Our material possesses the characteristic morphology of the German material described by Hiltermann and Koch (1950).

Bolivinoides praelaevigatus Barr (Plate 2, Figs 11 and 12) was described from the Late Cretaceous of Britain (Barr, 1966a). It has a very distinctive, gradually tapering, narrow test, with a compressed shape in cross-section. The test surface is smooth to weakly lobed, with 2 or 3 lobes on the final chambers. Its length/breadth ratio is very distinctive at between 2.1 and 2.3.

The Late Campanian–Early Maastrichtian succession of NE Iraq can be subdivided into three Bolivinoides biozones: the B. decoratus Biozone (Late Campanian), subdivided into lower B. decoratus and upper B. laevigatus biosubzones; the B. miliaris Biozone (Earliest Maastrichtian) and the B. draco Biozone (late Early Maastrichtian). This zonal scheme provides greater precision in the regional correlation of the Shiranish Formation in NE Iraq, firmly establishes the Campanian/Maastrichtian boundary, and constrains the timing of sea-level fall from the latest Campanian onwards, which is consistent with evidence for marine regression globally.

RBNJ thanks the Kurdistan Regional Government (KRG) for funding this work. We also thank Rob Wilson for his help during imaging of microfossils, and Colin Cunningham for thin section preparation at the University of Leicester. IPW publishes with permission of the Executive Director of the British Geological Survey (N.E.R.C.). The authors thank two anonymous reviewers, and GeoArabia’s Editor Mike Stephenson and Assistant Editor Kathy Breining for their helpful comments and for proof reading the manuscript. We also thank GeoArabia’s Production Co-manager, Nestor “Nino” Buhay IV, for designing the paper for press.

Stratigraphic position of sample numbers given in plates 1-3.

The specimens illustrated in this paper are deposited in the British Geological Survey, Keyworth, Nottingham. The MPA numbers are the British Geological Survey numbers for the samples from which the fossil specimens come.

Azmer section

ASH-02, MPA63960, 1.5 m above the base of the Shiranish Formation.

ASH-10, MPA63961, 15 m above the base of the Shiranish Formation.

ASH-15, MPA63962, 22 m above the base of the Shiranish Formation.

ASH-25, MPA63963, 37 m above the base of the Shiranish Formation.

ASH-40, MPA63964, 57 m above the base of the Shiranish Formation.

ASH-52, MPA63965, 73 m above the base of the Shiranish Formation.

ASH-62, MPA63966, 87 m above the base of the Shiranish Formation.

Dokan section

DSH-05, MPA63967, 12.5 m above the base of the Shiranish Formation.

DSH-08, MPA63968, 17.5 m above the base of the Shiranish Formation.

DSH-15, MPA63969, 29.5 m above the base of the Shiranish Formation.

DSH-36, MPA63970, 64 m above the base of the Shiranish Formation.

DSH-48, MPA63971, 85 m above the base of the Shiranish Formation.

DSH-80, MPA63972, 148.5 m above the base of the Shiranish Formation.

DSH-86, MPA63973, 162 m above the base of the Shiranish Formation.

DSH-88, MPA63974, 167 m above the base of the Shiranish Formation.

DSH-90, MPA63975, 171 m above the base of the Shiranish Formation.

DSH-103, MPA63976, 195.5 m above the base of the Shiranish Formation.

DSh-110, MPA63977, 212 m above the base of the Shiranish Formation.

DSH-116, MPA63978, 226.5 m above the base of the Shiranish Formation.

DSH-117, MPA63979, 228 m above the base of the Shiranish Formation.

Rawand Bakir Noori Jaff completed his Bachelors degree in the Geology Department at the University of Sulaimani, Iraq in 2005. He then joined the same department as an Assistant Geologist in 2005, finishing his Masters degree in the same University in 2008 on the sequence stratigraphy of the Palaeocene-Eocene succession in the Kurdistan region, NE Iraq. Rawand is currently a PhD student at the University of Leicester, UK where he is researching the Upper Cretaceous record of foraminifera in Kurdistan.

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Mark Williams is a Geologist at the University of Leicester where he researches climate and environmental change reflected in the fossil record. A graduate of the University of Hull (UK) in 1987, he completed his PhD at Leicester University (UK) in 1990 and subsequently has worked at the Universities of Frankfurt, Lyon and Portsmouth, and for the British Geological Survey and British Antarctic Survey. He has a strong interest in the geology of the Arabian Peninsula and has consulted for Saudi Aramco. He is Professor of Geology at Leicester.

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Ian Wilkinson is Principal Scientific Officer with the British Geological Survey. A graduate of the University of Wales, Aberystwyth (UK), he went on to conduct both Masters and PhD projects in calcareous micropaleontology. With some forty years experience, Ian is a specialist of both Mesozoic and Cenozoic ostracods, foraminifera and stratigraphy, and his research underpins survey mapping and research projects. He also contributes actively to commercial work.

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Fadhil Lawa is Assistant Professor in the Department of Geology of Sulaimani University (Iraq). He researches regional geology, sequence stratigraphy and palaeontology. His PhD work focussed on sequence stratigraphy. For many years Fadhil worked for the Iraqi Geological Survey, and since 1991 he has participated in the establishment and development of the Kurdistan Geological Survey and Kurdistan Geological Society (being president of the latter between 1994 and 2000).

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Sarah Lee is a Sedimentologist and Teaching Fellow in the Department of Geology at the University of Leicester. Sarah gained her Geology degree from Cardiff University (UK) in 1992 and completed an MSc in Applied Oceanography at Bangor University (UK) in 1994. She worked in the Geology Department at Cardiff University and in 1999 obtained her PhD, where, as part of the LISP-UK program, she investigated the sedimentological and geochemical properties of modern estuarine sediments.

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Jan Zalasiewicz is Senior Lecturer in the Geology Department at Leicester University. A geologist, stratigrapher and palaeontologist, Jan graduated from the University of Sheffield (UK) and then took up a PhD position in Cambridge working on the Lower Palaeozoic geology of North Wales. He later joined the British Geological Survey, where he worked as a mapping geologist and field biostratigrapher on the geology of East Anglia and central Wales. As well as consultancy work that includes analysis of the rocks of the Arabian Peninsula, Jan is also the author of three popular science books on geology.

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