Early Palaeocene Parvularugoglobigerina and late Eocene Praetenuitella: does evolutionary convergence imply similar habitat?

The species of the earliest Palaeocene planktonic foraminiferal genus Parvularugoglobigerina are characterized by a small test with a smooth, microperforate wall and an elongate aperture. Pore-mound structures may occur on some specimens, while the coiling mode varies from high- to low-trochospiral. Four morphotypes are distinct enough to be recognized as species: P. eugubina (Luterbacher & Premoli Silva) is low spiral and multichambered and P. perexigua n. sp. is four-chambered; P. fodina (Blow) has a Globigerina bulloides-type morphology and P. alticonusa n. sp. has a high trochospire. With the exception of the high spire, this general morphology is repeated in late Eocene forms classified as Praetenuitella: P. insolita (Jenkins), P. patefacta Li, and other associated forms. The two groups acquired their strong similarities – highly distinctive, peculiarly elongated aperture and microperforate walls – through evolutionary convergence, not by being directly related. Stratigraphically they each have a brief occurrence in a geologically significant slice of Palaeogene time: the one during the recovery of ecosystems in the earliest Palaeocene; the other immediately prior to the great cooling and in the time of rapid change known as the Terminal Eocene Event. This study shows that Praetenuitella flourished in eutrophic conditions and that their evolution might have been nutrient-driven. We suggest by morphological pattern analogy that forms of Praetenuitella and Parvulorugoglobigerina reflect similar habitat in their similar form and especially in their aperture.


INTRODUCTION
introduced the generic name Parvularugoglobigcrina to include forms described as and related to Globigerina eugubina Luterbacher & Premoli Silva (1964), occurring immediately above the Cretaceous/Palaeogcne (K/P) boundary. Using schematic drawings, Hofker referred forms with heavy pustules to the type species euguhina. Smit (1982), however, showed that eugubina is smooth and finely (rather than heavily) pustulate and microperforatc, although the micropores are scattered and difficult to observe. Globorotalia (Turborotalia) longiapertura Blow (1979) falls within Smit's (1982) species concept for Clohigerina eugubina; accordingly, we treat longiaperta as a junior synonym of eugubina. This view has been followed by several others including Boersma & Premoli Silva (1983), Toumarkine & Luterbacher (1985), Brinkhuis & Zachariasse (1988) and Keller (1988), but Canudo et a/. (1991) considered longiapertura as a distinct species. Specimens of P. eugubinu from the Millers Ferry section in Alabama have recently been found to possess pore-mounds on the wall surface (Olsson et a/., 1992), whereas most individuals are smooth with scattered micropores. Wall texture aside, the most conspicuous character of P. eugubina is the highly elongate aperture. Praetenuitella spp. from the late Eocene also possess an elongate aperture. Beginning with a comparison of the two groups, this study considers the implications of the strongly convergent development of the aperture, which is most unusual among the Cenozoic planktonic foraminifera in its form. Material from DSDP Holes 152 and 577, ODP Hole 749B and the Otway Basin in southern Australia was examined and some typical specimens of selected species are illustrated.

PAR VULARUGOGLOBIGERINA 1. Test and coiling
The test in most species of Paruularugoglobigerina has 8-12 subglobular to globular chambers, with 4-7 in the final whorl. Chambers increase slowly in the inner whorl but rapidly in the outer, final whorl. The test diameter ranges commonly from 80-150 p m (PI. I), although tests as large as 220pm have been found (Olsson, 1992, pers. comm.). Coiling is dominantly low trochospiral, as seen in the type species, P. eugubina (PI. 1, figs 1-11), but intermediates are common between the low-and high-trochospiral forms (PI. 2,figs 8,9).

Surface texture
The wall is smooth but may be slightly rugose due to the overgrowth of calcite particles on many specimens in our material. Unlike the true pustules, these calcite particles, or pseudopustules, are closely packed (see also Hemleben et al., 1991: Olsson et a/., 1992. This can be easily observed when specimens have been poorly preserved or slightly dissolved (Pl. 1, fig. 7; PI. 2, fig. 3). On the other hand, forms with typical pore-mounds (Pl. 1, figs. 3-7) have similar, but less distinct, characters to those on the triserial Guembelitria cretacea Cushman. This has led Olsson et al. (1992) to propose their affinity, i.e. the parvularugoglobigerines may be the direct descendants of G. cretacea. This can be disputed because the pore-mound structure has been observed independently on several forms which are phylogenetically unrelated: the early Cretaceous Blefuscuiana (see illustrations in Banner & Desai, 1988;Banner et al., 1993), the late Cretaceous to early Palaeocene G. cretacea and Oligocene-Miocene Cassigerinella chipolen-SO s.1. Banner & Desai (1988) suggested that the origin of P. eugubina could be descended directly from late Cretaceous Blefuscuiana with minimal morphological change.
The perforations on P. eugubina, when observable, are extremely small, about 0.2-0.3 p m in diameter, and irregularly distributed (Pl. 1, figs 2, 3, 6, 7). With about 5 micropores per 100 pm', pore density of P. eugubina is the lowest among the Cenozoic microperforate planktonic taxa, as is the porosity which is only 2% or less (Li, 1991).

MORPHOTYPES OF PAR VULA R UGOGLOBIG ERINA
Four morphotypes here grouped within the genus Paruularugoglobigerina are considered to warrant taxonomic distinction. They are P. eugubina (Luterbacher & Premoli Silva), P. fodina (Blow), P. perexigua n. sp. and P. alticonusa n. sp. Specimens of the eugubina-type and perexigua-type are both characterized by a low trochospire, but they can be separated by 5 or more and only 4 chambers in the final whorl respectively. By contrast, P. fodina possesses a medium-high spire and an almost circular aperture, while P. alticonusa is high and has an elongate aperture similar to that of typical eugubina. Detailed taxonomic discussions on these and several related taxa are presented in Appendix A.

EVOLUTION AND DISTRIBUTION OF PAR VULARUGOGLOBIGERINA
Paruularugoglobigerina is now known to be a microperforate genus having various morphotypes. Changes in the spire height from high to low or vice versa, accompanied by changes in the apertural location, are useful for differentiation of species (or morphotypes). Some morphotypes have been misidentified; those, for example, with four-chambered tests described by Brinkhuis & Zachariasse (1988) among others, as Globigerina fringa Subbotina should be the new species P. perexigua, because the types of G. fringa possess a cancellate wall and belong therefore in the eoglobigerines (Berggren, 1990, pers. comm.;. Similarly, the records of P. minutula from various K/P boundary sections (e.g. Smit, 1982;as G. conusa, 1989as G. conusa, in Keller, 1988 should be changed to P. alticonusa, for Globigerina minutula Luterbacher and Premoli Silva is in fact an early subbotinid with a distinct cancellate wall (Premoli Silva, 1990, pers. comm.), although the type material has recently been found to be so heavily recrystallized 'that the wall texture was completely uninterpretable' (Olsson, 1992, pers. comm.). From our present knowledge of this group, however, it became diverse shortly after the K/P boundary mass extinction (Premoli Silva, 1977;. Figure 1 shows the approximate ranges of Parvularugoglobigerina spp. and other genera in the early Palaeocene. From the K/P boundary section at El Kef in NW Tunisia, Brinkhuis & Zachariasse (1988) suggested that both Globoconusa minutula (= P. alticonusa) and P. fringa ( = P. perexigua) probably evolved from a benthic form Caucasina, simply by increasing chamber volumes to achieve buoyancy. This suggestion may confirm Hofker's (1978) view that Paruularugoglobigerina might have arisen from the larval stage of a benthic form. But alternative explanations are equally tenable. For example, Banner & Desai (1988) concluded that the Cretaceous Blefuscuiana was its likely ancestor, while we obeserved a complete transitional series between the triserial-biseral planktonic Guembelitria-Woodringina and Paruularugoglobigerina spp. from DSDP Hole 465A. On the other hand, Olsson et al. (1992) derived both Paruularugoglobigerina and Globoconusa from Guembelitria, on the evidence that early representatives of these genera are all similar to Gumbelitria in having a microperforate and mounded wall, although diagenetic calcite growth may alter this wall surface texture. Also like Guernbelitria, many forms of Paruularugoglobigerina (referable to P. alticonusa) are high trochospired. From the El Kef section, Brinkhuis & Zachariasse (1988), Keller (1988) andD'Hondt & reported that forms of the alticonusa-type (= P. minutula, or P. morphotype 1 of these authors) occurred together with the compressed P. eugubina. If Gumbelitria is the ancestral form, then the immediate descendant to mark the establishment of the genus Paruularugoglobigerina must be P. alticonusa, from  which all other parvularugoglobigerine morphotypes evolved in succession. We therefore suggest the evolutionary bioseries to be likely from P. alticonusa to perexigua (and fodina) to eugubina, where P. fodina may only represent a short branching from the main stock ( Fig. 1). After a short period of proliferation, all species of Paruularugoglobigerina became extinct within Zone P1, leaving no direct descendants. (In contrast, Blow (1979) and Banner (1989) suggested that this lineage might lead to the appearance of several early Palaeocene groups, including Globanomaha .) Species of Paruularugoglobigerina occur immediately above the KIP boundary in the earliest Palaeocene and indicate an age older than 65 Ma in the early part of Zone Pa of Blow (1979) (Berggren et al., 1985), a level now recognized as Zone PO (Smit, 1982;Olsson et al., 1992). A recent discovery by Montgomery et al. (1992) that a clastic event bed at the Brazos River KIP boundary section previously attributed to the latest Cretaceous is in fact the earliest Palaeocene. The presence of several Cretaceous species in that layer is due to reworking which had occurred several times during earliest Palaeocene time.
A reconstruction of the spatial distribution of P. eugubina ( Fig. 2) shows that this species is widely distributed, with high abundances inferred in upwelling regions during the earliest Palaeocene. It may reach 50% in samples from the eugubina zone from many localities, including Spain (Smit, 1982), Denmark (Boersma & Premoli Silva, 1983, Shatsky Rise (Gerstel et al., 1986) and Tunisia (Keller, 1988). In polar areas it is rare or absent, and the planktonic foraminifera1 fauna there is dominated by fringa-type, macroperforate forms (Stott & Kennett, 1990, Weddell Sea, Antarctica;Berggren, 1992, Kerguelen Plateau).

Explanation of Plate 2
Purvularugoglobigerina spp. from the basal Palaeocene (Zone Pa). Scale bar = 50 y m unless indicated otherwise.  Another species commonly encountered is P. alticonusa. Smit (1982) and Brinkhuis & Zachariasse (1988) demonstrated that this species (as G. conusa) is the second most common microperforate species in Palaeocene sections in Spain and Tunisia. It was also recorded in this study from DSDP Hole 152 in the Caribbean and DSDP Hole 577 on Shatsky Rise. O n the other hand, the geographic distributions of both P. fodina and P. fringa are poorly known, although the former was found in its type locality in DSDP Hole 47.2 on Shatsky Rise by Blow (1979) and in Hole 152 in this study.

THE LATE EOCENE PRAETENUITELLA, AN ANALOGUE OF PARVULARUGOGLOBIGERINA?
The genus Praetenuitella, erected by Li (1987) and discussed further by Li et a / . (1992), includes the late Eocene tenuitellids with a small maximum test size (about 150pm) characterized by a smooth, microperforate wall and by an elongate aperture (Pls 3 and 4). Represented by P. insolita (Pl. 3, figs 1-12; P1. 4, figs 7-9) and P. patefacta (Pl. 4, figs 1 -4), Praetenuitella is believed to have originated from Pseudohustigerina and subsequently given rise to Tenuitella spp. close to the Eocene/Oligocene boundary. Uncertainty remains because Pseudohastigerina is planispiral and smooth-walled, whereas Tenuitella is trochospiral and pustulate-walled. Although the trochospiral coiling is constantly low, Praetenuitella mimics the apertural character of Parvularugoglobigerina and these two taxa, as shown in Plates 1-4, are extremely similar in overall test morphology, thus representing one of the strongest convergent developments among Cenozoic planktonic foraminifera. The late Eocene Praetenuitella is a homeomorph of, but phylogenetically unrelated to, the early Palaeocene Parvularugoglobigerina.
Unlike the parvularugoglobigerines, Praetenuitella had issue, giving rise to Tenuitella close to the Eocene-Oligocene boundary in an evolutionary transformation recorded in many localities (Li, 1991). Brief notes on Praetenuitella species are given in Appendix B.
Praetenuitella insolita was described from a short interval in the Port Elizabeth section in New Zealand, where it extends from just below the highest Acarinina collactea

Explanation of Plate 3
Praetenuirellu spp. from the late Eocene of the Browns Creek Formation, Otway Basin, southern Australia (see McGowran et ul., 1992 for discussions on stratigraphy and palaeoenvironment). Scale bar = 50 Fm. Figs 1-7, 9, 10. Pruefenuitella insolita (Jenkins). This species is characterized by 4-5 oval chambers in the final whorl, a smooth wall surface and a rather convex dorsal (spiral) side. Fig. 8. Intermediate form between P. insolifa and P. putefacta (see PI. 4). Figs 11, 12. Intermediate specimens between P. insolira and P. pruegemma (see PI. 4) with more than 5 chambers in the final whorl. (Finlay) to just below the highest Globigerinatheka spp. (Jenkins, 1966). The composite range in southern Australia is very similar or even identical, extending as it does from one recorded co-occurrence with Acarinina primitiva (Finlay) at the base (correlated approximately with the P141P15 boundary), to the topmost records which are with the last Globigerinatheka (McGowran, 1991). The brief range of P. insolita coupled with their sometimes high frequency encouraged the establishment and recognition of a P. insolita zone (= Globorotalia insolita zone of Jenkins & Orr, 1972) in the southern hemisphere (Nocchi et al., 1991;Li et al., 1992). The zone is distinctive and easily recognized particularly at high southern latitudes, as at ODP Hole 749B on the Kerguelen Plateau (Fig. 4). Kaiho (1984) found similar forms in Japan but most records are from the southern hemisphere ( Fig. 3; see also Quilty, 1976;Jenkins & Srinivasan, 1985).

77.
The occurrence of P. insolita in neritic sediments in southern Australia gives us some insight into the species' preferences. Figure 5 shows the relative abundances of 'Tenuitella gemmalmundalinsolita' (which is mostly P. insolita in the late Eocene). Visual inspection shows a distinct tendency to associate with Chiloguembelina cubensis and Pseudohastigeria micra. This group of species collectively is high in its relative abundance when Globigerinatheka is low and vice versa. That suggests fluctuations in nutrient, Globigerinatheka being the more oligotrophic. But the Blanche Point Formation as a whole is grey-green to black with high carbon content and very rich in opaline silica, and its benthic foraminiferal faunas are rich in uvigerinids and bolivinids (McGowran & Beecroft, 1986). The combined foraminiferal (benthic and planktonic), organic geochemical, macrofossil and sedimentary evidence suggests a brief time of high productivity on the southern Australian margin in both open and restricted environments. That brief time essentially is confined to third-order cycles 4.2-(lowermost) 4.3 or, approximately, to planktonic foraminiferal zones upper P15-Pl6 (Fig. 6).
The narrow band of high productivity signalled especially by the accumulation of opaline silica, organic carbon and benthic foraminifera1 biofacies is neither a localized nor only a neritic phenomenon. The Oamaru Diatomite in New Zealand and the diatomite at Fundo Desbarrancado in Peru are in the same silica window, which in Peru is constrained by the radiolarian Calocyclas bandyca subzone (McGowran, Marty et al., 1989). The silica window thus is trans-Pacific at least, and is sandwiched between a significant warming event early in the late Eocene and the great cooling at the end. We believe that it signifies a brief time of intensified upwelling. Be that as it may, though, the close parallel in time of the silica window and the common and morphologically distinctive P. insolita is significant. It is significant too that Praetenuitella appears first at the time of a pronounced spike in abundances of chiloguembelinids at the zone P14/P15 boundary at higher latitudes in the Atlantic Ocean, and that its peak in abundance in the silica window is at the next chiloguembelinid spike in zone P16 (spikes are in Boersma & Premoli Silva, 1989;Li & Radford, 1991). The P16 spike in the ocean thus is coeval with the neritic spike in C. cubensis shown below the maximum flooding surface of cycle TA4.2 (Fig. 5).

DISCUSSION AND CONCLUSION
It has been suggested that the evolutionary recovery of planktonic foraminifera after the Cretaceous/Palaeogene boundary event was due to the re-establishment of temperate to warm climate and a new ecosystem in the water column of the global ocean in the earliest Palaeocene. The evidence for that conclusion is rapid colonization and speciation at all latitudes . The most conspicuous evolutionary response is the diversification among the triserial guembelitriids and biserial chiloguembelinids (Boersma & Premoli Silva, 1989). Although they did not attain the levels of the chiloguembelinids, species of Paruularugoglobigerina commonly constituted 20-50% of the total fauna. Predominating in mid-latitudes and upwelling regions, the parvularugoglobigerines may have been opportunists seeking nutrientrich waters in the earliest Palaeocene . The small maximum test size and the typical elongate aperture might relate to rapid reproduction and large populations with a range of phenotypes. Eutrophic to highly eutrophic conditions, as depicted by Hallock et al. (1991), are commonly occupied by r-mode opportunists which in this case included the chiloguembelinids and globigerinids. Because opportunistic species can inhabit a broad range of conditions and respond to physical instability they are usually long-lived, in the mode of generalists. Unlike opportunists, however, parvularugoglobigerines occurred only in the earliest Palaeocene for a time span of about half a million years, indicating that they speciated as eutrophic colonizers (Table 1). A record of rare P. eugubina in some early Palaeocene sections, such as the Brazos River Section in Texas (Keller, 1989), may indicate a relatively warm, nutrient-poor environment there, unless it had been obscured by hiatuses (Montgomery et al., 1992).
We can use the ecological notions of r-and K-selection related to the trophic resource continuum (TRC) in the photic zone (Hallock et al., 1991; and relate the fluctuating fortunes of neritic and planktonic communities to the palaeoceanographic events of the Palaeogene at geological, not ecological, time scales. Perhaps reduced oceanic mixing enhances a tendency toward stratification, both oligotrophy and eutrophy at the respective extremes of the T R C and niche specialization, whereas cooling stimulates mixing and promotes opportunism. In broad terms, the diverse communities in K-mode develop in the latest Cretaceous, late Palaeocene-early Eocene, and middle to late Eocene. Following the perturbations at the Cretaceous/Palaeogene, early/middle Eocene and Eocene/Oligocene boundaries respectively, we find survivors or opportunists (see also McGowran, 1991. Populations of Praetenuitella occurred most commonly within the late Eocene which broadly was a time of partial restoration of K-mode communities following the Khirthar transgression (shown on Fig. 6). But the sum of evidence suggests high productivity at the actual times of common Praetenuitella, as discussed above. This may well be due to a pronounced leakage of nutrients into what becomes the silica window at one end of an expanded TRC, still at a time of general warmth (at least at the surface, although bottom waters never warmed greatly again after the global cooling in the early middle Eocene). A cooling spike is shown in   1987,1989). Time scales, third-order sequences and Shackleton's (1986) isotopic curves, correlated using the Berggren et al. (1985) scales. Wilson Bluff to Aldinga: marine transgressiods in southern Australia; Wilson Bluff is but part of the fndo-Pacific Khirthar transgression. It is suggested that the Khirthar transgression and the great cooling in the earliest Oligocene bound the partial restoration of a stratified ocean, Within that time span there is the narrow 'silica window' based on the occurrence of the Fundo Desbarracando, Blanche Point and Oamaru siliceous deposits. Note that the neritic-oceanic silica window spans the neritic record of common 'Tenuitella spp.' (mostly Praetenuitella isolita) in Fig. 5. Fig. 6 in Zone P16, although it is premature to take correlations at this resolution too seriously in the late Eocene. At present we cannot say whether that event was the stimulus for high productivity or its very opposite, the preceding warming at the Tuketja transgression. The most recent evidence for that comes from the deep sea in the Southern Ocean (Miller, 1992). The essential point here is not the mechanism but the association of test morphology and facies.
The similar wall in Parvularugoglobigerina and Praetenuitella may reflect similar conditions where slightly corrosive waters are prevailing because, like modern high-latitude forms such as Neogloboquadrina pachyderma and Tenuitellinata uvula (Hemleben et al., 1989), they show a similar pattern in the test morphology, the test became smooth and the porosity decreased. But physiochemical variables were balanced and dissolution was rare. The small, delicate test would otherwise have been dissolved and the variation of various morphotypes eliminated. The growth of calcite crystals on the test wall of P. eugubina, according to Olsson et ul. (1992), is evidence that the species might be well resistant to dissolution.
The subsequent oceanographic developments in both the Palaeocene and the latest Eocene to early Oligocene may have generated and enhanced competition between the new and surviving species. Warming in the early Palaeocene gave oligotrophic forms, such as the subbotinids and acarininidmorozovellids, opportunities to diversify, whilst forcing Parvularugoglobigerina to extinction in Zone P1. By contrast, the pronounced cooling with steepening thermal gradients close to the Eocene-Oligocene boundary stimulated the replacement of Praetenuitella by the typical tenuitellids (Li, 1991). Unlike their Palaeocene counterparts which left no distinct morphotypes, Praetenuitella spp. were able to change to Tenuitella gernrna (Jenkins) and related forms with a pustulate wall and a low aperture in the earliest Oligocene. Some of their descendants, including Tenuitellinata juvenilis (Bolli) and Globigerinita glutinata (Egger) show typical characters of opportunists: little morphological variability and long ranges (Table 1).
In summary, Parvularugoglobigerina and Praetenuitella are unique in possessing a microperforate, smooth test with an elongate aperture. There are variations, particularly in the details of the microperforate wall texture and the trochospiral coiling. Morphotypes of Parvularugoglobigerina exhibit a wall sometimes with pore-mounds and a coiling mode from high to low, while Praetenuitella spp. are constantly smooth and rather low trochospiral. Their respective radiations coincided with two short but significant events in the Cenozoic: the initial return of a normal planktonic ecosystem in the earliest Palaeocene and the climatic fluctuations in the late Eocene. We suggest by morphological pattern analogy, in our ignorance of morphological function, that these forms reflect similar habitat in their similar form and especially in their aperture. The mechanism producing their peculiar morphology may lie in a similar life style in nutrient-rich, oxygen-poor upper waters. This study thus partially supports the suggestion of Banner & Desai (1988) that all microperforate, non-spinose and non-muricate globigerines preferred such eutrophic conditions where the particle-size of the seston was smallest.
edita, Globigerina Subbotina, 1953. Brinkhuis & Zachariasse (1988 assigned some medium-spired microperforate forms to Globigerina edita. Although showing transitional morphology between P. alticonusa and P. eugubina, the specimens illustrated by these authors may not truly represent Subbotina's species. With a mean size of 250 pm, the type of G. edita is almost twice as large as the specimens assigned to it by these authors. In his work, Blow (1979) did not recognize this species in any small-sized groups but regarded it as a large-sized Eoglobigerina. Blow also described a subspecies E. edita praeedita, and both edita and praeedita are distinctly cancellate. Olsson et al. (1992) clarify the matter by confirming that edita is a cancellate Eoglobigerina.
eugubina, Globigerina Luterbacher & Premoli Silva, 1964. P1. 1, figs 1-11. This form is characterized by a slightly to strongly flattened test commonly with 5 or more chambers in the final whorl. The test size, commonly <150pm, is variable, as forms as large as 220pm have been measured (Olsson, 1992, pers. comm.). Chambers are subtriangular to oval in strongly compressed tests but become subglobular to globular in tests with increasing spire height. The aperture is constantly elongate, with or without a thin lip. Smit (1982) first clarified the species concept of P. eugubina but retained it in the genus Globigerina. The typically mounded to microperforate wall, however, indicates that it is not a Globigerina. The specimens with heavy pustules as drawn by Hofker (1978) might have been mistaken for those with overgrowth of calcite due to dissolution when viewed with light microscopes. The massive calcite crystals are now interpreted by Olsson et al. (1992) to signal its dissolution-resistant capacity. In contrast to these views, Canudo et a/. (1991) used longiapertura for those compressed morphotypes. extmsa, Globigerina Blow, 1979. Similar to Parvularugoglobigerina spp. in having a smooth, microperforate wall and an elongate aperture, this taxon may represent a morphotype of this group. Its medium-high trochospiral test and the oblique extraumbilical aperture explicitly show transitional features between those in P. alticonusa and P. eugubina (see PIS. 1-2). It is thus considered to be an intermediate form between the latter two.
fodina, Eoglobigerina Blow, 1979. P1. 2, figs 6, 7. This is a rare but typically smooth-walled morphotype of Parvularugoglobigerina. Unlike P. eugubina, P. fodina has a medium-high trochospire with an aperture which is almost circular on the umbilical side. Chambers are inflated or globular, with 3-4 constituting the final whorl. Bordered with a thin lip, its circular aperture represents an extreme variation to the Globigerina bulloides-type morphology. As Globobastica Blow possesses a densily pustulate wall and is probably a junior synonym of Globoconusa Khalilov (Li, 1991), it should not embrace this smooth-walled species, as suggested by Canudo et a/. (1991).
fringa, Globigerina Subbotina, 1953. Stainforth et a / . (1975), Smit (1982) and  all considered Globigerina fringa to be densely perforate to weakly cancellate, so that G. fringa should be considered as typical Eoglobigerina and probably synonymous with E. eobulloides, as in Stainforth et al. (1975) and Toumarkine & Luterbacher (1985). Material from Russia did show G. fringa to be cancellate (Olsson, 1992, pers. comm.). For this reason, any proposals that G. fringa might be a parvularugoglobigerine could not be upheld, and all the previous records of P. fringa by authors should be considered to represent those of the new species P. perexigua. hariana, Postrugoglobigerina Salaj, 1986(fide Loeblich & Tappan, 1988. This is a trochospiral form with pore-mounds found in the lowermost Palaeocene of Tunisia. The overall morphology overlaps with that observed in some Parvularugoglobigerina eugubina and P. fringa. It appears to us that the type specimens of this taxon probably represent an immediate descendant from Guembelitria. hillebrandti, Globigerina Orue-Etxebarria, 1985. The medioperforate to weakly cancellate wall in this taxon is similar, if not identical, to that in Globigerina fringa of Stainforth et al. (1975) and Smit (1982), although its chamber enlargement in the final whorl is slow. Whether G. hillebrandti and G. fringa of authors represents a single species is not clear, but the cancellate wall suggests that G. hillebrandti belongs to neither Globigerina nor Parvulurugoglobigerina, but to Eoglobigerina. longiapertura, Globorotalia (Turborotalia) Blow, 1979. This work follows the conventional view that this species is a junior synonym of P. eugubina (Smit, 1982;Li & Radford, 1991;Olsson et al., 1992). By contrast, Canudo et al. (1991) recognized this species for forms with a compressed, multichambered test and a narrow elongate aperture, some extreme variants of P. eugubina (above). Further work is necessary to resolve this. minutula, Globigerina Luterbacher & Premoli Silva, 1964. According to Krasheninnikov & Hoskins (1973) and Boersma & Premoli Silva (1983), this is a weakly cancellate form having affinity with Subbotina triloculinoides, although Stainforth et al. (1975) regarded it as a junior synonym of Globigerina fringa. In contrast, Smit (1982) illustrated a smooth, microperforate form as representing this taxon. Smit's species concept was followed by Brinkhuis & Zachariasse (1988) but as Globoconusa minutula. This study, however, identifies all high trochospiral forms with a smooth and microperforate wall as P. alticonusa (see below), for the same reason as indicated by Premoli Silva (1990, pers. comm.), that typical minutula represents an early Subbotina because it bears a weakly cancellate wall.
perexigua, Parvularugoglobigerina n. sp. P1. 2, figs 1-5. This is a tiny form (about 8 0 p m ) with only 4 chambers in the last whorl but possessing a microperforate, smooth wall as in the majority of P. eugubina. Otherwise it is similar to equally small but weakly cancellate Eoglobigerina fringa (Subbotina  fig. 9. Description. Test small, high trochospiral, chambers subglobular, four in the final whorl, wall smooth to weakly pustulate, early part sometimes with pore mounds, aperture elongate, extending obliquely from the base of last chamber near the umbilicus to the apertural face, with a distinct lip. Remarks. This species is proposed to include forms described by authors as Globigerina minutula (Luterbacher & Premoli Silva) which, however, is a medium-spired, cancellate form. See above for notes on these two species.

Description.
Test small, about 80 p m , low trochospiral, chamber subglobular, increasing rapidly, four chambers in the final whorl, wall smooth to weakly pustulate, rarely with pore mounds, aperture elongate, extraumbilicalperipheral, or extending to the upper part of the apertural face, with or without a thin lip.
Remarks. This species is proposed to include forms which have been widely misidentified as Globigerina fringa by several workers. Studies of Russian material by the Palaeogene Planktonic Foraminifera] Working Group, however, indicate that G. fringa belongs to the cancellate group (Olsson, 1992, pers. comm.) and should be considered a species of Eoglobigerina . See above for notes on these two species.
patefecta, Praetenuitella Li, 1987. PI. 4, figs 1-4. Similar to P. impariapertura, this taxon has a high elliptical test outline with more than 5 chambers in the final whorl, a flat dorsal side and a wide umbilicus, but can be identified by its more distinct trochospiral coiling with a flat spiral side and an aperture being peripheral-extraumbilical-umbilical, rather than only peripheral-(short) extraumbilical.
praegemma, Praetenuitella Li, 1987. PI. 4, figs 10, 11. This form is recognized by its four-or five-chambered, biconvex test and an extraumbilical aperture. It differs from the immediate early Oligocene descendant Tenuitella gemma (Jenkins) in having a smooth to weakly pustulate (rather than heavily pustulate) microperforate wall.