Paleoecology and evolutionary response of planktonic foraminifera to the mid-Pliocene Warm Period and Plio-Pleistocene bipolar ice sheet expansion

. The Pliocene-Recent is associated with many important climatic and paleoceanographic changes, which have shaped the biotic and abiotic nature of the modern world. The closure of the Central American Seaway and the development and intensiﬁcation of Northern Hemisphere ice sheets had profound global impacts on the latitudinal and vertical structure of the oceans, triggering the extinction and radiation of many marine groups. In particular, marine calcifying planktonic foraminifera, which are highly sensitive to water column structure, exhibited a series of extinctions as global temperatures fell. By analyzing high-resolution ( ∼ 5 kyr) sedimentary records from the Eastern Equatorial Paciﬁc Ocean, complemented with global records from the novel Triton dataset, we document the biotic changes in this microfossil group, within which three species displayed isochronous co-extinction, and species with cold-water afﬁn-ity increased in dominance as meridional temperature gradients steepened. We suggest that these changes were associated with the terminal stages of the closure of the Central American Seaway, where following the sustained warmth of the mid-Pliocene Warm Period, bipolar ice sheet expansion initiated a world in which cold-and deep-dwelling species became increasingly more successful. Such global-scale pa-leoecological and macroevolutionary variations between the Pliocene and the modern icehouse climate would suggest signiﬁcant deviations from pre-industrial baselines within modern and future marine plankton communities as anthropogenic climate forcing continues

The timing of closure for the Isthmus of Panama at ∼ 4.7-2.7 Ma (Keigwin, 1978(Keigwin, , 1982;;Keller et al., 1989;Haug and Tiedemann, 1998;Haug et al., 2001;Groeneveld et al., 2006;Steph et al., 2006Steph et al., , 2010;;Molnar, 2008;Fedorov et al., 2013;O'Dea et al., 2016) remains contentious, though the ultimate role of this event in late Cenozoic icehouse evolution is clear, proving to be pivotal to the intensification of Northern Hemisphere glaciations.The precise dating of the final isthmus A. Woodhouse et al.: Paleoecology and evolutionary response of planktonic foraminifera formation is less essential than the repercussions of the gradual shoaling and restriction of the Central American Seaway (CAS), which triggered significant global paleoceanographic effects fundamental to the evolution of the present climate state.The gradual restriction of consistent throughflow between the tropical Atlantic and Indo-Pacific Oceans via isthmus formation (O'Dea et al., 2016) was coupled with bipolar cryosphere development that significantly restructured global vertical and meridional temperature gradients (Schmidt et al., 2004a, b;Mudelsee and Raymo, 2005;Boscolo-Galazzo and Crichton et al., 2021;Boscolo-Galazzo et al., 2022;Ford et al., 2022;Gaskell et al., 2022), altering marine ecosystems and trophic structure (Woodhouse and Swain et al., 2023).The recorded effects on global paleoceanography and biodiversity are of particular importance, as this ice sheet expansion was preceded by the sustainedly warmer world of the Pliocene.In particular, the mid-Pliocene Warm Period (mPWP, 3.264-3.025;Dowsett et al., 2012;Haywood et al., 2016) is increasingly imperative to our understanding of future climate change as global continental configuration, faunal and floral distributions, mean global temperatures (2-3 • C warmer than pre-industrial), and pCO 2 (350-450 ppm) were comparable to levels expected by the closure of the twenty-first century (Chandler et al., 1994;Haywood et al., 2000Haywood et al., , 2016;;Jiang et al., 2005;Pagani et al., 2010;Seki et al., 2010;Bartoli et al., 2011;IPCC, 2022).
Here, we report the high-resolution biotic response of planktonic foraminifera during the terminal stages of closure of the CAS in the Eastern Equatorial Pacific (EEP) Ocean, focusing on the co-extinction of three members of the genus Dentoglobigerina through documentation of high-resolution (∼ 5 kyr) paired single-specimen morphometric, with multiand single-specimen geochemical analyses, and their paleoceanographic implications.Moreover, we assess the global paleoecological response of planktonic foraminifera from the Pliocene to the Recent, assessing the role of the transition from the sustained warmth of the Pliocene to the bipolar icehouse world of Pleistocene-Recent on global planktonic foraminiferal macroevolutionary dynamics.

Site selection
The integrated Ocean Drilling Program Expedition 321 Site U1338 (Hole 1338A) (2 • 30.469N, 17 • 58.162 W), situated in the EEP, was drilled to 410 m below seafloor (mbsf) through Holocene -early Miocene pelagic sediments (Pälike et al., 2010).At ∼ 3 Ma, the site was at ∼ 2 • N paleolatitude (Drury et al., 2014) in a deep-water pelagic environment of similar water depth to the modern (∼ 4 km).The primary lithologies represented are calcareous, diatomaceous and radiolarian nannofossil oozes and chalks.Despite the deepwater settings, and primarily calcareous nature of the sediments, excellent microfossil preservation has been recorded in planktonic foraminiferal specimens through intervals of this core (Fox and Wade, 2013;Woodhouse et al., 2021).A preliminary assessment of core U1338A was carried out to determine the approximate position of the extinction of several species of Dentoglobigerina (∼ 3 Ma) based on tropical biostratigraphy (Wade et al., 2011), and shipboard paleomagnetic data (Pälike et al., 2010).

Foraminiferal assemblage analysis
Sediment volumes of 20-40 cm 3 were collected and washed with de-ionized water over a 63 µm sieve; the residues were dried in an oven at 40 • C and split.All samples were examined using a Zeiss Stemi 305 Compact Stereo Microscope.Planktonic foraminifers were identified following the taxonomy of Kennett and Srinivasan (1983), Schiebel andHemleben (2017), andWade et al. (2018).We performed assemblage counts on >63 µm splits yielding >300 individuals (Table S1 in the Supplement).Assessments of taxonomy and test preservation of foraminifera were performed via analysis with the Tescan VEGA3 XM Scanning Electron Microscope (SEM) at the University of Leeds, UK.

Morphometric analysis
Specimens of the genus Dentoglobigerina were measured to compare species size with stable isotope ratios to investigate species ecology and ontogeny.Complete specimens of Dentoglobigerina were picked and mounted in umbilical posi-123 tion on card slides pierced with a fine needle to accommodate the variably spired nature of species in the genus (Wade et al., 2018).Specimens were imaged umbilically using a Zeiss Axio Zoom V16 microscope with attached Canon EOS 100D camera at ×19.4 magnification.All specimens were then rotated 90 • laterally and imaged whilst propped onto their penultimate chamber.Images were processed using the image analysis software Image Pro Premier, and the maximum test diameter, previously deemed a statistically repeatable measurement amongst Dentoglobigerina (Brombacher et al., 2017b(Brombacher et al., , 2018;;Woodhouse et al., 2021), was captured from both orientations, and the lower of the two values assigned as test size.
Specimens of Cibicidoides wuellerstorfi were also used to create a benthic foraminiferal δ 18 O record for this study to supplement the shipboard paleomagnetic data (Pälike et al., 2010).This record was constructed and tuned to the Ocean Drilling Program Site 849/IODP Site 1338 stack constructed by Lyle et al. (2019) using QAnalySeries software (Kotov and Pälike 2018) to better constrain the timing of events (see Woodhouse et al., 2021), where the study section is calculated to represent the Pliocene interval from ∼ 3.47-2.98Ma.

Global data analysis
To investigate how planktonic foraminiferal macroevolution and paleoecology has developed since the Pliocene, the Triton dataset (Fenton and Woodhouse et al., 2021) was downloaded, and all macroperforate planktonic foraminiferal records occurring from 5.3-0 Ma (early Pliocene-Recent) were binned into 53-time bins with equal length (100 kyrs).Species were assigned the speciation and extinction datums in accordance with Aze et al. (2011) and Fenton and Woodhouse et al. (2021), and all species occurrences located outside of these assigned stratigraphic ranges were removed.This range trimming was applied to eliminate much of the occurrence data likely attributable to misidentification and/or reworking that may create artificial "tails" within speciation and extinction data (Liow et al., 2010;Lazarus et al., 2012;Flannery-Sutherland et al., 2022).The trimming of taxa resulted in a dataset of 239 317 planktonic foraminiferal occurrences.Furthermore, all species were assigned to their respective "ecogroups", which represent broad ecological categories based on paleoecological and phylogenetic data (Aze et al., 2011).These ecogroups are defined as: ecogroup 1 = surface mixed layer dweller with photosymbionts, ecogroup 2 = surface mixed layer dweller without photosymbionts, ecogroup 3 = thermocline dweller, and ecogroup 4 = subthermocline dweller, ecogroup 5 = highlatitude.
Comparing the assemblage composition of warm and surface dwellers against cold and deep dwellers, we document generally consistent species abundances until ∼ 36.26 m b.s.f.(∼ 3.08 Ma), where the assemblage exhibits consistently greater abundances of cold and deep dwellers for the rest of the record (Fig. 2).

Global Pliocene-Recent Ecogroup trends
The global proportions of planktonic foraminiferal ecogroups within the Triton dataset (Fenton and Woodhouse et al., 2021) show that throughout the time interval studied (5.3-0 Ma), surface mixed layer dwellers without photosymbionts (orange) proportions remain relatively consistent, making up ∼ 10 % of the total global fauna (Fig. 5).From 5.3-3 Ma, global ecogroup proportions are relatively consistent, where the dominant forms are thermocline dwellers (cyan) and surface mixed layer dwellers with photosymbionts (red) (Fig. 5), making up ∼ 40 % and ∼ 35 % of the global fauna, respectively.During this interval, the proportion of subthermocline dwellers (blue) and high-latitude forms (yellow) also remain relatively consistent with ∼ 10 % and <5 % of total proportions, respectively.After ∼ 3 Ma, both thermocline dwellers and surface mixed layer dwellers with photosymbionts show a steady decline in global representation approaching the Recent, making up ∼ 20 % each in the modern ocean.At ∼ 3 Ma, both the subthermocline dwellers and high-latitude ecogroup start to show increases in their proportions, though this increase approaching the modern is much greater in the latter group.During the last 100 kyrs, subthermocline and high-latitude species have constituted ∼ 15 % and ∼ 25 %, respectively (Fig. 5).

Discussion
Few major changes in the assemblage composition are observed through the study interval, other than the isochronous extinction of D. altispira, D. baroemoenensis, and D. globosa at ∼ 3.037 Ma (Fig. 2; 35.50 m b.s.f.), and the influx of the two species M. cf.exilis and M. cf.pertenuis through ∼ 3. .56m b.s.f.), defined henceforth as the "Menardella acme" (Figs. 2 and 6).
Studies of extant species suggest a strong positive correlation between planktonic foraminifera δ 13 C and test size, paired with a lack of a strong negative significant relationship in δ 18 O and test size, is indicative of species bearing photosymbiotic algae (e.g., Berger et al., 1978;Bouvier-Soumagnac and Duplessey, 1985;Spero andWilliams, 1988, 1989;Spero et al., 1991;Spero, 1992;Spero and Lea, 1993;Ravelo and Fairbanks, 1995;Norris, 1996;Birch et al., 2013).Our data suggests that all three species of Dentoglobigerina studied here are symbiont-bearing, displaying mean stable isotope data similarly to the symbiont-bearing surface mixed layer dwelling G. ruber (Figs.2-4).Moreover, the regression lines for the ancestor-descendent pair D. globosa -D.altispira are remarkably similar, suggesting that the species share similar stable isotope-test size relationships, despite the speciation of D. altispira occurring ∼ 20 Myrs prior (Aze et al., 2011;Wade et al., 2011Wade et al., , 2018)).However, the substantially fewer data for D. globosa currently limits the significance of this observation for this particular species (Fig. 3).
The results presented here contribute to the variety of interpretations from previous studies on the paleoecology of D. altispira.Spanning different ocean basins throughout the species' stratigraphic range they suggest: a shallow-dwelling (e.g., Keller and Savin, 1985;Vincent et al., 1985;Prentice and Matthews, 1988;Corfield and Cartlidge, 1991;Norris et al., 1993;Hodell and Vayavananda, 1994;Sosdian and Lear, 2020), deep-dwelling (Opdyke and Pearson, 1995;Pearson  and Shackleton, 1995), or lower mixed layer/upper thermocline (Zou et al., 2022) ecological niche habit.Woodhouse et al. (2021) suggested that prior to extinction, the D. altispira geochemical signal may signify that this species underwent adaptive ecological niche migration across multiple depth habitats.Upon further investigation, by isolating all D. altispira specimens present after the migration horizon at ∼ 3.061 Ma (Woodhouse et al., 2021), we show that these specimens do, in fact, display a steeper negative relationship between δ 18 O and test size (Fig. S1), consistent with asymbiosis; however, this relationship lacks statistical significance.Nevertheless, this observation lends support to the conclusions of Woodhouse et al. (2021) that this species underwent niche adaptation prior to extinction.
Another plausible scenario may be the existence of indeterminate cryptic diversity within the D. altispira morphospecies complex where multiple ecological strategies or phylogenetic expressions may be present (e.g., Huber et al., 1997;Bijma et al., 1998;de Vargas et al., 1999de Vargas et al., , 2002;;Weiner et al., 2012;Schiebel and Hemleben, 2017;Nirmal et al., 2021;Pearson and Penny, 2021), and the stepwise changes observed by Woodhouse et al. (2021) may indicate the systematic loss of "cryptic genotypes" within this morphospecies complex.Indeed, Pearson and Penny (2021), hypothesized that dramatic abundance switches in the Indo-Pacific Warm Pool of ecologically distinct, alternately coiled populations of Pulleniatina morphospecies may signify re- placement by distinct cryptic genotypes, and such coiling switches are noted throughout the planktonic foraminiferal fossil record (Ericson et al., 1955;Saito et al., 1975;Bossio et al., 1976;Hallock and Larsen, 1979;Hornibrook, 1982;Scott et al., 1990;Norris and Nishi, 2001;Winter and Pearson, 2001;Crundwell and Nelson, 2007;Wade et al., 2011;Pearson and Ezard, 2014;Crundwell, 2015a, b;Levin et al., 2016;Wallace et al., 2019;Crundwell and Woodhouse, 2022a, b).Therefore, the range of interpreted paleoecologies in D. altispira may, in fact, be due to the occurrence of distinct cryptic populations from across the geological record.Irrespectively, the abiotic conditions at this time appear to have become fatally detrimental to the entire ecological habit of all three morphospecies of Dentoglobigerina analyzed in the EEP, and subsequently across the entire globe (Shackleton et al., 1995;Chaisson and Pearson, 1997;Wade et al., 2011;Raffi et al., 2020;Groeneveld et al., 2021;Woodhouse et al., 2021).

The Menardella acme
The transient influx and co-occurrence of M. cf.exilis and M. cf.pertenuis from ∼ 3.45-3.36Ma may indicate a shared ecological affinity between these species (Fig. 2; Kennett and Srinivasan, 1983;Knappertsbusch, 2016).Furthermore, this association may suggest that these two similar forms exist within the same genetic species complex, though further study on internal shell ontogeny and external morphology would be required to confirm this hypothesis.Notably, however, Kaneps (1970) and Chaisson (2003)    "aberrant" forms of Menardella limbata and Menardella menardii, with the M. exilis-pertenuis plexus being solely endemic to the Atlantic basin (Sexton and Norris, 2011).Scanning election photomicrographs and pore density analysis of Menardella morphospecies within this study (Fig. 6; Table 1) suggests that the M. cf.exilis and M. cf.pertenuis morphotypes ascribed to "aberrant" forms may, in fact, be phylogenetically distinct from both M. menardii and M. limbata, as well as from the endemic Atlantic M. exilis-pertenuis plexus.Where the Atlantic type specimens exhibit finely perforate tests (Kennett and Srinivasan, 1983), the specimens within this study appear to show test perforation intermediate between "normally perforate" menardellids such as M. menardii and M. limbata (Fig. 6), and the "finely perforate" M. exilis-pertenuis plexus (Kennett and Srinivasan, 1983;Chaisson, 2003).Whether all Indo-Pacific occurrences of these morphotypes (e.g., Brönniman and Resig, 1971;Jenkins and Orr, 1972;Thunell, 1981;Keigwin, 1982;Thompson, 1982;Chaisson and Leckie, 1993) exhibit similar test perforation remains to be determined.However, these forms could represent either: (1) convergent evolution of a geographically isolated endemic population restricted to the Indo-Pacific triggered by vicariance, or (2) specimens within the M. exilis-pertenuis plexus exhibiting a differential phenotypic expression of pore density, potentially due to regional differences in paleoceanography between the Atlantic and Indo-Pacific basins at this time (Haug et al., 2001).Irrespective of the biological implications, this acme event may represent a regionally valuable biostratigraphic marker horizon.

Pliocene EEP paleoceanography
Comparing the assemblage composition of warm and surface dwellers against cold and deep dwellers, we document a gradual turnover from an assemblage exhibiting relatively even abundances of these two groups to one of increasing occupation of cold and deep dwellers from ∼ 3.08 Ma onwards (36.26 m b.s.f.; Fig. 2).This may reflect regional thermocline shoaling similar to patterns observed at DSDP Site 84 in the proximal Panama Basin (Lutz, 2010).Other geological intervals associated with significant global cooling such as the Eocene-Oligocene transition and late Miocene cooling exhibit similar patterns of gradual, successive turnover of warm-water dwellers by cold-water taxa potentially associated with contractions and expansions in their respective ecospaces (Keller, 1983;Boersma and Premoli Silva, 1991;Keller et al., 1992;Molina et al., 1993;Wade and Pearson, 2008;Ezard et al., 2011;Lowery and Fraass, 2019;Lowery et al., 2020;Boscolo-Galazzo and Crichton et al., 2021;Boscolo-Galazzo et al., 2022;Woodhouse and Swain et al., 2023).
The establishment of the Isthmus of Panama played a key role in Atlantic Meridional Overturning Circulation intensification by barring Caribbean inflow from the Atlantic (O'Dea et al., 2016;Hayashi et al., 2020), leading to a new paleoceanographic state defined by an equatorial Pacific thermocline exhibiting a high-angle east-west tilt (Fiedler and Talley, 2006;Yang and Wang, 2009;Zhang et al., 2012;Ford et al., 2015).Changes in the EEP water column structure are compounded within biotic and abiotic records, where global changes in ice volume, as shown by benthic δ 18 O (Fig. 5), and the formation of the isthmus contributed to the gradual cooling and shoaling of the thermocline (Ford et al., 2015).Isochronous records of ice-rafted debris in the North Atlantic and Pacific infer a substantial change to high-latitude global climate ∼ 3 Ma (Shackleton et al., 1984;Maslin et al., 1996;Kleiven et al., 2002;Lawrence et al., 2006).Consequently, the already restricted CAS was likely subjected to substantial eustatic sea level fluctuations (Chaisson, 2003;Bartoli et al., 2005;O'Dea et al., 2016), causing cool water within or below the thermocline to become shallow enough to be mixed by surface winds (Philander and Fedorov, 2003;Fedorov et al., 2004Fedorov et al., , 2006;;Ford et al., 2012Ford et al., , 2015)).In turn, this contributed to a dramatic increase in regional upwelling associated with further development of the EEP cold tongue (Herbert et al., 2010).We suggest that the increasing dominance of cold and deep dwellers in the EEP (Figs. 2 and  5) are a direct manifestation of the water column structure changes associated with closure of the CAS and cryosphere intensification, marking the initiation of transition from the early Pliocene "El Padre" mean state to one more similar to the modern ocean (Seki et al., 2012;Ford et al., 2012Ford et al., , 2015)).
The geochemical fluctuations noted within G. tumida from 3.071-3.061Ma (36.17-35.86m b.s.f.; Fig. 2) are coeval with the interval assigned to the "phase transition" by Woodhouse et al. (2021), in which D. altispira and D. baroemoenensis exhibit dramatic fluctuations in size and shape preceding rapid ecological changes.Here, the δ 18 O signal of G. tumida exhibits substantial and rapid changes up to ∼ 2.1 ‰, switching from typical thermocline values to those indicative of the subsurface, and back again, whereas all other water column δ 18 O value changes are nominal (Fig. 2).
If the fluctuations within the δ 18 O signal of G. tumida were related to fluctuations in its depth habitat, we would expect the inverse pattern to occur in its δ 13 C signature, as δ 13 C values decrease with depth (Cannariato and Ravelo, 1997;Ford et al., 2012;Birch et al., 2013); however, this is not the case (Fig. 2, Table S2).The maximum δ 18 O excursion value (∼ 2.1 ‰) is equivalent to a temperature change of ∼ 10 • C, based on a mid-Pliocene SMOW value of −0.3 ‰ (Williams et al., 2005;Medina-Elizalde, Lea and Fantle, 2008;Tindall and Haywood, 2015) and the paleotemperature equations of Kim and O'Neil (1997).Previous studies from EEP sites show Mg / Ca-derived thermocline temperature fluctuations of ∼ 3 • C (Site 1241; Steph et al., 2006) to ∼ 5 • C (Sites 848, 849, and 853;Ford et al., 2012) across the same interval, and modern ocean seasonal deviations within EEP surface waters are minor at ± 1 • C (Fiedler, 1992).However, these can be intensified by El Niño conditions by up to +3.8 • C (Pérez-Angel and Molnar, 2017).
Modern regional evaporation-precipitation balance within the EEP also shows very little variation, wherein δ 18 O sw values average 0.26 ‰ (Fairbanks et al., 1992), ranging from ∼ 0.2 ‰-0.5 ‰ for the entire tropical Pacific (Ravelo and Hillaire-Marcel, 2007).Factors other than temperature and salinity (e.g., chlorophyll a, the lunar cycle) that trigger species-specific habit changes (Rebotim et al., 2017) could be at least partially responsible for these dramatic changes in the G. tumida δ 18 O records; however, this species is known to calcify at the base of the photic zone (Ravelo and Shackleton, 1995), irrespective of thermocline depth (Ravelo and Fairbanks, 1992;Rincon-Martinez et al., 2011).
Despite the present low range in Pacific equatorial δ 18 O sw values, modern Atlantic-Caribbean surface waters record a salinity value ∼ 3 ‰ less than the modern EEP (Haug et al., 2001;Garcia et al., 2006;Schmidt et al., 2016;Ögretmen et al., 2020), equating to ∼ 1.5 ‰ lower in mean δ 18 O sw values (Ravelo and Hillaire-Marcel, 2007).This salinity contrast was fully established by ∼ 4.2 Ma (Haug et al., 2001), and consistent breaching of Atlantic-Caribbean waters over the still-submerged isthmus may have occurred as late as 1.9 Ma (Coates and Obando, 1996;Keller et al., 1989;Schmidt et al., 2016).Therefore, a breaching event is the most probable cause for the substantial variations in the δ 18 O record of G. tumida from 3.071-3.061Ma, where this apparently thermocline-restricted (Fig. 2) disturbance may have contributed to disruption of the Dentoglobigerina ecological niche habit at this time (Woodhouse et al., 2021).
It should be noted however, that there is a prominent increase in sampling of Quaternary high latitudes that is yet to be replicated in deep-time marine records (Lazarus, 1994;Diepenbroek et al., 2002;Sellén et al., 2010;O'Regan, 2011;Siccha and Kučera 2017;Waelbroeck et al., 2019;Renaudie et al., 2020;Fenton and Woodhouse et al., 2021).This is due to the difficulties encountered in deep-sea scientific drilling of higher latitudes through the combined impacts of unpredictable and detrimental oceanographic conditions, and ephemeral sea ice (Barker et al., 1977;Backman et al., 2006;Lamy et al., 2019;McKay et al., 2019).Consequently, the substantial increase in cold-water forms observed from ∼ 3 Ma to the Recent (Fig. 5) may be at least partly driven by sampling efforts.

Conclusions
The high-resolution planktonic foraminiferal biotic record at IODP Site U1338 chronicles important changes in late Cenozoic development of global climate and the evolutionary history of this microfossil group.The co-extinction of three species of Dentoglobigerina and the acme of M. cf.exilis and M. cf.pertenuis signify useful regional biostratigraphic markers within the Pacific chronological framework, where the former appears to be associated with abiotic changes in water column structure associated with the closure of the Central American Seaway, and intensification of bipolar cryosphere development.These three extinct dentoglobigerinids appear to exhibit a symbiotic, mixed layer ecological niche habit; however, the compilation of results from previous studies may suggest a high degree of unknown cryptic diversity within dentoglobigerinid morphospecies complexes.The abiotic extinction mechanism is likely signified by the initiation of a critical stage in the formation of Northern Hemisphere ice sheets and the accompanying changes to global paleoceanography and water column structure, where cold and deep dwelling species started to become more dominant across the globe.
Globally, planktonic foraminiferal ecological and macroevolutionary patterns were fundamentally different prior to bipolar ice sheet expansion, and past intervals with climatic conditions analogous to future-warming scenarios such as the mid-Pliocene Warm Period require further prospection at multiple spatiotemporal scales to better predict potential changes in global marine biodiversity as the Earth continues to shift away from its pre-industrial state.Furthermore, anthropogenic forcing has the capability to melt modern continental-scale ice sheets, which hold the potential to dramatically disrupt global ocean circulation patterns, nutrient distributions, and water column structure.Based on past changes in such systems, this may signify impending repercussions for planktonic foraminiferal biodiversity and other planktonic groups whose survival depends on the vertical structure of the oceanic water column.

Figure 3 .
Figure 3. Test size -δ 13 C and δ 18 O relationships for the three species of Dentoglobigerina that underwent extinction through the study section.Trend lines for each species represent linear regressions based on the entire per species dataset (dashed line).Significance (p) and measure of fit (r 2 ) were calculated for each linear regression.

Table 1 .
The number of pores per 2500 µm 2 in the penultimate chamber of select species of Menardella.