New palynological, sedimentological, and geochemical records spanning the Middle Eocene Climatic Optimum (MECO; ca. 40 Ma) in the equatorial Atlantic Ocean indicate that peak warming was associated with upper-ocean stratification, decreased export production, and possibly harmful algal blooms, followed by slight oxygen minimum zone expansion. Combining these findings with published MECO records suggests that export production collapse and benthos starvation during the zenith of MECO warmth were widespread in the Atlantic. Furthermore, comparison to records across the Paleocene-Eocene thermal maximum (ca. 56 Ma) at the same site suggests a similar system response to warming, but with different impact on benthic communities.
Rapidly rising atmospheric CO2 concentrations are currently driving upper-ocean warming and acidification (IPCC, 2013). Warming and associated intensification of the hydrological cycle contribute to stronger upper-ocean stratification and expansion of oxygen minimum zones (OMZs), particularly in regions already prone to these conditions, such as low-latitude regions (Stramma et al., 2008). Moreover, warming in conjunction with nutrient-rich runoff and stratification is increasing the global occurrence of harmful algal blooms (HABs), including toxic dinoflagellate blooms (Fu et al., 2012). Both OMZ expansion and HAB development have detrimental economical and ecological effects on coastal areas (Anderson et al., 2012), and prediction of their occurrence in a progressively warmer climate is an urgent challenge.
Past events of climate change allow assessment of marine environmental and ecological responses to warming. Records of Paleogene transient global warming events such as the Paleocene-Eocene thermal maximum (PETM; ca. 56 Ma) indicate stratification, OMZ expansion, increased phytoplankton productivity (Carmichael et al., 2017), and perhaps HABs (Sluijs et al., 2018). Comparatively little is known about the environmental effects of more gradual warming phases, such as the Middle Eocene Climatic Optimum (MECO; ca. 40 Ma). While the MECO reached less extreme maximum temperatures than the PETM, the magnitude of deep- and surface-ocean warming of 3–6 °C was comparable (Bohaty et al., 2009; Dunkley Jones et al., 2013). Warming, biotic turnover, and OMZ expansion during the PETM have recently been documented at Ocean Drilling Program (ODP) Site 959 in the eastern equatorial Atlantic Ocean (Frieling et al., 2018). We generated similar palynological, sedimentological, and geochemical records at the same site to assess the tropical response to MECO warming.
ODP Site 959 (3.6276°N, 2.7352°W) is located in the Deep Ivorian Basin offshore West Africa, near the crest of the subsided Cote d’Ivoire–Ghana Marginal Ridge (Mascle et al., 1996). In the modern ocean, this region is characterized by seasonal upwelling and phytoplankton blooms (Signorini et al., 1999) and an OMZ at 400–500 m water depth (Karstensen et al., 2008). During the MECO, the site was also positioned at bathyal depths and equatorial latitudes (Fig. 1). Middle–upper Eocene sediments at Site 959 consist of relatively organic-rich, carbonate-lean, porcellanites (diagenetically altered biogenic silica) and siliciclastics, suggesting a similar high-productivity setting (Mascle et al., 1996; Wagner, 2002). The MECO interval at Site 959 was previously identified based on biostratigraphy, chemostratigraphy, and paleothermometry (Cramwinckel et al., 2018; van der Ploeg et al., 2018; see the GSA Data Repository1).
We used palynological materials from the study of Cramwinckel et al. (2018) for quantitative determination of dinocyst abundance. Bulk sediment elemental compositions were determined using inductively coupled plasma–optical emission spectrometry (ICP-OES; Perkin Elmer Optima 3000) in total acid–digested solutions. Stable carbon (δ13C) and oxygen (δ18O) isotope ratios of bulk carbonate were measured using a Thermo Scientific Kiel IV carbonate device coupled to a Thermo Scientific MAT 253 isotope ratio mass spectrometer (IRMS). Total organic carbon (TOC) and nitrogen contents were measured on decalcified bulk sediment using a Fisons elemental analyzer, and stable carbon isotope ratios of TOC (δ13Corg) were subsequently determined using a Finnigan DELTAplus IRMS. Polar fractions separated from the total lipid extracts of Cramwinckel et al. (2018) were desulfurized for five samples across the MECO interval, which were then analyzed by gas chromatography–mass spectrometry to assess the presence of isorenieratene and derivatives. For characterization of bioturbation, high-resolution images were made using a GEOTEK Geoscan-III line-scan camera (see the GSA Repository for detailed methods).
RESULTS AND DISCUSSION
Background Middle Eocene Setting
A productive oceanographic setting at Site 959 during the middle Eocene is indicated by several lines of evidence, including relatively high abundances of heterotrophic protoperidinioid dinocysts and a biosiliceous lithology with relatively high TOC (Fig. 2). Fairly low abundances of detrital components (Al, Ti, Fe, Zr, and K), negligible amounts of terrestrial palynomorphs and lipid biomarkers, and δ13Corg values (–25‰ and –27‰) consistent with Eocene marine organic matter (Hayes et al., 1999) indicate that terrigenous input was limited (Supplementary Data). Dinocyst assemblages are dominated by the open-marine taxa Spiniferites spp. and Operculodinium spp. Based on these observations, productivity was dominantly fueled by upwelling rather than fluvial nutrient input, in agreement with the offshore position of the site. The long-term increase in Ba content (560–500 m below seafloor [mbsf]) suggests a long-term post-MECO increase in export production, which is mirrored in absolute protoperidinioid contents (Fig. 2). In the same interval, a modest increase in terrigenous input is indicated by slightly lower hydrogen index values for organic matter (Wagner, 2002), increasing branched and isoprenoid tetraether (BIT) index values, and higher C/N ratios (Fig. DR1).
Harmful Algae and Hyperstratification During Peak MECO
The MECO at Site 959 is recorded as a gradual warming from background temperatures of ∼29 °C to a peak of ∼33 °C, followed by gradual cooling (Cramwinckel et al., 2018). Peak temperatures are associated with an acme of Polysphaeridium zoharyi (>70% of the total dinocyst assemblage; Fig. 2; Fig. DR2), which represents the cyst of the extant dinoflagellate Pyrodinium bahamense. This bloom-forming species can produce neurotoxins, and high abundances are restricted to subtropical–tropical lagoonal habitats (Usup et al., 2012). Polysphaeridium zoharyi occurs in open-ocean environments of the study area at present, although never in high abundance (<10% of total dinocysts; Marret, 1994). P. zoharyi and related taxa also preferred low- to mid-latitude coastal waters in the Paleogene, and carbon isotopic signatures of Eocene specimens suggest this group was bloom-forming (Sluijs et al., 2018). Given the lack of terrestrial input (Fig. DR1), these lagoonal dinocysts were unlikely to have been transported offshore to Site 959 from the shelf. We therefore surmise that P. zoharyi thrived in situ in the open ocean during the MECO, similar to recorded blooms of this species in the Arabian Sea during phases of hyperstratification in warm Pleistocene interstadials (Reichart et al., 2004). We suggest similarly strong thermally induced stratification facilitated the complete life cycle of P. zoharyi during the zenith of MECO warmth in the equatorial Atlantic. Although we cannot assess if high P. zoharyi cyst abundance reflects true biological blooms, as abundances in cells per liter of paleoseawater cannot be determined, these harmful algae were certainly abundant in particulate matter exported to the seafloor.
Subsurface and Seafloor Conditions
Background Middle Eocene Setting
Our reconstructions of seafloor conditions suggest that inferred high sea-surface productivity throughout the middle Eocene study interval at Site 959 was linked to high organic matter export fluxes. Sediments are relatively rich in TOC (averaging ∼1.6%), palynomorph preservation is good, and, overall, trace-element concentrations mirror the geochemical composition of sediments underlying upwelling sediments in the modern ocean (Brumsack, 2006) (Fig. 2). Especially in the younger part of the record, Corg/Ptot values rise markedly above those associated with the Redfield ratio of algal matter (Corg/Ptot ≈ 106), indicating some regeneration of P resulting from low-oxygen conditions at the seafloor. However, the trace fossil assemblage (Planolites, Chondrites, Zoophycos, Thalassinoides, and Teichichnus; Fig. 3; Table DR1) and consistent presence of organic benthic foraminiferal linings and Mn (Fig. 2; Fig. DR1) throughout the Site 959 study section indicate at least occasional seafloor oxygenation. Combined, these lines of evidence indicate that an extensive midwater OMZ was likely present, although the seafloor was not hypoxic.
In the post-MECO interval (560–500 mbsf), TOC contents increase progressively, and redox-sensitive trace elements, including Zn, Ni, Cr, Cu, V, and particularly Mo, record slight enrichments (i.e., typically <100 ppm; Fig. 2). We interpret this as vertical expansion or intensification of the OMZ toward the seafloor. This is consistent with inferred increasing productivity due to long-term strengthening of upwelling throughout the late post-MECO Eocene at Site 959 (Wagner, 2002; Cramwinckel et al., 2018).
Export Production and Benthic Food Limitation during the MECO
Within the MECO interval at Site 959, redox tracers and TOC together indicate more reducing bottom water conditions compared to the pre-MECO interval. Isorenieratene or its derivatives were not detected, however, suggesting that photic zone euxinia did not develop during the MECO. Synchronous with peak MECO warming and the P. zoharyi acme, ichnofossils derived from burrowing organisms decrease in average diameter, and benthic foraminiferal linings decrease in abundance (Fig. 2). This benthic community change was likely unrelated to seafloor deoxygenation, as peak OMZ expansion (based on Cr, Cu, V, and Zn increase) and potential increases in productivity (based on Ba and TOC increase) at 577 mbsf postdate peak MECO warmth (∼580 mbsf). Organic carbon delivery to the sediments is a major factor governing the body size of benthic organisms (Rex et al., 2006). We therefore interpret the decrease in size of bioturbating benthos as resulting from decreased organic carbon delivery to the seafloor during peak MECO warmth. Enhanced warmth likely added to seafloor food shortages by decreasing the efficiency of export productivity and by increasing organic carbon remineralization in warm subsurface waters (Laws et al., 2000). Combined, we infer that intensified thermal stratification during peak MECO suppressed upwelling and thus sea-surface (export) productivity, resulting in seafloor food shortage. These changes were immediately followed by increasing productivity and subsurface deoxygenation during the MECO recovery phase.
Combined with published results, these data reveal spatially variable environmental and ecological change across the MECO (Fig. 1; see also references in Table DR2). Peak MECO warmth was also linked to decreased export productivity and benthos starvation at ODP Site 1263 in the South Atlantic, based on coupled planktic-benthic records (Boscolo-Galazzo et al., 2014, 2015), suggesting this response was widespread in the Atlantic, possibly through stratification. Dinocyst assemblages from the southwest Pacific also indicate more oligotrophic conditions during the MECO (Bijl et al., 2010). In contrast, records of planktonic siliceous and carbonate microfossils from the Southern Ocean and Tethys indicate increased surface-ocean productivity that in turn stimulated benthic communities (e.g., Witkowski et al., 2012; Luciani et al., 2010; Table DR2). These regional differences testify to a pronounced change in global ocean nutrient distribution across the MECO.
Comparison of System Response to MECO and PETM at ODP Site 959
The Eocene record at Site 959 provides the unique opportunity to compare the system response to warming between the PETM (Frieling et al., 2018) and the MECO. Warming of ∼4 °C led to seawater deoxygenation during both events, although the middle Eocene high-productivity background setting was possibly more susceptible to OMZ expansion compared to the late Paleocene (Wagner, 2002). Intriguingly, while the benthos was adversely affected during the MECO at Site 959, the PETM is instead marked by increased amounts of benthic foraminiferal linings and sustained bioturbation. Another difference is the sharp regional demise of eukaryotic primary producers during peak PETM warmth (Frieling et al., 2017, 2018), likely related to higher absolute temperatures than those reached during the MECO.
We reconstruct short-lived stratified conditions and high abundance of harmful algae during peak MECO warmth at eastern equatorial Atlantic ODP Site 959, that led to a drop in export production and food limitation of benthic communities. Compilation of these data with other available MECO records (Boscolo-Galazzo et al., 2014, 2015) suggests that export production collapse and benthos starvation during the zenith of MECO warmth might have been widespread in the Atlantic Ocean. At Site 959, these oceanographic and biological changes were immediately followed by subsurface deoxygenation as stratification decreased. Qualitatively, these changes are analogous to present-day trends (Breitburg et al., 2018; Fu et al., 2012), underlining the observation that development of stratification and deoxygenation is an inherent Earth system response to warming. The occurrence of possible harmful dinoflagellate blooms during the MECO is also qualitatively similar to modern trends and suggests that future warming and stratification are increasingly preconditioning oceans for harmful algal blooms.
We thank Tim Bralower and two anonymous reviewers for constructive comments that improved the manuscript. This research used samples and data provided by the International Ocean Discovery Program (IODP) and its predecessors. We thank the Netherlands Earth System Science Centre (NESSC), financially supported by the Dutch Ministry of Education, Culture and Science. Sluijs thanks the European Research Council for Consolidator grant 771497. We thank Ellen Thomas for providing benthic foraminiferal lining identifications; Thomas Wagner for providing total organic carbon data; Niels van Helmond, Joost Frieling, and Matthew Huber for discussions; and Giovanni Dammers, Arnold van Dijk, Coen Mulder, Natasja Welters (Utrecht Geolab), Vera Lukies (MARUM), and Anchelique Mets (NIOZ) for analytical support.